- 
 
;. ','"'',. .,' ; ' > '" 
 ; - - - 
 
 No 
 
 Division 
 
 Range 
 
 Shelf... 
 
 Received _.(_...^s. 
 
 PRINTING . BIMtl 
 
GEOLOGY OF CANADA 
 

 GEOLOGICAL SURVEY OF CANADA. 
 
 REPORT OF PROGRESS 
 
 ITS COMMENCEMENT 
 
 1863; 
 
 ILLUSTRATED BY 498 WOOD CUTS IN THE TEXT, 
 
 ACCOMPASIJCD BY 
 
 AN ATLAS OF MAPS AND SECTIONS. 
 
 OFFICERS OF THE SUEVEY: 
 
 SIR WILLIAM E. LOGAN, LL.D., F.R.S., F.G.S., DIRECTOR. 
 ALEXANDER MURRAY, ESQ., ASSISTANT GKOLOOIST. 
 T. STERRY HUNT, M.A., F.R.S., CHBMIST AND MINERALOGIST. 
 E. BILLINGS, F.G.S., PALEONTOLOGIST. 
 
 MONTREAL: DAWSON BROTHERS. 
 tX)NDON, PAEIS, AND NEW YORK: BALLIERE. 
 
 1863; 
 
V3.S 
 
 EARTH 
 
 SCIENCES 
 
 LIBRARY 
 
 MONTREAL: 
 
 JOHN LOVELL, PRINTER, ST. NICHOLAS STREET. 
 1863. 
 
GEOLOGY OF CANADA.-1863. 
 
 The Maps for the Atlas designed to accompany this volume will be as follows : 
 
 I. A colored geological map of British North America, and of the adjacent 
 parts of the United States; on a scale of 125 miles to an inch. This is reduced 
 from a map on a scale of twenty-five miles to an inch ; which is already engraved, 
 and will be published separately. 
 
 II. A detailed map of the Laurentian rocks in the counties of Ottawa, Terre- 
 bonne, Argenteuil, and Two Mountains ; on a scale of seven miles to an inch. 
 This map shows the distribution of the limestones, anorthosites, and intrusive 
 rocks of the Laurentian system, and also the outcrops of the adjacent Lower 
 Silurian formations. 
 
 III. A detailed map of the Huronian series along the north shore of Lake 
 Huron, showing also the relations of the Laurentian and Silurian systems ; on a 
 scale of eight miles to an inch. 
 
 IV. A detailed map of a portion of the Quebec group, from Stanbridge, C. E., 
 to St. Alban's, Vermont, showing also its relations to the Potsdam and Trenton 
 groups ; on a scale of two miles to an inch. 
 
 V. A map of the limestones of the Quebec group at Point Le'vis ; on a scale 
 of a mile to three inches. 
 
 VI. A map of the Superficial Geology, which will be upon the same scale as I. 
 
 All of these are engraved on steel or copper, and with the exception of IV, 
 will be printed in oil colors by chromo-lithography. 
 
 The sections, which will be about ten in number, it is proposed to give on a 
 scale of five miles to an inch. 
 
 This Atlas will not be ready before the end of the present year. 
 Montreal, August 19, 1863. 
 
(\ 
 
PREFACE. 
 
 The Geological Survey of Canada was instituted by the Provincial 
 Government in 1843 ; since which time the results arrived at in its inves- 
 tigations have been submitted to the successive Governors-General in 
 Annual Reports, which have been from time to time transmitted to the 
 Legislature, and published by authority. Of these Annual Reports, particu- 
 larly of the earlier ones, there was in general but a moderate number of 
 copies issued ; and, with the exception of one or two of the later Reports, 
 they are now all out of print. The present volume contains, in a con- 
 densed form, the substance of all the previous Reports, with much original 
 matter ; and the work may be considered a Report of Progress from the 
 commencement of the Survey to the termination of the year 1862. 
 
 In the investigation of the Geology of the Province, I have been aided 
 in the field-work, not only by the Government-appointed officers of the Sur- 
 vey, but by explorers who have received their training from me, and have 
 acted under my instructions. The results obtained by some of these have 
 in part, appeared as separate Reports, addressed to me as Director of the 
 Survey, and have been transmitted to the Government, and published with 
 my own. In the present volume however no separate mention is made 
 of the special labors of my colleagues or assistants ; and it is but due to 
 them to state, in this place, the part which each one has taken in the 
 investigation. 
 
 The explorations of my colleague Mr. Murray have extended over most 
 of the settled parts of western Canada, and over a large portion which 
 is still in forest ; and he may be said to have blocked out nearly all 
 " at is known of the distribution of the rocks in that division of the 
 province ; while, in respect to the limits of some of the formations, the 
 investigation has been carried into farther detail by others connected 
 with the Survey. He has also examined several parts of Gasp, where 
 
iv PREFACE. 
 
 his explorations include surveys of the Rivers Matanne, Ste. Anne, St. 
 John or Douglastown, and Bonaventure, and the examination of parts of 
 the Shickshock Mountains. 
 
 Mr. James Richardson, formerly a farmer settled in Beauharnois, has 
 been in the employ of the Survey nearly from its commencement, and has 
 become a most valuable and indefatigable explorer, capable of mapping 
 accurately his survey of rivers, lines of traverse through the forest, and 
 outcrops of rocks ; but he requires aid in working up his materials into a 
 report. His labors, following preliminary explorations by myself, have 
 shown, in considerable detail, the distribution of the Lower Silurian rocks 
 for a moderate distance on each side of the Ottawa, from Pembroke to 
 Grenville ; and on the north side of the St. Lawrence between Montreal 
 and the St. Maurice ; as well as on its south side from St. Regis to 
 Phillipsburgh and Laprairie. On the south side of the St. Lawrence he 
 has farther partially traced out the rocks of the Hudson River formation 
 and of the Quebec group, in some of the seigniorial lands, and in several 
 parts of the Eastern Townships. In the Quebec group his explorations 
 have embraced a portion of the country from St. Nicholas to St. Thomas, 
 and have extended almost continuously along the south bank of the 
 St. Lawrence from Riviere du Loup to the Marsouin, including a breadth 
 of from five to fifteen miles. He has examined a section across the 
 Silurian rocks from the St. Lawrence to the Restigouche, by the Great 
 Metis and Patapedia Rivers ; and another from the Marsouin across 
 the Shickshock Mountains, to the neighborhood of the Great Casca- 
 pedia. He has surveyed the Quebec group on the Magdalen, and 
 explored the Gasp^ limestones and sandstones on a line of country from 
 this river, by the Dartmouth, to Gasp6 Basin. He has partially traced 
 out the distribution of the Lower Silurian and Laurentian rocks about Lake 
 St. John on the Saguenay ; and of the Lower and Middle Silurian around 
 the Island of Anticosti in the Gulf of St. Lawrence. His examination of 
 the Lower Silurian series has been continued in the Mingan Islands, and of 
 the Laurentian system along the north shore of the Gulf between the Min- 
 gans and the Strait of Belle Isle ; where finally, by his examination of the 
 fossiliferous rocks on both sides of the strait, and the specimens which he 
 has there collected, he has afforded the means of establishing pretty 
 clearly that the Quebec group is of Lower Silurian age, and younger than 
 the Potsdam. 
 
 The work of Mr. Robert Bell, a young civil engineer, whose connection 
 with the Survey as an explorer is comparatively recent, comprises an 
 examination of some parts of the Gaspe* peninsula, in which he has added 
 to our knowledge of the distribution of the Gaspe* limestones and sand- 
 stones on the Dartmouth, York, Malbay, and Grand Rivers, and of that of 
 the Bonaventure formation behind Perce* ; as well as an examination of 
 
PREFACE. v 
 
 portions of the western peninsula of western Canada, where he has traced 
 out in greater detail the limits of the Middle Silurian rocks, of which Mr. 
 Murray had previously ascertained the general outlines. In his explora- 
 tions, Mr. Bell has devoted a good deal of attention to the phenomena of 
 Superficial Geology ; and he has aided in collecting the facts on this sub- 
 ject which have been ascertained by others connected with the Survey, 
 and by various investigators who have elsewhere published their obser- 
 vations. 
 
 Mr. J. De Cew, a provincial land-surveyor of Decewville, Cayuga, who 
 has been occasionally employed for short periods on the work of the 
 Survey, has added many details to Mr. Murray's lines along the contiguous 
 limits of the Onondaga, Oriskany, and Corniferous formations, from Middle- 
 ton to Bertie on the Niagara River. 
 
 Mr. James Lowe, a farmer settled in the township of Grenville, after 
 acquiring sufficient experience by accompanying me as assistant in my 
 explorations in his own neighborhood, has been employed in tracing out, 
 under my direction, the distribution of the crystalline limestones inter- 
 stratified in the Laurentian system, and of the intrusive masses which 
 intersect this, in the counties of Ottawa, Argenteuil, Two Mountains, and 
 Terrebonne. In this intricate investigation, in a district almost wholly 
 covered with forest, he has accumulated a great number of valuable facts, 
 which, joined to my own labors in these counties, have enabled me to prepare 
 a detailed map of the geology of this interesting region. 
 
 Mr. Richard Oatey, a practical Cornish miner, residing in Montreal, has 
 from time to time been entrusted with the examination of metalliferous 
 lodes and deposits, particularly those holding lead, copper, silver, and 
 gold, with a view of ascertaining their economic value. 
 
 The Rev. L. T. Wurtele, formerly of Lennoxville, and now of Acton- 
 vale, has on several occasions volunteered short explorations on behalf 
 of the Survey ; and we are more particularly indebted to him for informa- 
 tion, and for specimens procured on an excursion up the St. Francis River 
 from its mouth to the neighborhood of Drummondville. 
 
 My own researches embrace explorations of Lake Superior, of the north 
 shore of Lake Huron, and of the valley of the Ottawa for about 300 miles, 
 with the valley of the Mattawa to Lake Nipissing. They include also the 
 study of the Laurentian rocks on the lower part of the Ottawa, and on its 
 tributaries the Rouge and North Rivers ; investigations of the geology of the 
 valley of the St. Lawrence at various points from Maiden and Windsor, by 
 Niagara, Toronto, Belleville, Kingston, Brockville, Cornwall, and Montreal, 
 to the St. Maurice ; a continuous examination of the distribution of the 
 Lower Silurian rocks from the St. Maurice by Quebec to Cape Tourmente ; 
 and examinations of the same series at Bay St. Paul and Murray Bay, as 
 well as among the Mingan Islands. They comprehend also a preliminary 
 
vi PREFACE, 
 
 exploration of the Gaspe* peninsula, by an examination of the whole coast 
 from the Restigouche, by Port Daniel, Perce*, and Cape Gasp6, to Cape 
 Chatte ; and by two transverse lines of examination, one of them along the 
 valleys of the Chatte and Great Cascapedia, to the Bay of Chaleurs, and 
 the other by the Matapedia and Kempt road to Metis. In this region 
 they farther include a survey of the St. John, and of its tributary the 
 Black River, as well as of a transverse line of section by the Madawaska 
 River, Temiscouata Lake, and Temiscouata Portage, to Rividre du Loup ; 
 and an examination of the country along the coast from Riviere, du 
 Loup, by Kamouraska, Ste. Anne, and L'Islet, to St. Thomas, com- 
 prehending a breadth of from five to ten miles. Among these researches 
 there is embraced a detailed, but still incomplete, examination of the rocks 
 of the seigniories and townships between the Chaudidre and Lake Chan*- 
 plain. These include the strata of the Quebec group on the southeast, 
 and those of the Hudson River formation on the northwest of the great 
 break or overlap which follows the valley of the St. Lawrence from Lake 
 Champlain to Cape Rosier. There is included also, along the western 
 side of this break, an examination of the Chazy formation, and of the 
 Trenton group, from St. Dominique to Farnham, continued by Highgate 
 Springs and Swanton, to St. Alban's Bay ; and on the east of the break 
 an investigation of the Phillipsburgh series of the Quebec group from the 
 centre of Stanbridge, across St. Armand, to the road between Highgate 
 Springs and Highgate Falls ; with an examination of the Potsdam group 
 still farther eastward. In the above investigations of the Ottawa, the 
 Eastern Townships, and Gaspe*, the explorations of Mr. Lowe, Mr,. 
 Richardson, Mr. Bell, and Mr. Murray have been important auxiliaries. 
 
 The labors of my colleague Mr. T. Sterry Hunt comprehend all that 
 has been done in connection with the Survey in the chemical analyses of 
 mineral species and mineral waters, of roxjks, and of minerals capable- 
 of useful applications. His researches have also been devoted to the 
 study of rock-metamorphism. The principal results of his investigations 
 are given in his own words in the four chapters, xvii-xx ; while many 
 of them are interwoven with the matter of other parts of the volume, par- 
 ticularly that of chap, xxi, which treats of Economic Geology. The 
 chemistry of sedimentary rocks is discussed at some length in the intro- 
 ductory portion of chap, xix, where the theory of metamorphism is 
 also considered. It is there asserted that heated alkaline waters have 
 produced the alteration of sediments ; but, in opposition to the view 
 of Daubre*e, who supposes that thermal springs acting near the surface 
 have been the agents in producing this change, it is maintained that, 
 except in local and comparatively rare cases, the process has only taken 
 place in sediments so deeply buried as to be directly affected by the inter- 
 nal heat of the earth. The ingenious experiments and observations of 
 
PREPACK. Vli 
 
 Daubre*e have thrown great light upon that production of crystalline minerals 
 in which metamorphism consists ; but it must be remarked that the effect of 
 alkaline waters in producing these changes was pointed out and insisted 
 upon, as the efficient agent of metamorphism, in the Reports of the Geo- 
 logical Survey, some time prior to the first publication of Mr. DaubreVs 
 views. (See Report of Progress for 1853-56, pages 479, 480). In addi- 
 tion to his researches in the laboratory, Mr. Sterry Hunt has aided the 
 Survey by explorations among the metamorphic rocks of the Laurentian 
 series on the north and south sides of the Ottawa, and the north side of 
 the St. Lawrence, as well as of the Silurian series in the Eastern Town- 
 ships ; and he has extended his examinations to the gypsiferous and oil- 
 bearing rocks of the western peninsula of Canada. 
 
 Mr. Billings was appointed Palaeontologist to the Survey in 1856, and 
 since then his unremitting attention has been devoted to the study of the 
 Palaeozoic fossils of Canada, of which very considerable collections have 
 been made in our various explorations. Of these fossils he has described 
 in the publications of the Survey, and in the scientific journals of the prov- 
 ince, 526 species ; of which 395 are Lower Silurian, 67 Middle and 
 Upper Silurian, and 64 Devonian. He has thus greatly facilitated the 
 means of determining with precision the limits and distribution of our 
 geological formations, and of the economic substances which, they contain. 
 In order to insure uniformity in the palaeontological part of this work, all 
 the palaeozoic fossils mentioned in it have been submitted to the inspection 
 of Mr. Billings, and the species are therefore all given on his authority. 
 Of the described Lower Silurian species found in Canada, not including 
 those of the Quebec group, he has prepared a catalogue, showing their 
 vertical distribution, and referring to the publications in which the de- 
 scriptions and figures will be found. This catalogue has been introduced 
 into the Appendix to this volume. 
 
 The age of those rocks which are now termed the Quebec group, was, 
 from an early period of the Survey, a subject of considerable difficulty. In 
 a preliminary Report made to the Government in December 1842, and, 
 with others, published by authority in 1845, it was stated as my impres- 
 sion that the contorted strata of Point LeVis, which form a part of the 
 group in question, came from beneath, and were older than the flat lime- 
 stones of the Trenton formation on the opposite side of the St. Lawrence. 
 It was found however on subsequent examination, that the black shales which 
 overlie these limestones, and hold fossils of the Hudson River and Utica 
 formations, passed, with apparent conformity, beneath the Point LeVis 
 rocks. The only fossils which had at that time been met with hi these last, 
 were a species of Leptcena, and an Orthis ; since then named L. discipiens, 
 and 0. Electra. These are so like L. sericea and 0. testudinaria, that 
 they were by me mistaken for them ; and had it not been for the discovery 
 
viii PREFACE. 
 
 of their interior structure in silicified specimens, dissolved out from masses 
 of limestone by the aid of an acid,. they might still have passed for these 
 species. With this apparent superposition of the strata, seemingly uncontra- 
 dicted by fossils, as the only evidence before me, I felt constrained to relin- 
 quish my first impression ; and in 1848 and 1849 enunciated the opinion that 
 the whole series composing the Quebec group was subordinate to that of the 
 Hudson River, and to its succeeding formation, the Oneida conglomerate. 
 But the discovery in May 1860 of the Point Le*vis fossils at once enabled 
 Mr. Billings to conclude that the rocks of the Quebec group must be 
 placed near the base of the second fauna of Barrande,* or about the hori- 
 zon of the Calciferous and Chazy formations. This opinion, our subse- 
 quent investigations in the neighborhood of Lake Champlain, and of the 
 Strait of Belle Isle, have completely borne out ; and there now remains 
 little doubt that the attitude of the rocks in question in the vicinity of 
 Quebec is due to a great overlap, which runs from southwest to northeast 
 through the whole length of the eastern part of the province, and extends 
 in both directions far beyond it. Dr. Emmons in 1842 stated his convic- 
 tion that rocks in Vermont, which have since been ascertained to be 
 equivalent to those of the Quebec group, were older than the Birdseye and 
 Black River formation ; but his view of the structure of that region made 
 a large part of them older than the Potsdam sandstone. In eastern Canada 
 we have as yet no proof that any great series of strata to the southward 
 of the St. Lawrence is of higher antiquity than the Potsdam group, to which 
 that sandstone belongs. The country through which the rocks in question 
 extend is still however under investigation ; and the structure which has 
 been assumed for the purpose of conveniently describing this metalli- 
 ferous region, which appears to be one of great economic importance, 
 must for the present be considered as in some degree provisional. 
 
 Before the Geological Survey of Canada was commenced, the investiga- 
 tions of Emmons, Mather, Vanuxem, and Hall, the four geologists to whom 
 
 * This opinion of the age of the Point L^vis limestones was communicated to Mr. 
 Barrande by Mr. Billings in a letter dated 12th July 1860. Specimens of trilobites from 
 the slates of Georgia in Vermont were received from Col. E. Jewett in the latter part of 
 1858, and pronounced by Mr. Billings to belong to primordial types ; but he then thought 
 it possible that these, with the several species of Triarthrus of the Utica slate, and 
 those referred, in the first volume of the Paleontology of New York, to Olenus and 
 Jlgnostus, might constitute a colony of primordial forms (or something analogous to the 
 colonies of Barrande), in the upper part of the Lower Silurian series. This view was 
 also transmitted to Mr. Barrande in a letter written in March or April 1860 ; but the great 
 amount of palseontological evidence furnished in the following month by the Point L^vis 
 fossils, rendered it necessary to seek for some other explanation. The supposed age of 
 these fossils was first stated, as already said, in Mr. Billings's letter of the 12th July; 
 and the explanation of the structure, which brings the Quebec group into the place now 
 assigned to it, was given in my letter of the 31st December 1860. (See Canadian 
 Naturalist and Geologist, v, 472 ; and American Journal of Science [2], xxxi, 216). 
 
PREFACE. ix 
 
 was entrusted the survey of New York, had correctly established 
 the sequence in that state of all the palaeozoic formations which lie to the 
 west of the great overlap that has just been mentioned. It is therefore 
 scarcely necessary to do more than allude to the great advantage which 
 has been derived from, their labors in following out the same formations 
 through western Canada. But in addition to the general benefit obtained 
 from the investigations of Professor Hall in his own division of the state 
 of New York, we have to express our obligations to him for the assistance 
 rendered to Mr. Murray in 1856, in tracing out the boundary of the 
 Upper Devonian rocks in a part of the western peninsula. The Survey 
 will be farther benefited by the labors of this distinguished naturalist in 
 his description of the compound graptolites obtained from the Quebec 
 group at Point LeVis. This work was kindly undertaken by Professor 
 Hall before the appointment of Mr. Billings as palaeontologist to the 
 Survey, and it will shortly appear as the second Decade of Canadian 
 Organic Remains. A list of the species to be described in it has been 
 introduced into the Appendix. 
 
 Amidst his many arduous duties connected with the University of 
 McGill College, Dr. J. W. Dawson has still found time to devote atten- 
 tion to many points in Canadian geology. His investigations into the 
 character of our Post-tertiary deposits have greatly extended our knowledge 
 of the subject ; while his study of the land-plants of the Devonian rocks of 
 North America has given a new interest to this series of deposits. He 
 was first incited to an examination of this flora by the numerous specimens 
 which he found ready for examination in the collection of the Survey 
 from the Gaspe* sandstones ; and the species found in Gaspe*, although few 
 in number, naturally suggested inquiry into the vegetable remains of equiv- 
 alent rocks in other parts. Goeppert, in his memoir on the flora of the Silu- 
 rian, Devonian, and Lower Carboniferous rocks of Europe and America, 
 enumerates in 1860, fifty-nine species as known in the Devonian series up to 
 that date. In 1859, Dr. Dawson described six species from specimens col- 
 lected by himself, and by the Geological Survey, in the Devonian rocks 
 of Gaspe\ In 1861, he added fifteen other species from Perry in Maine, 
 and from St. John in New Brunswick. In 1862, having had placed in 
 his hands the collections of the New York Survey, and those made by 
 Messrs. Matthew and Hartt at St. John in New Brunswick, he raised 
 the number of American species to sixty-nine ; and in a paper read before 
 the Geological Society of London, in May 1863, he has added to these, 
 thirteen more, including two from Gaspe* ; making the whole number of 
 species in the Devonian flora of eastern North America, eighty-two, 
 belonging to thirty-five genera. Of these species eight had previously 
 been recognized in Europe, and about ten of them had been more or less 
 perfectly noticed or figured in reports on American geology. On the 
 
X PREFACE. 
 
 subject of the Post-tertiary deposits, we have availed ourselves not only of 
 Dr. Dawson's published observations, but of various manuscript notes 
 which he has kindly placed in our hands. In his investigations of these 
 deposits, Dr. Dawson has more than doubled the number of species of 
 invertebrate animals previously known in them m r and Mr. J. F. Whit- 
 eaves, so well known as a naturalist, has kindly aided in preparing a 
 catalogue of these fossils. 
 
 Mr. Sandford Fleming of Toronto has communicated to the Canadian 
 Journal several interesting papers upon points connected with the lacustrine 
 deposits of Lakes Ontario and Huron, of which use has been made in 
 describing our Superficial Geology. We have also given the ancient water- 
 margins occurring between Lakes Ontario and Simcoe, as described by the 
 late Mr. Thomas Roy of Toronto ; and we are indebted to Mr. A. Dickson 
 of Pakenham for various facts relating to the Post-tertiary formation, and 
 for specimens from this, and from the Lower Silurian rocks. 
 
 Admiral Bayfield's excellent maps of the lakes, river, and Gulf of St. 
 Lawrence have always been of the utmost aid to the Survey in such 
 explorations as came upon the great water-lines of the province. Their 
 value however is not confined to the indication of geographical features. 
 There is registered upon his charts, a considerable amount of accurate 
 geological information, in the form of notes, which he has in many places 
 given of the character of the rocks forming the coast. These notes have 
 on some occasions immediately directed attention to points of interest, and 
 at other times have saved much labor in tracing out the distribution of 
 formations. It is understood that Admiral Bayfield, in his surveys of the 
 St. Lawrence, made, with the aid of Dr. Kelly, a considerable collection of 
 organic remains, which were presented to various societies and institutions 
 of natural history. It is much to be regretted that these had not been 
 figured and described before they were thus distributed, as we should 
 thus probably have long ago obtained a knowledge of many fossils, the 
 descriptions of which have been only recently published from specimens 
 in the collections of the Survey. Admiral Bayfield has communicated to 
 the Literary and Historical Society of Quebec, and to the Geological Society 
 of London, various interesting papers on subjects connected with Canadian 
 geology, with the facts in which it will be found that we have on several 
 occasions availed ourselves. 
 
 Among the pioneers in Canadian Geology, no observer was more 
 accurate than Dr. J. J. Bigsby, secretary to the Boundary Commis- 
 sioners under the Treaty of Ghent. His range of investigation extended 
 from Quebec to Lake Superior, and beyond the limits of the province in 
 that direction ; and he has accumulated and published a great store of 
 facts, upon the exactness of which the greatest reliance can be placed. 
 He is in consequence frequently quoted in this volume as an authority. 
 
PREFACE. xJ 
 
 Lieutenant, now Major-General Baddeley, of the Royal Engineers, 
 when in Canada, now nearly forty years since, was an ardent promoter of 
 geological inquiry, and his services were made available to the Provincial 
 Government in explorations in the region of the Saguenay, and in the penin- 
 sula of Gaspe*. To him we are indebted for the first published notice of 
 the Lower Silurian limestones on Lake St. John, Bay St. Paul, and Murray 
 Bay, as well as of the existence of gold in the drift of the Eastern Town- 
 ships. Lieut. F. L. Ingall was another explorer, who about that time did 
 good mineralogical service on government expeditions; the district to 
 which his attention was directed being the country between the St. Mau- 
 rice and the Ottawa. Captain R. H. Bonnycastle, R.E., at a somewhat 
 later period interested himself in the examination of various mineralogical 
 and geological phenomena, more particularly in the neighborhood of Kings- 
 ton, where his military duties had placed him. The results of his obser- 
 vations were given in Silliman's Journal in 1831, and in other publications, 
 and have been cited in this Report. 
 
 Although Dr. James Wilson, who practised during many years as a physi- 
 cian at Perth, in the county of Lanark, has personally communicated little 
 to the public, he has devoted considerable attention to the natural history 
 of the district in which he resided, and has enriched the mineralogy of 
 the province by the discovery of several very interesting species. To him 
 we are indebted for pointing out the sandstone bed near Perth, from which 
 were obtained the specimens of Climactichnites Wilsoni; and we have on 
 several ocasions, received from him information regarding the occurrence 
 in his own neighborhood of minerals capable of economic application. 
 With the Climactichnites at Perth, there occurs also the Protichnites of 
 Owen, the first discovery of which at Beauharnois was made by the late 
 Mr. Robert Abraham, then editor of the Montreal Gazette, in which he gave 
 an interesting description of these curious foot-prints. 
 
 The late Dr. A. F. Holmes of Montreal, long a diligent collector of 
 minerals, was instrumental in bringing several Canadian species or varie- 
 ties into notice, by transmitting them for analysis to Dr. Thomas Thompson 
 of Glasgow. His cabinet has now become the property of the University 
 of McGill College, and we have on several occasions been favored with 
 authentic specimens from it, for the purpose of comparative analyses. 
 
 The late Reverend Andrew Bell of L'Orignal, from about the time 
 the Geological Survey commenced, devoted a portion of his attention to 
 the collection of fossils from the Lower and Middle Silurian rocks of 
 Canada, and at the time of his death bequeathed his cabinet to the Uni- 
 versity of Queen's College, Kingston. In addition to a large number of 
 organic remains, it contained many of the mineral species of the province, 
 and now forms the nucleus of the museum of that university, to which 
 Drs. Williamson and Lawson have since made many additions. The 
 
xn 
 
 PREFACE. 
 
 authorities of the university have, on several occasions, kindly permitted to 
 Mr. Billings the use of specimens from their museum for the purpose of 
 comparison. We are besides indebted to Dr. Lawson for several facts 
 connected with the drift. 
 
 Professor E. J. Chapman, of Toronto University, so favorably known for 
 his contributions to mineralogy, has advanced the science of geology in the 
 province, not only by his lectures in connection with the University, but by 
 such field explorations as he has had an opportunity to make ; by his col- 
 lections and descriptions of Canadian fossils ; and by his communications 
 to the Canadian Journal on various points relating to his investigations of 
 the Drift and the Silurian formations of western Canada, of which we 
 have availed ourselves. We are indebted to him for important mineral- 
 ogical observations ; and to Professor Henry Croft, of the same univer- 
 sity, for several chemical analyses. Through Professor Chapman, Mr. 
 Billings has been permitted the use, for the purpose of description, of 
 some of the corals from the Corniferous formation of western Canada, 
 which are preserved in the collections of the Canadian Institute of Toronto, 
 Professor Hind, of Trinity College, Toronto, has also favored the Survey 
 with fossils for description, from collections made by himself for the 
 museum of his college. By his excursion up the Moisie River, in Eastern 
 Canada, Professor Hind has added to our knowledge of the distribution of 
 the anorthosite rocks ; and by his explorations in the Red River region 
 he has shown the extension in that direction of the Lower Silurian and 
 Devonian series, without the intervention of the Middle and Upper Silurian. 
 
 We are indebted to the late Mr. John Head for specimens from the Cor- 
 niferous formation of western Canada, and for aid in the examination of 
 the rocks of Point LeVis. In our investigations in the vicinity of Phillips- 
 burgh, both Mr. Billings and myself have on several occasions been 
 favored with the assistance of Dr. P. J. Farnsworth ; and in the neighbor- 
 hood of Swanton we have been indebted for guidance and kindly aid to the 
 Rev. J. B. Perry and Dr. G. M. Hall, who have devoted much attention 
 to the geology of their own district. By these three gentlemen the Survey 
 has been supplied with several new species of fossils from the Quebec 
 group, which have been described by Mr. Billings. 
 
 I have in addition to express our obligations to many persons who 
 have either presented specimens of Canadian organic remains to the 
 Survey, or lent them to the palaeontologist for comparison or de- 
 scription. Among these contributors are Mr. T. Devine and Mr. E. 
 Cayley of the Crown Lands Department, Quebec, the former of whom 
 has described two new species discovered by himself; Mr. G. Barnston, 
 Mr. II. G. Vennor, Dr. W. Eraser, Mr. T. Peel, Mr. W. Bulmer, and Mr. 
 N. S. Whitney, of Montreal, as well as the Montreal Natural History 
 Society ; Mr. T. E. Blackwell and Mrs. A. M. Ross, formerly of Montreal ; 
 
PREFACE. Xlii 
 
 Dr. J. A. Crevier of Ste. Cesaire ; Mr. Brown of Hawkesbury ; Dr. E. 
 Vancortlandt, Dr. James Grant, and Mr. J. Mackinnon, of Ottawa ; the 
 Rt. Rev. Dr. Horan, R. C. Bishop of Kingston ; Mr. A. T. Drummondof 
 Kingston ; Mr. W. M. Roger of Peterborough ; Mr. J. F. Smith of 
 Toronto ; -Mr. W. Saunders of London, C. W. ; Mr. J. Dalgleish of Gait ; 
 Judge W. B. Wells of Chatham; Mr. A. D. Hager of Vermont, Col. E. 
 Jewett of Albany, N. Y., and Mr. W. Denton of Ohio. 
 
 For the localities and modes of occurrence of several mineral de- 
 posits of economic importance, more particularly of copper ores, we have 
 been indebted to Mr. Charles Robb and Mr. J. L. Willson, mining engi- 
 neers of Montreal ; to Mr. Herbert Williams, manager of the Harvey-Hill 
 mine, Leeds, C. E. ; and to Mr. R. H. Fletcher of Sault Ste. Marie, 
 C. W. Mr. T. Macfarlane, formerly of Actonvale mine, and now of the 
 Wickham mine, C. E., has also furnished valuable information, and has 
 published in the Canadian Naturalist and Geologist several interesting 
 papers on the mineralogy and geology of the province. Among these is 
 a comparative view of the rocks of Canada and Norway, in which latter 
 country Mr. Macfarlane resided for several years. 
 
 For the purpose of representing correctly the geological features ascer- 
 tained in the explorations of parts of the country which had not been 
 previously delineated topographically, it became necessary for the officers 
 and assistants of the Survey, from the very commencement of their opera- 
 tions, to measure carefully many of the rivers and other geographical lines. 
 The amount of work of this description has been very considerable ; but it 
 will be more particularly alluded to in describing the map which has 
 been constructed to show the distribution of our geological formations. 
 This map has been compiled on a scale of twenty-five miles to an inch, 
 by Mr. Robert Barlow, aided by his son Mr. Scott Barlow. A reduction 
 of it to 125 miles to an inch, with other maps, on a larger scale, showing 
 the distribution of small typical portions of the Laurentian and Huronian 
 rocks, will be given in a separate Atlas, whioji will accompany the present 
 volume, and be of a uniform size with it. The Atlas will contain in addition 
 one or two plans, and a series of sections illustrating the geological 
 structure of different parts of the province. 
 
 One of the duties imposed by the Government upon the Survey, at the 
 time of its institution, was the formation of a Provincial Museum, which 
 should illustrate the geology and the mineral resources of the country. This 
 object has been constantly kept hi view; and since a suitable building 
 has been placed at the disposal of the Survey, the Museum has gradu- 
 ally assumed a value and importance which at the present time render 
 it second to few on the continent for the special purposes to which it 
 is devoted. The Museum is separated into two parts. One of these is 
 devoted to Economic Geology, and in it are displayed specimens of such 
 
XIV PREFACE. 
 
 rocks and mineral substances as can be applied to the usoful purposes of life. 
 These are subdivided into two classes ; one of them containing the more 
 important metals and their ores, and the other what may be termed the 
 non-metalliferous mineral substances. These various materials are again 
 classified technically, pretty much in the way in which they are described 
 in the twenty-first chapter of this volume ; each specimen being placed 
 under a label giving its locality, and the geological formation to which it 
 belongs. The various substances are as much as possible reduced to 
 forms showing their uses, thus at once making the design of the arrange- 
 ment intelligible. In this division of the Museum there is a classified 
 collection of all our mineral species ; and another of our rocks, more par- 
 ticularly those of a metamorphic or of an intrusive character. This part 
 of the Museum it is proposed to illustrate farther by geological maps, 
 sections, and models. 
 
 The geographical distribution of any series of formations can scarcely be 
 followed out correctly over a large area without a preliminary knowledge 
 of the true geological superposition, or the natural order in which these for- 
 mations have been deposited. It is now well established that throughout 
 a very large proportion of the whole series of rocks composing the earth's 
 crust, the best means of determining their succession is by their fossils ; it 
 being a fundamental principal of geology that different formations are char- 
 acterised by different groups of organic remains. The study and deter- 
 mination of fossils thus becomes an indispensible part of a geological 
 survey. But these organic forms are so many and so various, and pass into 
 one another by such insensible gradations, that to make them truly available 
 requires the special attention of a person versed in natural history, and 
 indeed of one who pursues an uninterrupted study of that department of 
 natural history which is devoted to these ancient forms. Hence the 
 necessity of attaching a palaeontologist to every important geological 
 survey ; and hence no geological museum can be complete without a full 
 and properly classified collection of described organic remains from the 
 fossiliferous rocks of the area which it is designed to illustrate. 
 
 The second division of the Museum is thus devoted to the palaeontology 
 of our formations. In this division the fossils are displayed in groups, 
 which succeed one another in the order of the formations, beginning with 
 the most ancient. In each group the specimens are arranged in a natural- 
 history order, commencing with the simplest or lowest forms, and rising to 
 the highest ; and to each specimen there is attached a label giving the 
 generic and specific names of the fossil, with its geological formation and 
 locality. In order that there may be no mistake as to the fossil indicated 
 by the label, the specimens are freed as much as possible from all other 
 fossils. In order at the same time to save space, the specimens have been 
 as much as possible reduced in size. In this operation the services of Mr. 
 
PREFACE. XV 
 
 T. C. Weston, a lapidary, have been made available ; and his skill has 
 also been applied to slitting many of the cephalopods and other fossils, and 
 rocks, for the purpose of showing their internal structure. By this reduc- 
 tion in the size of the specimens we have been able to arrange a much 
 greater number in our limited space than would otherwise have been 
 
 The number of species of fossils displayed in the Museum is about 1500. 
 Figures engraved on wood of 543 of the more characteristic of these, are 
 given in the present volume. These are chiefly by Mr. J. H. Walker of 
 Montreal, with a few by Mr. A. W. Graham and Mr. G. G. Vasey ; the 
 whole from excellent drawings by Mr. H. S. Smith. With a few exceptions, 
 the species here figured are distinct from those which have already been 
 given in the Decades of Canadian Organic Remains, published by the 
 Survey. Of these, I, III, and IV have appeared, and it is expected 
 that Decade II, already referred to, will shortly be published. For the 
 descriptions of Decade I we are indebted to Mr. J. W. Salter, palaeontolo- 
 gist to the Geological Survey of the United Kingdom. It contains twenty- 
 one species from the Birdseye and Black River formation, the figures of 
 which are drawn by Mr. C. R. Bone, and engraved by Mr. W. Sowerby. 
 Decade II will contain fifty-one species of graptolitidge, by Prof. James 
 Hall "of Albany. Decade III contains twenty-nine species of Lower 
 Silurian cystideae and asteridae, described by Mr. Billings, and one species 
 of cyclocystoides, by Messrs. Salter and Billings ; with fourteen species of 
 Lower Silurian bivalved entomostraca, by Mr. T. Rupert Jones, of 
 the Geological Society of London. The figures are drawn on stone by 
 Messrs. C. R. Bone, J. Dinkle, Tufien West, G. West, and H. S. Smith. 
 Decade IV contains forty-three species of Lower Silurian crinoidea, 
 described by Mr. Billings ; the figures drawn on stone by Mr. H. S. 
 Smith, and printed by Mr. G. Matthews of Montreal. As already stated, 
 Mr. Billings has described altogether 526 species of fossils. Those not 
 included in the Decades have been published in the Canadian Journal 
 of Toronto ; the Canadian Naturalist and Geologist of Montreal ; in the 
 Annual Reports, and in the volume entitled Palaeozoic Fossils of Canada, 
 published by the Survey. 
 
 In the collection of the Survey there are probably at the present time 
 about 500 species of fossils still remaining undescribed. The publica- 
 tion of these will be an additional contribution to the general fund of palae- 
 ontological knowledge ; to which, as it has been of great utility in our own 
 investigations, we are bound to add what we can for the benefit of others. 
 But independent of the instruction derived from fossils as guides to our- 
 selves, and proofs to others in regard to the succession of our rocks, there 
 is a higher consideration attached to them than their mere utilitarian appli- 
 cation. For, as remarked by Conybeare, they bring us supplementary 
 
xvi PREFACE. 
 
 information of numerous species which have long vanished from the actual 
 order of things ; and by their resurrection they unexpectedly extend our 
 views of the various combinations of organic forms. In many instances they 
 supply links otherwise wanting, in uniting the different terms of the series 
 in an unbroken chain, and thus aid in the elucidation of those general 
 laws of natural history, the investigation of which is always of so much 
 interest to enlightened minds. 
 
 W. E. LOGAN. 
 
 OFFICE OF THE GEOLOGICAL SURVEY, 
 Montreal, May 1863. 
 
GEOLOGY OF CANADA. 1863, 
 
 ERRATA. 
 
 The reader will please to make the following corrections : 
 
 Page 11, line 6 from the foot, for Henley's read Healy's. 
 " 29, " 10 " " " supply the figure 2. 
 
 " 162 ; the numbers of the woodcuts, 161 and 162, are to be* transposed 4 . 
 
 " 268, line 19 from the foot, for Stromatopora read Stenopora. 
 
 11 420, " 20 from the head, for Devonian read Upper Silurian, 
 
 " 718, at the top, for fifteenth read fourteenth. 
 
 M 734, line 12 from the top, for Devonian read Silurian, 
 
XVI 
 
 PREFACE. 
 
 information of numerous species which have long vanished from the actual 
 order of things ; and by their resurrection they unexpectedly extend our 
 views of the various combinations of organic forms. In many instances they 
 supply links otherwise wanting, in uniting the different terms of the series 
 in an unbroken chain, and thus aid in the elucidation of those general 
 laws of natural history, the investigation of which is always of so much 
 interest to enlightened minds. 
 
 W. E. LOGAN, 
 
 OFFICE OF THE GEOLOGICAL SURVEY, 
 Montreal, May 1863. 
 
TABLE OF CONTENTS. 
 
 CHAPTER I. 
 
 INTRODUCTION. 
 
 Page 
 
 Geographical description, 1 
 
 Mountains and lakes, 2 
 
 St. Lawrence valley, 8 
 
 Lower Silurian formations, 9 
 
 Intrusive rocks, 9 
 
 Adirondack Mountains, 10 
 
 Rocks of western Canada, 11 
 
 Page 
 
 Middle Silurian escarpment, 13 
 
 The western peninsula, r . 16 
 
 The peninsula of Michigan, 17 
 
 Geology of the Great Lakes, 17 
 
 American coal fields, 18 
 
 Mississippi and Missouri Rivers, 18 
 
 Rocky Mountains, 18 
 
 CHAPTER II. 
 GEOLOGICAL NOMENCLATURE. 
 
 Divisions of the New York rocks,.. 
 Table of Canadian formations,. . . . 
 
 Rocks of Great Britain, 20 
 
 Azoic formations, 21 
 
 CHAPTER III. 
 LAURENTIAN SYSTEM. 
 
 Laurentian rocks ; their antiquity .... 22 
 
 Orthoclase gneiss, 23 
 
 Limestones and dolomites, 24 
 
 Contorted strata, 27 
 
 Conglomerates, 31 
 
 Anorthosite rocks, 33 
 
 Intrusive rocks, 38 
 
 Extent of the Laurentian system, 43 
 
 Distribution of limestones, 43 
 
 General section, 45 
 
 Laurentian rocks on Lake Superior,. . 48 
 
 Supposed fossils, 49 
 
 CHAPTER IV. 
 HURONIAN SERIES. 
 
 Rocks of Lake Temiscamang, 50 
 
 Section in Lake Huron, 52 
 
 Slates in Lake Superior, 52 
 
 Rocks of the Thessalon, 55 
 
 Stratified and intrusive diorites, 57 
 
 Metalliferous lodes, 59 
 
 Thessalon trough and dislocation, .... 61 
 
 Missisagui anticlinal, 62 
 
 Huronian series on Lake Superior,. ... 63 
 
 Azoic rocks of the northwest, 65 
 
 Azoic rocks of Missouri and Arkansas, 66 
 
 Azoic rocks of Newfoundland, 66 
 
XVU1 
 
 TABLE OF CONTENTS. 
 
 CHAPTER V. 
 UPPER ROCKS OF LAKE SUPERIOR. 
 
 Page 
 
 Upper copper-bearing rocks, 67 
 
 Lower division, 67 
 
 Sandstones, shales, and limestones,. . . 68 
 
 Beds of columnar trap, 69 
 
 Upper division, 70 
 
 Limestones and shales, 70 
 
 Page 
 
 Amygdaloids with copper, 71 
 
 Beds and dykes of trap, 72 
 
 Metalliferous lodes, 74 
 
 Distribution of the two divisions, 77 
 
 Sandstones of St. Mary, 84 
 
 Ages of these series, 86 
 
 CHAPTER VI. 
 POTSDAM GROUP. 
 
 Potsdam sandstone in New York, 87 
 
 Its distribution in Canada, 88 
 
 Conglomerates with shale, 88 
 
 Absence of the formation westward,. . 93 
 
 Sandstones of Belle Isle, 97 
 
 Sandstone of western Canada, 97 
 
 Fossils, Scolithus, etc 100 
 
 Protichnites at Beauharnois, 102 
 
 Climactichnites at Perth, 107 
 
 The sandstone a shore deposit, 108 
 
 CHAPTER VII. 
 CALCIFEROUS FORMATION. 
 
 The formation in New York, 110 
 
 On the Mississippi, 110 
 
 Sections of it in Canada, Ill 
 
 Its distribution, 113 
 
 Its absence from western Canada, .... 110 
 
 Concretionary claystone, 112 
 
 Outliers of this formation, 118 
 
 The formation at the Mingan Islands,. 119 
 
 CHAPTER VIII. 
 CHAZY FORMATION. 
 
 Its nature on the Ottawa, 123 
 
 Lingulae and phosphatic nodules, 125 
 
 Limestones of crystalline texture, .... 125 
 
 Distribution of the formation, 126 
 
 Water-lime beds, 128 
 
 Section at the Mingan Islands, 134 
 
 CHAPTER IX. 
 THE TRENTON GROUP. 
 
 Birdseye and Black River formation,.. 136 
 
 Trenton formation, 137 
 
 Section at Montreal, 137 
 
 Distribution of the formation, 139 
 
 Mount Royal, and intrusive dykes, ... 142 
 
 Montmorenci dislocation, 157 
 
 Mingan Islands and the Saguenay, .... 164 
 Distribution in the Ottawa valley,. . . . 165 
 
 The group west of Kingston,.. 178 
 
 The group on Lake Huron, 193 
 
 Dolomites and sandstone at Lacloche, 194 
 Section at Campement d'Ours, 196 
 
 CHAPTER X. 
 THE UTICA AND HUDSON RIVER FORMATIONS. 
 
 Utica slates and Loraine shales, 198 
 
 Section on the river Ste. Anne, 198 
 
 Graptolitic shales of Orleans Island... 200 
 
 Distribution of the formations, 201 
 
 Overlying red shales, 205 
 
 These formations in Eastern Canada,.. 210 
 Outliers on the Ottawa and Saguenay, 219 
 Hudson River formation on Antlcosti,. 221 
 
TABLE OF CONTENTS. 
 
 XIX 
 
 CHAPTER XL 
 THE QUEBEC GROUP. 
 
 Page 
 The Le>is and Sillery formations,. . . . 225 
 
 Section on Orleans Island, 227 
 
 Fossils of Point L( vis, 232 
 
 Age of this group, 233 
 
 Section from Montmorenci to Orleans, 234 
 Great dislocation and overturn dips, .. 234 
 
 Lower black shales, 234 
 
 Bayer and Stanbridge anticlinal, 238 
 
 Lauzon and Farnham synclinal, 241 
 
 Copper-bearing strata, 242 
 
 Shipton and St. Armand synclinal,... 245 
 
 Metamorphic rocks, 245 
 
 Danville and Sutton anticlinal, 247 
 
 Sutton Mountain, 251 
 
 Upper rocks of Lake Memphramagog,. 251 
 Stoke and Ham Mountains, 252 
 
 Page 
 
 Shipton and Leeds synclinal, 256 
 
 Northeast of the Chaudiere, 258 
 
 Shickshock Mountains, 265 
 
 Stratified serpentines of Mount Albert, 266 
 
 The Quebec group in Gaspe', 266 
 
 The Quebec group near Vermont, 273 
 
 Section at Phillipsburgh, 278 
 
 Red sandrock of Vermont, 281 
 
 Paradoxides slates, 282 
 
 The Potsdam group, 283 
 
 Straits of Belle Isle, 287 
 
 Quebec group in Newfoundland, 288 
 
 Section of the group in " 289 
 
 General considerations, 294 
 
 Conditions of deposition, 294 
 
 Ideal section of the group, 295 
 
 CHAPTER XII. 
 ANTICOSTI GROUP AND GUELPH FORMATION, 
 
 The Middle Silurian series, 298 
 
 Rocks of Anticosti, 298 
 
 Anticosti group in Gaspe", 309 
 
 Medina and Clinton formations, 310 
 
 Their distribution in Canada, 312 
 
 The Niagara formation, 331 
 
 Its distribution in Western Canada,. . 322 
 
 The formation on Lake Temiscamang,. 334 
 
 The Guelph formation, 336 
 
 Its distribution, 337 
 
 CHAPTER XIII. 
 THE ONONDAGA FORMATION AND LOWER HELDERBERG GROUP. 
 
 Upper Silurian series, 345 
 
 Onondaga salt group, 345 
 
 Gypsiferous formation,. . . 347 
 
 Its distribution in Canada, 347 
 
 Formation of gypsum, 352 
 
 Lower Helderberg group, 353 
 
 Water-lime division, 353 
 
 Eurypterus limestones, 353 
 
 Rocks of St. Helen's Island, 356 
 
 Dolomitic conglomerates, 356 
 
 CHAPTER XIV. 
 THE ORISKANY AND CORNIFEROUS FORMATIONS. 
 
 Lower Devonian series, 359 i Its distribution in Western Canada, . . 362 
 
 The Oriskany formation in Canada,.. . 360 j Bituminous beds, 378 
 
 Petroleum springs, 379 
 
 Upper Helderberg group, 362 
 
 Undulations of the formation, 379 
 
 CHAPTER XV. 
 THE HAMILTON FORMATION AND THE PORTAGE AND CHEMUNG GROUP. 
 
 Upper Devonian series, 380 
 
 Hamilton formation in Canada, 382 
 
 Portage and Chenmng group, , 387 
 
 Black shales of Bosanquet, 38fi 
 
 Devonian rocks in Michigan, 388 
 
 Devonian rocks in New York, 389 
 
XX 
 
 TABLE OF CONTENTS-. 
 
 CHAPTER XVI. 
 THE GASPE SERIES, 
 
 Page 
 
 The Gasp limestones, 390 
 
 Upper Silurian age of the limestones,. 391 
 
 The Gaspe' sandstones, 394 
 
 Petroleum springs, 402 
 
 Devonian age of sandstones, 403 
 
 The Bonaventure formation, ,.... 405 
 
 Bocks of Magdalen River, 40*? 
 
 " Chatte and Cascapedia,... 410 
 " " Matanne and Matapedia,... 413 
 " " Great Metis and Patapedia, 416 
 
 " " Rimouski River, 418 
 
 " " Lake Temiscouata, 419 
 
 . " " Walloostook River, 425 
 
 Rocks of the Chaudiere , 42 T 
 
 " " St. Francis, 429 1 
 
 Limestone of Dudswell, 431 
 
 Intrusive granites, 434 
 
 Stoke Mountains, , 435- 
 
 Section along the Bay of Chaleurs,.. . . 437 
 
 Bonaventure formation, 437 
 
 Anticosti group at Port Daniel, 445 
 
 Crystalline rocks of New Carlisle,. . . . 446 
 Cascapedia and Restigouehe Rivers,. . 448 
 
 Rocks of New Brunswick, 451 
 
 Intrusive granites ; their age, 452. 
 
 CHAPTER XVII. 
 
 MINERAL SPECIES. 
 
 Classification, 454 
 
 Calcite, travertine, tufa, 455 
 
 Aragonite, dolomite, 456 
 
 Magnesite, heavy-spar, , 457 
 
 Celestine, gypsum, 459 
 
 Anhydrite, epsom-salt, apatite, 460 
 
 Coprolites, linguist, serpulites, 461 
 
 Fluor-spar, 462 
 
 Olivine, chondrodite, 464 
 
 Lievrite, wollastonite, 465 
 
 Hornblende, raphillite, pyroxene, 466 
 
 Diallage, talc, 469 
 
 Pyrallolite, serpentine, 470 
 
 Chrysotile, aphrodite, 473 
 
 Scapolite, orthoclase, 474 
 
 Perthite, loxoelase, 475 
 
 Albite, peristerite, oligoclase, 477 
 
 Andesine, labradorite, 478 
 
 Bytownite, anorthite, 479 
 
 Opalescent feldspars ; nepheline, 480 
 
 Petalite ; spodumene ; zeolites, 481 
 
 Prehnite, chlorastrolite, 481 
 
 Agalmatolite, gieseckite, wilsonite, . . 482 
 
 Dysyntribite, parophite, 484 
 
 Glauconite ; green-sand, 446 
 
 Chlorite, pyrosclerite, clintonite,. .. .. 488 
 
 Foliated and sparry silicates, 489 
 
 Loganite and related minerals, 490 
 
 Beryl, tourmaline ; axinite, 492 
 
 Micas ; muscovite, fuchsite, 494 
 
 Phlogopite ; pholerite, 495 
 
 Gartiet ; idocrase 496 
 
 Chrome-garnet ; epidote ; 497 
 
 Chloritoid, phyllite ; staurotide, 498 
 
 Andalusite, zircon, 490- 
 
 Spinel, corundum, 499 
 
 Quartz, agate, jasper, 500 
 
 Ilmenite, rutile, 501 
 
 Sphene, lederite, 502 
 
 Wolfram, molybdenite, 503: 
 
 Uranium, coracite, 504 
 
 Chromium ; chromic iron, 504 
 
 Cerium, allanite, 505 
 
 Arsenic; cobalt-bloom; mispickel,.. .. 505 
 
 Nickel and cobalt, 506 
 
 Copper-nickel, domeykite, 506 
 
 Nickel-gymnite, millerite, 506 
 
 Manganese, wad, 507 
 
 Native iron ; carbonate of iron, 508 
 
 Magnetite; hematite, 509 
 
 Limonite, iron ochres, oxalite, 510 
 
 Cubic pyrites, pyrrhotine, , 513 
 
 Zinc-blende, copper-pyrites,. 514 
 
 Native copper ; sulphurets, 515 
 
 Galena ; native silver, 516 
 
 Argentiferous galena, 517 
 
 Mercury ; amalgam, 518 
 
 Gold, platinum, iridosmine, 519 
 
 Bitumens, petroleum, 520 
 
 Asphalt ; altered bitumen, 524 
 
 Origin of bitumens ; marsh-gas, 526 
 
 Bituminous shales, coal, 528 
 
 Plumbago or graphite, 529 
 
 Native sulphur, 530 
 
TABLE OF CONTENTS. 
 
 xxi 
 
 CHAPTER XVIII. 
 WATERS OP SPRINGS AND RIVERS. 
 
 Page 
 
 'Classification of mineral waters, 531 
 
 Ancaster, Assumption, 533 
 
 Baie du Febvre, Bay St. Paul, 534 
 
 Beloeil, Berthier, 534 
 
 Brampton, Brant, Caledonia, 538 
 
 Caxton, Chambly, Charlotte ville, 536 
 
 THtzroy, Gloucester, Hallowell, 537 
 
 Hawkesbury, Hamilton, 537 
 
 Henryville, Jacques Cartier, 530 
 
 Joly, Kingston, Lanoraie, 539 
 
 Niagara, Chippawa, Nicolet, 540 
 
 Plantagenet, Quebec, 541 
 
 Sawdon, Riviere Ouelle, 541 
 
 Page 
 
 Sabrevois, Scarborough, Ste. Anne,.... 542 
 St. Benoit, St. Catherines, St. Eustache, 543 
 
 St. Genevieve, St. Hyacinth, 544 
 
 St. Leon, Ste. Marline, St. Ours, 544 
 
 Tuscarora, 545 
 
 Varennes, 546 
 
 Westmeath, Whitf>y, 547 
 
 Tables of analyses, 547 
 
 C hemistry of mineral springs, 550 
 
 Their geological relations, 561 
 
 Origin of mineral waters, 562 
 
 St. Lawrence and Ottawa Rivers,. . . . 565 
 Analyses of their waters, 566 
 
 CHAPTER XIX. 
 
 SEDIMENTARY AND METAMORPHIC ROCKS, 
 
 Chemistry of sediments, 570 
 
 History of aluminous rocks, 570 
 
 Action of waters and vegetation, 571 
 
 Action of organic matters, 573 
 
 Origin of iroii ores, 573 
 
 Origin of metallic sulphurets, 574 
 
 Dissolved silica and silicious deposits,. 574 
 
 Carbonates of lime and magnesia,. . . . 575 
 
 Origin of gypsum, 576 
 
 Classification of sediments, 576 
 
 Silicates of magnesia and alumina,.... 577 
 
 Minerals of altered rocks, 579 
 
 Conditions of alteration, 579 
 
 Modes of metamorphism, 581 
 
 Agencies in metamorphism, 582 
 
 Metamorphic rocks of Canada, 585 
 
 Rareness of intrusive rocks, 585 
 
 Rocks of Laurentian system, 586 
 
 Rocks of the Huronian series, 594 
 
 Eastern palseozoic rocks, 597 
 
 Western palaeozoic rocks, 618 
 
 Soils and clays, 636 
 
 Analyses of soils, 636 
 
 Table of analyses, 640 
 
 CHAPTER XX. 
 
 ERUPTIVE ROCKS. 
 
 Theory of their origin, 43 
 
 Crystalline silicated rocks, 44 
 
 Their classification, 45 
 
 Indigenous and exotic rocks, 47 
 
 Granite, syenites, and orthoclase, . . .- 47 
 
 Trachytes and pitchstone^, .- 648 
 
 Diorite and diabase, 649 
 
 Hyperite, euphotide, and dolerlte, 650 
 
 Diorite of Yamaska, 663 
 
 Diorites of Mt. Johnson and Beloeil,.. . 664 
 Dolerites; MontarvilleandRougemont, 665 
 Olivene ; peridotite 669 
 
 Greenstones and basalt, 651 
 
 Garnet and epidote rocks, 651 
 
 Dolerites of Grenville, 653 
 
 Syeaite and porphyry of Grenville, .. . 654 
 
 Trachytes of Brome and Shefford, 656 
 
 Trachytes of Chambly and Montreal,.. 667 
 
 Phonolite of Lachine, 661 
 
 Feldspars of trachytes, 662 
 
 Dolerite of Mount Royal ; pyroxenite,. 667 
 
 Ages of these intrusive rocks, 668 
 
 Granites of Canada, 669 
 
 Distribution of intrusive rocks, 669 
 
XX11 
 
 TABLE OF CONTENTS. 
 
 CHAPTER XXI. 
 ECONOMIC GEOLOGY. 
 
 Page 
 
 Classification, 671 
 
 IRON ORBS, 672 
 
 Magnetic ore, 672 
 
 Grenville, Wentworth, Hull, 673 
 
 South Crosby, Bedford, 674 
 
 South Sherbrooke, 674 
 
 Escott, Madoc, Marmora, 675 
 
 Belmont, Seymour, 676 
 
 Sutton, Leeds, 677 
 
 Red hematite ; MacNab, 677 
 
 Bristol, Lake Nipissing, 678 
 
 Specular schist, 678 
 
 St. Armand, Sutton, 679 
 
 Brome ; section of strata, 680 
 
 Inverness, Bastard, Ancaster,. ... 681 
 
 Clay iron-stone ; Gaspe", 682 
 
 Limonite, or bog iron ore, 682 
 
 Lake Erie, Vaudreuil, 683 
 
 Bastard, Stanbridge, 683 
 
 St. Vallier, Green Island, 684 
 
 Cacouna, Saguenay, 684 
 
 St. Maurice ; Champlain, Batiscan, 685 
 
 Industry, Kildare, 685 
 
 Radnor forges, 686 
 
 Iron smelting in Canada, 687 
 
 LEAD ORE; Bedford, 687 
 
 Lansdowne ; Ramsay, 688 
 
 Fitzroy, Gatineau, 689 
 
 Lake Superior ; Mamainse, 690 
 
 Upton, Acton, St. Armand, 690 
 
 Ascot, Potton, Gaspe", 691 
 
 COPPER ORES ; Burgess, Bastard, 692 
 
 Escott, Lanoraie, 693 
 
 Black River, Dore~e River, 694 
 
 Bruce mines, 694 
 
 Wellington mine, Wallace mine,.. 695 
 
 Spanish River, Echo Lake, 696 
 
 Root River. Maskinonge', 697 
 
 Missisagui River, 697 
 
 Lake Superior; south shore, 698 
 
 Cupriferous rocks, amygdaloids,.. 699 
 
 Bachewanung Bay, Mamainse,.... 700 
 
 Section, ancient workings, etc.,.. 7<>1 
 
 Pointe aux Mines, Mica Bay, 702 
 
 Michipicoten Bay and Island,. . . . 703 
 
 Fletcher's mine ; Otter Head, .... 704 
 
 Black River, Terrace Bay, 705 
 
 St. Ignace and Simpson's Islands, 706 
 
 Point Porphyry, Thunder Bay,... 707 
 
 Prince's mine ; Kaministiquia, 708 
 
 P&ge 
 
 Quebec group ; its distribution, 709 
 
 Three principal synclinals, 710 
 
 Copper-bearing strata,. 711 
 
 First synclinal, 712 
 
 Milton, Granby, and Upton, 712 
 
 Acton, Actonvale mine r 713 
 
 Wickham, Durham,.... 718 
 
 Roxton, Wendover r 718 
 
 Somerset, Nelson, St. Flavien r 719 
 
 St. Henry, Point Le>is, Quebec,... 720 
 
 Second synclinal, 721 
 
 Sutton, Shefford, 721 
 
 Stukley, Melbourne, 722 
 
 Cleveland, Chester, 723 
 
 Halifax, Ireland, Inverness, Leeds, 724 
 
 Harvey-Hill mine, 725 
 
 St. Giles, St. Margaret, St. Mary,. 730 
 
 Third synclinal, 731 
 
 Broughton, St. Joseph, Orford,. . . 731 
 
 Ascot, Sherbrooke, 732 
 
 Ham, Garthby, 733 
 
 Gaspe; Barford, 734 
 
 Origin of copper deposits; mining, 735 
 
 Copper smelting, 736 
 
 NICKEL ORES, 737 
 
 Michipicoten Island,Wallace mine, 737 
 
 Quebec group ; Orford, "... 738 
 
 SILVER ORES ; argentiferous galena,. . . 738 
 
 GOLD ; in veins on the Chaudiere,. . . . 739 
 
 Gold in the drift, 739 
 
 Gold-washing at Riviere du Loup, 740 . 
 
 Hydraulic method of washing,. . . 742 
 
 Lake Superior ; Nova Scotia, .... 745 
 
 IRON PYRITES ; its uses, 746 
 
 Sulphuric acid ; copperas, 747 
 
 Elizabethtown, Garthby, 747 
 
 CHROMIC IRON ; its uses and value,. . . . 748 
 
 Ham, Bolton, Melbourne, Gaspd,.. 749 
 
 COBALT ORE ; Elizabethtown, 750 
 
 Escott, D'Aillebout, 751 
 
 MANGANESE ; Bachewanung Bay 751 
 
 Earthy oxyd ; Bolton, Stanstead, 752 
 
 Tring, St. Mary, Cacouna, etc., . . 752 
 
 TITANIUM ; its uses, 753 
 
 Vaudreuil, Bay St. Paul, 754 
 
 MOLYBDENUM, its uses, 754 
 
 Manicougan Bay, Leeds, etc. .... 755 
 
 MAGNESIA, extraction and uses, 756 
 
 Magnesite ; Bolton, Sutton, 756 
 
 Magnesian cement, 75? 
 
TABLE OF CONTENTS. 
 
 XXlll 
 
 Page 
 
 PHOSPHATB OF LIMB, its sources, 757 
 
 Superphosphate of lime, 158 
 
 Mineral phosphate ; its value,. ... 759 
 
 Phosphates as manure, 760 
 
 Ross, Elmsley, Burgess, 761 
 
 GYPSUM ; Grand River, etc., 762 
 
 Magdalen Islands, 763 
 
 FBESH- WATER MARL ; origin and uses, 763 
 
 Various localities, 764 
 
 MINERAL PAINTS, serpentine, 767 
 
 Soapstone, talcose slate, 767 
 
 Iron ochres; Ste. Anne, etc 768 
 
 Pointe du Lac, Vaudreuil, etc.. . . 769 
 
 Sulphate of barytes ; its uses, 770 
 
 Lansdowue, Burgess, Gasps', 771 
 
 Lake Superior, . .. 771 
 
 PEAT ; mode of working ; cost, 772 
 
 Compression of peat, 777 
 
 Value compared with coal, 775 
 
 Peat charcoal, 775 
 
 Distilling peat for oils, 776 
 
 Various processes and results,.. .. 777 
 
 Localities of peat, 780 
 
 BITUMINOUS SHALES ; Collingwood,. . . . 784 
 
 Distilling shale for oils, 784 
 
 Bosanquet, Gaspe, 785 
 
 BITUMENS ; Petroleum, 785, 786 
 
 Enniskillen oil wells, 786 
 
 Amount of oil obtained, 786 
 
 Conditions of its accumulation,.. 787 
 
 Oxford, Mosa, Tilsonburg, 787 
 
 Localities in Gasp6", 788 
 
 Refining petroleum ; naphtha,... 790 
 
 Asphalt for pavements, 790 
 
 FOSSIL RESIN from Gaspe, 791 
 
 Its nature and uses, 792 
 
 PLUMBAGO, its uses and value, 793 
 
 Grenville, Lochaber, Burgess,. . . . 794 
 
 Loughborough, Bedford, 795 
 
 MICA ; its uses and price, 795 
 
 Grenville, Burgess, 796 
 
 SOAPSTONE ; its applications, 796 
 
 Sutton, Bolton, Potton, 797 
 
 Pyrallolite ; Grenville, Ramsay, ... 798 
 
 Potstone; Bolton, Shipton, 799 
 
 SANDSTONE and SAND for furnaces, .... 799 
 
 St. Maurice, Pittsburg, 799 
 
 Moulding-sands, 800 
 
 Fire-brick, 800 
 
 Sandstone for glass-making, 800 
 
 Materials for porcelain, 801 
 
 CLAYS; Brick-clay ; white bricks .... 801 
 
 Fire-clay ; pottery 802 
 
 Page 
 
 LIMESTONES for lime, 803 
 
 Laurentian limestones, 804 
 
 Gale-spar, marl, and tufa for lime,.. 804 
 
 HYDRAULIC CEMENT, or water-lime, 805 
 
 Gasps', Quebec, 805 
 
 Nepean, Kingston, Thorold, 806 
 
 Oneida, Brantford, Point Douglas, 807 
 
 Garnet-rock,. 807 
 
 MILLSTONES ; chert of Grenville, 808 
 
 Gneiss and conglomerates, 808 
 
 Grindstones and whetstones, 809 
 
 BUILDING STONES ; granite, 810 
 
 Stanstead, Barford, etc 810 
 
 Syenite; Grenville, Barrow Island, . 811 
 
 Gneiss; St. Joseph ; Shipton, 811 
 
 Laurentian gneiss, 812 
 
 Trachytes of Brome and Sheflford,.. 812 
 Intrusive diorites and dolerites,. . . . 812 
 
 Sandstones ; Lyn, Beauharnois, 813 
 
 Vaudreuil, Petite Nation, Nepean, 813 
 St. Maurice, Sillery, Pembroke,.. 814 
 The Grey-Band of Canada West,. 814 
 Esquesing, Hamilton, Dundas, etc. 815 
 
 Laurentian limestones, 815 
 
 Silurian limestones, 816 
 
 Kingston, Prescott, Cornwall,.... 816 
 Ottawa, Caughnawaga, Isle Bizard, 817 
 
 Montreal, Lachenaye, 818 
 
 Industry, Chevrotiere, 819 
 
 Pointe aux Trembles, Beauport,.. 819 
 Murray Bay, Saguenay, Mingan,.. 819 
 
 St. Hyacinth, Phillipsburg, 820 
 
 Niagara, Gait, Guelph, 820 
 
 Rockwood, Owen Sound, Brant,.. 821 
 
 St. Marys, Goderich, Maiden, 821 
 
 MARBLES AND SERPENTINES, 822 
 
 Portage du Fort, Beverley, Madoc, 823 
 
 Marmora, Barrie, Arnprior, 823 
 
 Grenville, Wentworth, Burgess,.. 824 
 
 Serpentines ; Melbourne, , 824 
 
 Orford, St. Joseph, Mt. Albert,.. . 825 
 
 Verd antique;polishing serpentines, 825 
 
 Marbles ; St. Joseph, Phillipsburg,.. 826 
 
 Caughnawaga, St. Lin, 826 
 
 St. Dominique, Mingan, 826 
 
 Cornwall, Pakenham, 827 
 
 Montreal, Dudswell, 827 
 
 FLAGGING STONES ; Temiscaming, 828 
 
 Sutton, Memphramagog, Dudswell, 828 
 
 Hemmingford, Rawdon, 829 
 
 Rawdon, St. Cuthbert, 829 
 
 Cap Sant6, Murray Bay, 829 
 
 Grey-Band in Canada West, 830 
 
XXIV 
 
 TABLE OF CONTENTS. 
 
 Page 
 ROOFING SLATES 830 
 
 Melbourne, Walton quarry, 830 
 
 Cleveland, Kingsey, Halifax, 831 
 
 Orford, Brompton, Westbury, etc. 831 
 
 ORNAMENTAL STONES, 831 
 
 Agates, gems, porphyry, 832 
 
 Page 
 
 Peristerite, perthite, 833 
 
 Labrador feldspar, 833 
 
 Epidote-rock, 834 
 
 Jaspers, 834 
 
 LITHOGRAPHIC STONES ; 834 
 
 Marmora, Brant, 835 
 
 CHAPTER XXII. 
 SUPPLEMENTARY. 
 
 LAURENTIAN SERIES, 836 
 
 Distribution of limestones, 83 V 
 
 Anorthosites, 838 
 
 Two formations in the series, 839 
 
 Dolerite dykes, 840 
 
 HURONIAN SERIES, 841 
 
 Its farther distribution, 842 
 
 QUEBEC GROUP, 844 
 
 Phillipsburgh series, 845 
 
 Province-line section, 846 
 
 Stanbridge and Bedford, 848 
 
 Highgate Springs, 855 
 
 Swanton and St. Albans, 856 
 
 Point LSvis limestones, 860 
 
 List of fossils from Point Le>is, 862 
 
 Strait of Belle Isle, 864 
 
 Strata of Newfoundland, 865 
 
 Bonne Bay section, 865 
 
 Table Head section, 869 
 
 Pistolet Bay section, 8*74 
 
 Diorites and serpentines, 875 
 
 General results, 879 
 
 OASPE SERIES, 880 
 
 Farther distribution, 881 
 
 Bonaventure formation, 886 
 
 SUPERFICIAL GEOLOGY, 887 
 
 Classification of deposits, 887 
 
 Rounded rocks and ice grooves,. . . . 888 
 
 Glacial origin of lakes, 889 
 
 List of ice grooves, < 890 
 
 Boulder formation, 893 
 
 Erie and Saugeen clays, 896 
 
 Their distribution, 897 
 
 Clays of Lake Superior, 905 
 
 Algoma sand, 907 
 
 Artemisia gravel, 908 
 
 Ancient beaches and ridges, 910 
 
 Champlain clays of eastern Canada, 915 
 
 Their distribution, 916 
 
 Fossil fishes and plants, 917 
 
 Clays and sands about Montreal,. . . 918 
 
 The Lower St. Lawrence, 921 
 
 Upper sands, St. Maurice, 924 
 
 Shell-beds of Beauport, 925 
 
 List of post-tertiary fossils, 926 
 
 Auriferous drift, 929 
 
 Ancient terraces, 929 
 
 Miocene of Vermont, 930 
 
 Recent deposits, 930 
 
 Infusorial Earth, 930 
 
 APPENDIX. 
 
 TABLE OF BOOK FORMATIONS, 932 
 
 Rocks of Great Britain and Canada, . . 933 
 " " Pennsylvania and Tennessee, 935 
 
 " " Missouri and Iowa, 935 
 
 List of Lower Silurian fossils, 936 
 
 List of Graptolites, 955 
 
 Figures of fossils, 957 
 
 INDEX OF SUBJECTS, 
 INDEX OF PLACES, . . 
 
 969 
 979 
 
LIST OF WOODCUTS. 
 
 CHAP, m. LATTRENTIAN SYSTEM. 
 
 Page 
 
 Contorted gneiss strata, .... 27 
 Gneiss bands in limestone, ... 28 
 
 Figure Page 
 
 3 Supposed organic remains, . . 49 
 
 1 "Vertical section of the same,. 49 
 
 CHAP. V. ROCKS 01- LAKE SUPERIOR. 
 -Wrinkles on a bed of trap, ... 72 I 6 Greenstone dykes, 73 
 
 CHAP. VI. POTSDAM GROTTP. 
 
 -Annelide burrows, 101 
 
 Brachiopoda, 102 
 
 Gasteropoda, 102 
 
 10, 1 1 Cephalopoda, 102 
 
 12-17- 
 
 -Protichnites, 104 
 
 -Climactichnites, 107 
 
 See also 285-299, on pages 283-286. 
 
 CHAP. VH. CALCIFEROLS FORMATION. 
 
 Crinoidea and Brachiopoda, 113 
 
 Laniellibranchiata, 113 
 
 Gasteropoda, 115 
 
 117 
 
 119 
 120 
 
 29-32 Gasteropoda, 
 
 33, 44 
 
 35_40 Cephalopoda, 121 
 
 41-43 Crustacea, 122 
 
 CHAP. VIII. CHAZY FORMATION. 
 
 44-49 Zoophyta and Brachiopoda,. 124 
 
 50, 51 Brachiopoda, 126 
 
 52,53 " 127 
 
 54-56 " 129 
 
 57-60 Brachiopoda, 130 
 
 61 Lamellibranchiata, 131 
 
 62, 63 Gasteropoda, 132 
 
 64-69 Crustacea, 133 
 
 CHAP. IX. TRENTON GROUP. 
 
 a, Birdseye and Black River formation. 
 
 Zoophyta, 
 
 139 
 140 
 
 Brachiopoda, 141 
 
 " 142 
 
 .143 
 
 Lamellibranchiata, 143 
 
 Gasteropoda, 144 
 
 " . 145 
 
 
 ... 147 
 
 
 ... 148 
 
 
 ... 149 
 
 
 ... 150 
 
 
 ... 150 
 
 
 ... 151 
 
 114.115 " 
 
 ... 153 
 
XXVI 
 
 LIST OF WOODCUTS. 
 
 j Trenton formation. 
 
 Figure Page 
 
 116-118 Zoophyta, 156 
 
 119 157 
 
 120-123 Bryozoa, 158 
 
 124-130 Brachiopoda, 159 
 
 131-138 
 
 139-141 " 
 
 142,143 
 
 144-147 " 
 
 148-151 " 
 
 152-154 " 
 
 155, 156 Lamellibranchiata,. . . . . 
 
 157 " 
 
 158,159 " 
 
 161 
 163 
 164 
 165 
 167 
 168 
 170 
 172 
 173 
 
 Figure Page 
 
 160-164 Lamellibranchiata, ........ 175 
 
 165-167 " ........ 176 
 
 168-170 Gasteropoda, .............. 178 
 
 175,176 " ............. 181 
 
 177-1 79 ............. 183 
 
 180, 181 " ............. 184 
 
 182, 183 Crustacea, ............... 184 
 
 184-186 " ............... 184 
 
 187-189 " ............... 188 
 
 190 - " ............... 190 
 
 191 - ............... 190 
 
 192 - Section at C ampement d'O urs, 1 96 
 
 CHAP. X. UTICA AND HUDSON RIVER FORMATIONS. 
 
 193-198 Graptolites, 200 
 
 196, 197 Brachiopoda, 201 
 
 198-200 Crustacea, 202 
 
 201 , " 204 
 
 202-204 Zoophyta, . . 206 
 
 205 " 208 
 
 206-208 Brachiopoda, 209 
 
 209,210 " 
 
 211-213 " 
 
 210 
 211 
 
 214-216 Brachiopoda, 212 
 
 2 1 7 Lamellibranchiata, 213 
 
 218 " 214 
 
 219,220 " 215 
 
 221-224 " 216 
 
 225, 226 Gasteropoda, 217 
 
 227 Cephalopoda, 218 
 
 228 " 218 
 
 229-231 Crustacea, 219 
 
 CHAP. XI. QUEBEC GROUP. 
 
 232-234 Graptolites, 226 
 
 235-238 " -. 228 
 
 239-242 Brachiopoda, 230 
 
 243-247 " 231 
 
 248, 249 Gasteropoda, 232 
 
 250-253 Crustacea, 233 
 
 254- 
 255- 
 256-260 
 
 -Section near Quebec, 234 
 
 -Crustacea, 235 
 
 "236 
 
 261-267 Crustacea, 237 
 
 268-273 " ; 238 
 
 274-277 " 239 
 
 278 Brachiopoda (Chazy) 274 
 
 279 Crustacea, ( " ) 274 
 
 280, 281 Gasteropoda, 276 
 
 282- 
 283- 
 284- 
 
 276 
 
 Cephalopoda, 277 
 
 Crustacea, 278 
 
 Potsdam group. 
 
 285, 286 Zoophyta, 283 
 
 287-291 Brachiopoda, 284 
 
 292 Annelidae, 285 
 
 293-297 Crustacea, 
 298, 299 " 
 
 300- 
 
 -Ideal section of strata,, 
 
 286 
 296 
 
 CHAP. XII. ANTICOSTI GROUP. 
 
 301-303 Zoopbyta, 305 
 
 304-309 
 310,311 
 
 306 
 308 
 
 312, 313 Tunicata, 309 
 
 314-317 Brachiopoda, 311 
 
 318-320 
 
 312 
 
 321-325 Brachiopoda, . . . . t 315 
 
 326,327 " 
 
 328-334 " 
 
 335-337 " 
 
 338, 339 Crustacea, 319 
 
 " . 320 
 
 316 
 31* 
 318 
 
LIST OF WOODCUTS. 
 Guelph formation. 
 
 XXV11 
 
 Figure Page 
 
 341 Brachiopoda, 337 
 
 342 Lamellibmnchiata, 338 
 
 343-346 Gasteropoda, 339 
 
 Figure Page 
 
 347 Gasteropoda, 341 
 
 348-351 " 343 
 
 352 .344 
 
 CHAP. XIV. CORNIB-EROUS FORMATION. 
 353-355 Zoophyta, 362 386-389 Brachiopoda, 370 
 
 358 359 " 
 
 . . . 364 
 
 391 394 " 
 
 . ... 372 
 
 360-363 " 
 
 365 
 
 395-399 " 
 
 . ... 373 
 
 364-372 " 
 
 366 
 
 400-405 " 
 
 .. 374 
 
 373377 Brachiopoda . 
 
 367 
 
 
 . ... 375 
 
 378-381 " 
 
 368 
 
 
 . ... 376 
 
 382-385 " 
 
 369 
 
 40D " 
 
 376 
 
 
 
 
 
 CHAP. XV. HAMILTON FORMATION. 
 
 410-414 Zoophyta, 383 
 
 415-418 Brachiopoda, 384 
 
 4 1 9-42 1 Brachiopoda, 385 
 
 422-424- " 386 
 
 425- 
 
 426- 
 427- 
 428- 
 
 433- 
 
 CHAP. XVI. GASPE SERIES. 
 
 -Contorted limestone beds, . . 392 i 429 Plantae, 400 
 
 -Plantae, 397 ' 429 (bis), 430, 401 
 
 398 
 
 389 432 
 
 431- 
 
 -Contorted slates, 425 
 
 -Granite dykes in limestone,. 434 
 
 CHAP. XIX. SEDIMENTARY BOCKS. 
 
 -Hopper-shaped mould, 625 
 
 434, 435 Crystallites, 632 
 
 436 Crystallites, 633 
 
 437, 438 Sections of the same, 633 
 
 439- 
 
 CHAP. XXI ECONOMIC GEOLOGY. 
 Plan of Harvey-Hill mine,. . 726 I 440, 441 Sections of Harvey-Hill mine, 727 
 
 CHAP. XXII. STTPPLEMEBTARY. 
 
 ction on the Province Line, 847 
 
 in St. Armand, 852 
 
 at Highgate Springs, 855 
 
 445 Section at Smith's lime-works,855 
 
 446 near Swanton, 857 
 
 447 " near Owen Sound,.. 898 
 
 APPENDIX. 
 
 448-457 Fossils of L. Helderberg gr., 957 
 
 458-463 " " " " 958 
 
 464 " Water limestone, " 959 
 
 465-467 
 
 468-470 " 
 
 471, 472 " 
 
 Oriskany formation, 960 
 
 961 
 962 
 
 473-479 Fossils of post-tertiary, 
 480-492 " " 
 
 493,494 " " " 
 
 495,496 " " " 
 
 497,498 " " " 
 
 963 
 964 
 965 
 966 
 967 
 
REPORT 
 
 GEOLOGY OF CANADA 
 
 CHAPTER I. 
 
 INTRODUCTION. 
 
 GEOGRAPHICAL DESCRIPTION. ST. LAWRENCE BASIN. LAURENTIDE AND NOTRE DAME MOUN- 
 TAINS ; THEIR LAKES AND KIVEE8. RAPIDS AND CANALS OF THE ST. LAWRENCE. LOWER 
 
 SILURIAN REGION OF WESTERN CANADA. MIDDLE AND UPPER SILURIAN REGION. 
 SURFACE OF THE WESTERN PENINSULA; ITS WATER-SHED AND RIVERS. PENINSULA OF 
 MICHIGAN. THE GREAT LAKES. AMERICAN COAL FIELDS. MISSISSIPPI AND BED RIVER 
 VALLEYS. ROCKT MOUNTAINS. 
 
 The hydrographical basin of the St. Lawrence and its estuary as far as Basih of the 
 the lower end of the island of Anticosti, comprises an area of about 530,000 stp Lawrence - 
 square miles. In form it presents an irregular parallelogram, running 
 nearly S. W. for about 900 miles, with a pretty uniform breadth of 250 
 miles ; the southern side, in its farther progress, sweeping round in a rude 
 semicircle, the diameter of which extends about 900 miles to the N. W. The 
 great lakes into which the river expands, with its estuary, have an area of 
 about 130,000 square miles ; leaving for the land drained by the river a 
 superficies of 400,000 square miles. More than eight tenths of this, or about 
 830,000 square miles, belong to Canada, while the remainder constitutes a 
 part of the United States. With the exception of about 50,000 square 
 miles (including the whole of the Gaspe* peninsula) in the eastern part of 
 the province, the Canadian portion lies wholly on the north side 'of the 
 river, while the only part of the United States which does so is situated 
 at the west end of Lake Superior. 
 
 A range of mountainous country rises on each side of the estuary of the Mountain 
 St. Lawrence, the Laurentides on the north, and the mountains of Notre Eanges - 
 Dame on the south. The opposing flanks of these ranges keep close on the 
 margin of the water for a considerable distance up the river. That of the 
 southern range begins to leave the margin in the neighborhood of Kam- 
 cruraska, nearly a hundred miles below Quebec, where the river is fifteen 
 miles wide. Opposite to Quebec the range is thirty miles distant from the 
 
2 GEOLOGY OF CANADA. [CHAP. I. 
 
 river, and opposite to Montreal about fifty miles, where it enters the State 
 Notre Dame of Vermont to form the eastern limit of the valley of Lake Champlain. 
 From the province line south-westward, the range is known as the Green 
 Mountains and the Alleghanies, and constitutes the Appalachian chain. 
 The flank of the northern range diverges from the St. Lawrence at Cape 
 Tourmente, about twenty miles below Quebec, and at Montreal is distant 
 from the river about thirty miles. Beyond this it extends up the Ottawa 
 on the north side, for about a hundred miles, and sweeps round thence to 
 the Thousand Islands, near Kingston ; from which it gains the southern 
 extremity of Georgian Bay, and continues along the eastern and northern 
 shores of Lake Huron and Lake Superior. It then turns up to the north- 
 westward, and ultimately reaches the Arctic Ocean ; the distance of the 
 whole course of the range from Labrador being about 3500 miles. 
 
 The southern range separates the tributaries of the river St. Lawrence 
 from those of the Gulf, as well as from those of the bay of Fundy and the 
 Laurentides. Atlantic, as far as Canada is concerned ; but is broken through by the Hudson, 
 the Delaware, the Susquehanna, and other Atlantic rivers farther westward. 
 The northern range gives the water-shed separating the tributaries of the 
 St. Lawrence from those of Hudson's Bay ; but beyond the basin of the St. 
 Lawrence it is traversed by two of the affluents of- this bay, the Saskatch- 
 ewan and the Churchill, the former taking its source in the Rocky Moun- 
 tains ; while still farther on, the range again becomes the limit of the Hudson's 
 Bay rivers, dividing their sources and those of the Back and other streams, 
 for 800 miles, from the tributaries of the Mackenzie. 
 
 Judging from the facts obtained in Canada, each of these ranges is 
 composed of sedimentary rocks in an altered condition ; those of the north 
 presenting the more crystalline character. The rocks of the northern 
 range are also the more ancient, being of the azoic era ; while those of the 
 southern are palaeozoic, though the fossils in a large portion of them 
 appear to have been obliterated through molecular movements. 
 
 structure of rpk e strata of both ranges are very much corrugated. In the southern 
 Mountains, mountains the axes of the folds run parallel with the range, and the hills 
 and valleys for the most part coincide with these bearings. Some of the 
 axes have been traced considerable distances, and though parallel with one 
 another they do not appear to maintain straight lines, but assume, as they 
 proceed, great sinuous sweeps. Following them from the extremity of 
 Gasp, they strike into the land with a north-west bearing, which gradually 
 rounds to west in the vicinity of Ste. Anne des Monts and the Chatte. 
 Farther on, they by degrees assume a nearly south-west course, and again 
 turn more west for a short distance, after passing the ChaudiSre ; but once 
 more bending to south-west, their course becomes nearly south as they quit 
 the province amid the Green Mountains, beyond which their course has been 
 described by Professor Rogers as being marked by sinuosities of a similar 
 
CHAP. I.] GEOGRAPHICAL DESCRIPTION. 3 
 
 character as far as Alabama. In one part or other of the range, rocks of Age of rocks 
 all the divisions of the palaeozoic period, from the Lower Silurian to the ^ ese 
 Carboniferous, appear to be involved in the folds, and though in some places 
 there is a want of conformity between the Lower and the Upper Silurian, 
 and between the Devonian and the Carboniferous, there is no want of paral- 
 lelism in the axes of the folds throughout the whole ; showing that the 
 forces which produced them continued in operation in the same directions 
 during nearly the whole of the palaeozoic period. 
 
 In the Canadian part of the range, it is the inferior deposits of this period 
 that present the highest peaks. To these deposits appear to belong the 
 Shickshock Mountains, which, in ascending the St. Lawrence towards 
 Quebec, are the highest that are displayed to view on the south side. 
 The whole of the Gaspe* peninsula may be considered a block of table-land 
 of about 1500 feet in height, in which the river-courses are deep and nar- 
 row excavations. Upon this the Shickshock Mountains are a conspicuous 
 range of highlands, extending about sixty-five miles from the east side of 
 the Ste. Anne des Monts to the Matanne. They stand on a breadth of from 
 two to six miles, at a distance of about twelve miles from the St. Lawrence, 
 and rise into points, attaining heights of between 3000 and 4000 feet. Heights of 
 But though the highest land, they do not form any part of the water- M 
 shed of the peninsula ; for the Ste. Anne des Monts, the Chatte and the 
 Matanne, taking their sources on lower land to the south, cut gorges through 
 them so deep that their channels, where they cross the range, are not more 
 than between 500 and 600 feet above the St. Lawrence. The waters of 
 one branch of the Matanne have their source on lower land on the north 
 side of the range, and flow south through a profound gap to join the main 
 stream, thus crossing the range twice in their course to the great river. 
 
 In the same part of the geological series are St. Ronan's Mountain in 
 Buckland, and White Mountain in Coleraine, each about twenty-five miles 
 from the Chaudidre on opposite sides, and about forty miles from its mouth, 
 as well as Ham and Orford or Victoria Mountains, some twenty or twenty- 
 five miles from opposite sides of the St. Francis, with Owl's Head and Sutton 
 Mountains, the whole being the highest series of summits along the range 
 to the province line, some of them supposed to equal in elevation the peaks 
 of Gaspe*. As in the case of the smaller streams cutting the Shickshock 
 Mountains, the Chaudiere and the St. Francis, which are two of the largest 
 tributaries on the south side of the St. Lawrence, traverse this portion of 
 the range ; gathering the chief part of their waters from lands to the south, 
 through valleys running with the strike. 
 
 Except near the water-shed, the valleys of the principal streams do not Lakes 
 attain a greater elevation than from 500 to 900 feet above the St. Law- 
 rence. They present but few abrupt cascades, and though no less than 
 sixteen ponds and larger sheets of water are included in the panorama 
 
 Dame Moun- 
 tains. 
 
4 GEOLOGY OF CANADA. [CHAP. I. 
 
 Their heights fr m the top of Orford Mountain, it cannot be said that on the whole the 
 and areas. Canadian part of the southern range abounds in lakes. The greatest of 
 these, with their areas and approximate heights above the sea, are : 
 
 HEIGHT. AREA. 
 
 Feet. Square Miles. 
 
 Memphramagog 756 37 
 
 Aylmer 795 9 
 
 St. Francia 890 12 
 
 Megantic ? 17 
 
 Temiscouata 467 24 
 
 Matapedia 480 12 
 
 The hills, exclusive of the summits of the highest ridge, seldom exceed 
 from 1000 to 1500 feet, and the country connected with the Canadian 
 part of the range, presenting a rolling rather than a rugged mountainous 
 surface, is for the most part, particularly in what is called the Eastern 
 Townships, capable of tillage or pasturage, and will in general be found 
 to constitute a useful agricultural area. 
 
 structure of While the corrugations of the Laurentides appear to be more complicated 
 ldes ' than those of the southern range, they have not yet received the same 
 amount of investigation. It would be hazardous therefore to express any 
 very confident opinion in regard to their general bearings. The northern 
 range, belonging, as has already been stated, to the azoic period, is 
 composed in Canada of two series of rocks, which have been termed 
 the Huronian and the Laurentian, the former overlying the latter. The 
 Huronian strata are met with on the north shore of Lake Huron and the 
 east and north shores of Lake Superior, and the axes of the folds which 
 these strata present appear to trend north-west on the former lake and 
 gradually turn round to south-west on the latter. The Laurentian folds 
 which have been investigated appear to hold courses wholly independent 
 of these, the chief part of them being north or a few degrees removed from 
 it. The plications appear to be sharp and numerous ; and as the bearing 
 of their axes would be transverse to the general bearing of the range, 
 while supposed equivalent rock-masses belonging to it are nevertheless found 
 towards both extremes of the province, as well as in intermediate parts, 
 it seems probable that the outcrops of the strata will exhibit a very deeply 
 serrated or zigzag arrangement in their geographical distribution, and that 
 the bearings of the mountains and valleys will conform to them. 
 
 The largest rivers issuing from the Laurentides in Canada are the 
 Ottawa and the Saguenay, the former between 500 and 600 miles, and the 
 latter between 300 and 400 miles in length. They take their sources 
 very nearly together, upwards of 200 miles north-west of the St. Lawrence, 
 and, after running for some distance parallel with it in opposite directions, 
 turn and flow nearly parallel with one another to join it ; their distance 
 
CHAP. I.] GEOGRAPHICAL DESCRIPTION. 5 
 
 apart being about 300 miles. Almost all the streams in the intermediate Elvers of the 
 
 country the Gatineau, the LiSvre, and the St. Maurice being the largest Lan ti d es- 
 
 three run very nearly from north to south, and it is upon some of those 
 
 which are tributary to the Ottawa that the axes of the folds have been 
 
 found to coincide with the rivers ; while the Ottawa itself, skirting the Lau- 
 
 rentides for a considerable distance in the lower part of its course, cuts the 
 
 folds transversely. From the upper end of Lake St. John to Chicoutimi, 
 
 sixty miles in a bearing south of east, the Saguenay appears to run with 
 
 the strata ; but from Chicoutimi to the mouth, seventy miles more in the 
 
 same bearing, it appears to cut them transversely. For some distance 
 
 below the Saguenay the streams flow nearly parallel with it, becoming 
 
 however more north and south approaching the Gulf. The largest of 
 
 these rivers appear to be the Betsiamite, the Outarde or Bustard, the 
 
 Manicouagan, and the Moisie ; but what relation their courses bear to the 
 
 strike of the strata has not been ascertained. 
 
 Between Lake St. John and Murray Bay the main ridge of that part Heights of the 
 which is cut transversely by the Saguenay is stated to attain 4000 feet Laurentides - 
 above the sea, while peaks in parallel ridges nearer the St. Lawrence may 
 exceed half that height. Bayfield gives 2547 feet to Mont Eboulemens, 
 between Murray Bay and Bay St. Paul ; and farther up the St. Lawrence, 
 ' among the summits that lend such majesty to -the view from Quebec, he 
 states Cape Tourmente to be 1919 feet, and Mount Ste. Anne 2687 feet. 
 In the country north of the Ottawa the most elevated summits seen by 
 the officers of the Survey are those of the Trembling Mountain in 
 Argenteuil. One of its peaks is estimated to be 2060 feet, while few 
 hills in the next gradation of heights in the same neighborhood exceed 
 1000 or 1200 feet. In the country between the Ottawa and Lake Huron 
 the highest summits do not appear to exceed 1500 or 1700 feet, though 
 one near the sources of the Muskoka and the Petewahweh probably attains 
 2300 feet : those on the northern tributaries of Lake Nipissing and the 
 French River are from 1400 to 1600 feet. To the Lacloche Mountains 
 on the north side of Lake Huron, belonging to the upper division of the 
 azoic rocks, 1000 feet have been given, and to hills farther north in 
 this part something less, while some of the summits of the same deposits 
 on Lake Superior attain 2000 feet. 
 
 As the various heights mentioned belong to points more prominent 
 than the country surrounding them, it may not be giving too low an estimate 
 of the general elevation of the Laurentide range in Canada to call it from 
 1500 to 1600 feet. The surface which the range presents is of a mammil- 
 lated character, its hills being worn by glacial action into round-backed 
 forms, in general thickly clothed with wood, the prevailing trees on the 
 summits being evergreens, in some parts chiefly pine, and in others 
 spruce, while hardwood sometimes abounds on the lower elevations and in 
 
6 GEOLOGY OF CANADA. [CHAP. I. 
 
 Lakes of the the valleys. The valleys are in general not very wide, and many are worn 
 Laurentides. . - ponds and lakes : some streams indeed are nothing 
 
 more from their sources to their mouths than a chain of such quiet expan- 
 sions united by short discharging channels. The prodigious number of 
 these sheets of water, great and small, bespangling the whole area, is 
 one of its most remarkable features, and when looked upon as displayed 
 on a map, they appear so scattered at random over the surface as to contra- 
 dict almost any supposed law of distribution. Some of the clusters 
 however that have been examined in connection with their geology are 
 most beautifully explained by the peculiar geographical distribution of the 
 strata, which results from their very corrugated condition, combined with 
 the unequal wear occasioned by the hardness and toughness of some parts, 
 and the softness of others, in the sequence of the metamorphosed deposits. 
 In the Laurentide district a straight line can scarcely be followed in any 
 direction for a great distance without the occurrence of one of these 
 expansions ; and it frequently happens that it will present a considerable 
 area even where discharging by a very slender outlet. The profusion in 
 which the lakes exist, with in some instances only a short interval of land 
 between them, though they may belong to different river-systems, affords, 
 with the aid of birch-bark canoes, a ready means of passing from one 
 navigable stream to another, in whatever part an explorer may be ; and 
 thus, if he is well acquainted with the country, he can reach almost any 
 position he may wish to attain without any very great deviation from a 
 direct route. Although a large number of the rivers of the Canadian 
 portion of the Laurentides is still unknown, or only partially explored, 
 upwards of a thousand of these lakes are represented on the published 
 Their heights maps of the country. It is only a few of them however that are sufficiently 
 and areas. l ar g e to deserve especial mention. The following six are the best known, 
 with their areas and their elevations above the sea : 
 
 HEIGHT. AREA. 
 
 Feet. Square Miles. 
 
 St. John ......................... 300 ? 360 
 
 Grand Lac ....................... 700 ? 660 
 
 Temiscamang ..................... 612 126 
 
 Keepawa ........................ 760 92 
 
 Temagamang .................... 800 ? 330 
 
 Nipissing ......................... 639 294 
 
 plain between From the opposing flanks of the two mountain ranges which have been 
 Laurentide & ^ escr i|)ed, there extends a vast intermediate plain, the limit of which 
 
 Appalachian . ' 
 
 Mountains, westward is the Rocky Mountains. In addition to six or seven isolated 
 trap mountains in Eastern Canada, varying in height from 500 to 1800 
 feet, (all visible from the hill near Montreal, which is one of them,) and the 
 Adirondack Mountains, a nearly isolated mass of Laurentian rocks rising in 
 
CHAP. I.J GEOGRAPHICAL DESCRIPTION. 7 
 
 New York to the height of 5000 feet between Lake Champlain and Lake Niagara FI 
 Ontario, there are few sudden inequalities to break the smoothness of the 
 general surface of the plain, with the exception of abrupt descents through 
 the drift to river courses, and an escarpment forming that step in the country 
 which produces the world-renowned cataract of Niagara. The summit of 
 that escarpment is of the Middle Silurian period, and tracing it from west 
 to east, it is known to form the two horns separating Green Bay from Lake 
 Michigan ; thence running along the south front of the northern peninsula 
 of the state which takes its name from that lake, and the south half of the 
 Manitoulin range of islands, it reaches Cabot's Head, and composes the 
 chief feature of the promontory separating Georgian Bay from the main 
 body of Lake Huron. From this it constitutes the summits of the Blue 
 Mountains, and, rounding the western extremity of Lake Ontario, it forms 
 St. Catherine Ridge and Queenston Heights. It thence follows at a short 
 distance the south side of Lake Ontario and of the valley of the Mohawk, 
 and sweeps round into the valley of the Hudson. By the addition of terrace 
 above terrace of Upper Silurian and Devonian age, the step farther on 
 rises info the Catskill mountains ; beyond which it becomes entangled 
 in the folds of the Appalachian chain and is lost. 
 
 In so far as relates to Canada, nothing can better shew the character of 
 this plain than a comparison between the surface of the land and the levels 
 of the great fresh-water seas that spread out on it. The following are the 
 areas of these lakes and their heights above tide-water : 
 
 
 HEIGHT. 
 
 Feet. 
 232 
 
 AREA. 
 
 Square Miles. 
 7330 
 
 Erie 
 
 565 
 
 10030 
 
 
 578 
 
 23780 
 
 
 578 
 
 25590 
 
 
 600 
 
 31420 
 
 The distance from Quebec to the western extremity of Lake Superior is Great we 
 about 1200 miles, so that the average ascent of the valley of the St. Law- ei 
 rence does not exceed six inches in a mile. But if we take the ascent of 
 the lower plain to the foot of the Niagara escarpment, and that of the upper 
 one from the edge of it, we have about six inches in the mile for the former 
 and only about three quarters of an inch in the mile for the latter ; the 
 difference of level between Lakes Erie and Superior being only thirty-five 
 feet. The land on the banks of the St. Lawrence and its lakes, either 
 immediately near the margin or at no very great distance removed from it, 
 rises in general to the height of from fifty to one hundred and fifty feet ; 
 and although, as has been said, no sudden important inequalities present 
 themselves on its surface with the exceptions mentioned, there are occasion- 
 ally gentle swells of ground, which, when extending over considerable areas, 
 
8 GEOLOGY OP CANADA. [CHAP. L 
 
 st. Lawrence attain greater heights than would be suspected without careful admeasure- 
 ments. There are few of these between Quebec and Montreal, and it is 
 not probable that in this part of the plain any point on either side of the 
 river rises beyond 300 feet above the sea. Above Lake St. Peter, a 
 considerable tract of country on the south-east side of the river, with a 
 very fruitful soil, is lower than the land on the opposite side. It is occi*- 
 pied by the valleys of the Richelieu and the Yamaska, two parallel streams, 
 not far distant from one another, which run in the strike of the formations, 
 on two low anticlinal forms with a third between, all belonging to the 
 Appalachian system of folds. The Richelieu is the outlet of Lake Cham- 
 plain ; the surface of which, with an area of 450 miles, is eighty-eight feet 
 above the sea. The Hudson River flowing in the same valley as Lake 
 Champlain, but in an opposite direction, approaches to within twenty miles 
 of the lake, with a height of land between them of one hundred and twenty 
 feet above the sea ; so that were the continent depressed a little over that 
 amount, there would be a continuous salt-water communication between the 
 Gulf of St. Lawrence and the Atlantic by this channel, and the states of 
 New England, with Nova Scotia, New Brunswick, and nearly all that part 
 of Canada on the south-east side of the St. Lawrence, would be converted 
 into an island. 
 
 plateau be- A triangular portion of the plain, still largely covered by forest, lies be- 
 Lawren* 116 mi ^ ween *k e Ottawa and the St. Lawrence, and abuts against the Laurentian 
 the Ottawa, range where this sweeps round from the Lac des Chats to the Thousand 
 Islands. In the whole of this triangle, comprising about 10,000 square 
 miles, it may be said that there is only one exception to its general horizon- 
 tality. This is found in the mountain of Rigaud, one of the trappean bills 
 which have been already alluded to. Its summit is 538 feet above the 
 RiviSre a la Graisse at its foot, where this stream joins the Lake of Two 
 Mountains, or 600 feet above the sea, while the land for nine miles 
 southward from the summit maintains an elevation which overlooks the 
 comparatively level tract beyond, up and across the St. Lawrence ; one 
 point of view in Lochiel, commanding the country around it for a consider- 
 able distance, being about 280 feet above the sea. To illustrate the near 
 approach of the district to horizontally, it may be stated that the South 
 Petite Nation, which drains a large part of it, takes its source in the 
 townships of Edwardsburgh and Matilda, within a mile and a half of the 
 St. Lawrence, in a water-shed which is only thirty feet above the surface 
 of the great river, or 252 feet above the sea, and falls but 144 feet in a 
 hundred miles before reaching the Ottawa in Plantagenet ; while on the 
 Ottawa and Prescott railroad, which crosses the Petite Nation in Edwards- 
 burgh, the two highest levels are 362 feet ten miles from the Ottawa, in 
 West Gloucester, and 358 feet about ten miles from the St. Lawrence, in 
 Edwardsburgh. The Rideau, discharging at Ottawa, is another stream 
 
CHAP. L] GEOGRAPHICAL DESCRIPTION. 9 
 
 which drains a considerable part of the triangle. Where this issues from 
 amidst the Laurentian hills at Rideau Lake its surface is about 400 feet above 
 the sea, and between the valley of this stream and the Lac des Chats the 
 highest levels belonging to the plain range from 330 to 410 feet above the 
 same base. 
 
 This triangular plateau is of a good agricultural character where it is 
 cleared, and has produced much heavy pine timber from its forests. It is 
 underlaid by rocks of the Lower Silurian age, reaching nearly to the 
 summit of the group. They lie in the form of a trough, the breadth of 
 which reaches across the St. Lawrence into the State of New York, where 
 the inferior members of the group occupy a margin of from fifteen to twenty- 
 five miles, and rest upon the azoic strata of the Adirondack Mountains. 
 To the south of the eastern apex of the triangle, at the junction of the Ottawa 
 and the St. Lawrence, these strata turn sharply round to the valley of Lake 
 Champlain, making an elbow which corresponds with a more obtuse form 
 of the same character north of the Ottawa, opposite the upper end of the 
 island of Montreal. The two pointing to one another indicate the existence 
 of a low transverse anticlinal arch, which nearly isolates the Silurian 
 triangle by leaving but the lowest Silurian formation to conceal the azoic 
 strata, and that only partially, since a dome of azoic rock protrudes through 
 the Silurian in Mont Calvaire, situated on the left bank of the Ottawa, in 
 the intermediate space. A longitudinal fold of some importance in the undulations 
 triangular trough divides it into two synclinal forms, of which the northern 
 one is the deeper ; the deepest part being near the north-west corner of 
 Russell, about fifteen miles from Ottawa City. The effect of this fold is 
 traceable all the way from the Lac des Chats to the trap mountain of 
 Ragaud, and it is probably connected with those of Montreal, Montar- 
 ville, Rouville, Rougemont, Yamaska and Shefford, all of which, being the 
 chief part of the trappean masses already alluded to, stand pretty nearly in 
 a straight line, shewing the disturbance to extend 180 miles across from 
 the Laurentian to the Appalachian range. 
 
 The Lac des Chats and Lake Ontario are very nearly on a common 
 level, and the channels of the Ottawa and the St. Lawrence descending 
 from them are worn out of equivalent strata on opposite sides of the 
 triangular trough. The former river leaves the Chats by a single 
 leap of fifty feet over Laurentian strata, and makes a plunge of upwards 
 of sixty feet more at Ottawa City in the ChaudiSre falls ; which, though they 
 break the navigation of the river, give inexhaustible water-power for 
 manufacturing purposes, and, with the aid of the horizontal limestone strata 
 piled up into crags and abrupt eminences over the river, combined with 
 the Laurentide mountains some few miles to the north, invest the scenery 
 of the neighborhood with much picturesque beauty. From the foot of the 
 Chaudidre falls, where the river is 118 feet above the sea, it is of easy 
 
10 GEOLOGY OF CANADA. [CHAP. I. 
 
 Rapids and navigation for steamboats for nearly sixty miles, to Grenville, between which 
 ottavra ftie an( ^ its junction with the St. Lawrence two interruptions from rapids occur. 
 These are obviated between Grenville and Carillon, where the difference 
 of level is forty-seven feet, by a canal capable of navigation by barges and 
 propellers of eighty tons, and at Ste. Anne by a lock enabling steamers of 
 300 tons to overcome a fall of three feet between the Lake of Two Moun- 
 tains and Lake St. Louis. 
 
 Lake St. Louis is fifty-seven feet above the sea. The descent to it from 
 Lake Ontario is therefore 175 feet, and to the head of sea navigation 
 in the harbor of Montreal there is an additional descent of forty-five feet 
 in the Lachine Rapids. The whole distance from Lake Ontario is between 
 140 and 150 miles, so that the inclination would be about eighteen inches 
 in a mile. In this there are no vertical falls, but several interruptions 
 of the st. from violent rapids. These do not impede the downward navigation of 
 lce ' vessels drawing nine feet ; but to enable such vessels to ascend the river, a 
 magnificent system of canals has been built by the provincial government. 
 These canals are nine in number, and their total length forty-two miles. 
 The number of locks is twenty-seven, obviating 205 feet of the fall, and per- 
 mitting the passage of vessels of 800 tons burden. 
 
 Adirondack This part of the St. Lawrence, it would appear, does not exhibit so 
 ^ousanT continuously deep an excavation in the rocks of the country as the Ottawa 
 islands. below the Chats. As in the case of the Lac des Chats, an exposure of 
 azoic rocks crosses the St. Lawrence at the outlet of Lake Ontario. It 
 unites the azoic mass of the Adirondack mountains with the main body of 
 the Laurentian range, and gives origin to the much-admired scenery of the 
 Thousand Islands. The exposure appears to be a part of an ancient 
 ridge in the bottom of the Lower Silurian sea, by the sediments from which 
 this low ridge was gradually covered up. . Again denuded at a compara- 
 tively recent period, the resistance which the hard gneiss composing it 
 has offered to the erosive forces excavating the valley has rendered it a 
 barrier to keep up the waters of the lake, and to produce between it and 
 Montreal the steepest part of the river in the lower plain. The width of 
 the denuded ridge at the narrowest part does not apparently exceed five 
 miles. 
 
 From the point where the azoic ridge is thus traversed by the St* 
 Lawrence, the junction of the azoic and palaeozoic rocks on the lower side 
 runs north of east down the river on the one hand, and west of north across 
 to the Ottawa on the other. On the upper side it runs north of west to 
 Georgian Bay in Lake Huron, and east of south along the valley of the 
 Black River to the valley of the Mohawk. The whole azoic mass in 
 immediate relation with the Adirondack mountains has an area of about 
 10,000 square miles. Its most southern part in the valley of the Mohawk 
 is near Johnston, where it approaches to within twenty miles of the Middle 
 
CHAP. I.] GEOGRAPHICAL DESCRIPTION. H 
 
 Silurian escarpment. This escarpment in a gently sinuous line runs very Lower suunan 
 nearly due west to Hamilton, whence it proceeds west of north to Owen 
 Sound in Georgian Bay. It will be observed from the bearings given, 
 that the Lower Silurian plain on the upper side of the Thousand Islands 
 presents the form of a rude east and west parallelogram, with the addition 
 of a truncated triangle based on the east end and applied to a prolongation 
 of the south side. The area of this figure comprises about 23,000 square 
 miles ; of which Lake Ontario, with an extreme length of 200 miles and an 
 extreme breadth of fifty miles, occupies about one third. 
 
 The terrestrial portion appertaining to Canada, exclusive of a small strip 
 bordering the south side of the lake between Hamilton and Queenston, 
 presents the form of a triangle, whose base is the escarpment between 
 Hamilton and Owen Sound, and whose apex is at the outlet of the lake 
 among the Thousand Islands. The area comprises about 16,000 square 
 miles. The chief streams by which it is drained are the Salmon, the 
 Moira, the Ottonnabee or Trent, the Humber, and the Credit, which are 
 tributary to Lake Ontario, and the Severn and the Nottawasaga, tributary 
 to Lake Huron. The first two streams, which are not of great importance, its rivers, 
 have their sources a considerable distance among the Laurentian rocks : 
 the Ottonnabee, as it is called in its upper, and the Trent in its lower part, 
 is the principal river of the area. Its valley is wide and its course very 
 crooked. Following the main stream, its whole length is about 170 miles, 
 while a straight line from its source to its mouth is only about ninety miles. 
 The difference arises from six sharp turns, in the stretches between which 
 the stream flows alternately westward of south and northward of east before 
 it is discharged into the bay of Quinte* ; in which bay the same alternate 
 courses, always giving angles less than ninety degrees, are repeated three 
 times to the open lake. The main stream and its northern tributaries for 
 sixty-five miles of longitude have their sources in the Laurentian range, 
 while the southern tributaries rise in a ridge of drift removed but from 
 seven to fifteen miles from Lake Ontario. The main stream flows among me lakes, their 
 the Laurentian hills for about thirty miles, and leaves them just before sources - 
 entering Balsam Lake ; though it still continues to skirt the range at a 
 variable distance, through a succession of lakes, for upwards of forty miles 
 to Salmon Trout Lake. Here making the second of the acute turns 
 mentioned, it arrives by a stretch of thirty miles to within ten miles of Lake 
 Ontario in Rice Lake, and by another stretch of about the same distance 
 returns to within five miles of the Laurentian range at Henley's Falls, 
 above the junction of Crow River. In the lakes skirting this range the fall 
 is about eighteen inches in a mile, but about four tunes as much to Rice 
 Lake. The following are the heights of the lakes above the sea: 
 
 Balsam Lake 820 feet. 
 
 Cameron Lake .. .... 815 " 
 
12 GEOLOGY OF CANADA. [CHAP. I. 
 
 Sturgeon Lake 793 feet. 
 
 Pigeon, Buckhorn, and Chemung Lakes 788 " 
 
 Deer Bay Lake 785 " 
 
 Stoney and Salmon Trout Lakes 758 " 
 
 Rice Lake 596 " 
 
 The distance from Salmon Trout Lake to the junction of Crow River is 
 about nineteen miles in a straight line, and the height of the Trent 
 there is 542 feet. Belmont Lake, which is surrounded by Laurentian strata, 
 is about eight miles to the north on Crow River, but not more than 
 eleven miles from Salmon Trout Lake, and is 599 feet above the sea ; by 
 which it appears that on the west side of Crow River, which has its source 
 forty miles north of Belmont Lake, there is a considerable rise in the land. 
 The main tributary on the south side of the Trent is the Scugog ; in 
 Scugog Lake it approaches to within seventeen miles of Lake Ontario. 
 The height of Scugog Lake is 797 feet above the sea, and as Sturgeon 
 Lake into which it is discharged is only a few feet lower, it is evident thai 
 the summit of the drift for twenty-five miles northward must be nearly 
 horizontal. This horizontally is preserved twenty-five miles eastward to 
 the neighborhood of Peterborough on the Ottonnabee, so that while the 
 latter stream flows southward, there are two additional parallel tributaries 
 between it and the Scugog which run northward. 
 Watershed be- A very narrow water-shed, bearing nearly north and south, separates 
 the tributaries of the Trent from those of Lake Simcoe and the Severn, 
 while the dividing line on the drift ridge between the tributaries of Lake 
 Huron and those of Lake Ontario is nearly east and west. Between the 
 Holland and the Humber, Mr. Tully, in his report on the proposed Geor- 
 gian Bay Canal, states the height of the ridge to be/904 feet above the 
 sea. To the east of this the ridge is crossed by the Toronto and Simcoe 
 railroad, in the Township of King, at a height of 987 feet ; while to the west, 
 where it abuts against the Upper Silurian escarpment on the line between 
 the townships of Adjala and Albion, and separates the Humber from the 
 Nottawasaga, its height is 950 feet. As shewing the slope of the drift 
 northward, it may be here stated that Lake Simcoe, occupying 283 square 
 miles, is 704 feet above the sea ; and though this lake is tributary to 
 Lake Huron, the depression in which it lies is a continuation of the valley 
 of the Trent, which can thus be traced from Georgian Bay to Kingston. 
 
 Except on or not very far from the shore of Lake Ontario, there are no 
 exposures of palaeozoic strata between Peterborough and the Niagara 
 escarpment for a breadth of forty miles, so that the deposit connected with 
 the drift ridge would appear to have an area of between 3000 and 4000 
 square miles. If the palaeozoic surface beneath presents the same char- 
 acter that it does in other parts of the plain, it seems probable that it will 
 rise with a pretty even elope from the exposures on the lake to those north 
 of it, and that a depression would accompany the softer deposits of the 
 
CHAP. I.] GEOGRAPHICAL DESCRIPTION. 13 
 
 period from Georgian Bay to Lake Ontario. This would give a probable 
 depth of 400 feet to the drift along the chief part of the ridge, with a still 
 greater depth over the depression. 
 
 In that part of the Lower Silurian plain which lies between Lake Ontario 
 and the Hudson River, Lake Oneida, discharging into Lake Ontario by the 
 Oswego river, occupies a position in the same valley as the Mohawk, which 
 flows hi a contrary direction to join the Hudson at Troy. Lake Oneida, Relative levels, 
 with a height of 400 feet above the sea, is only fifteen miles removed from 
 the Mohawk at Rome, and the height of land between them is forty-two 
 feet above Oneida ; so that a depression of the continent of 442 feet would 
 bring the ocean into Lake Ontario by the valleys of the Mohawk and the 
 Hudson, as well as by that of the St. Lawrence. It would drown all the 
 Lower Silurian plain in Eastern Canada, as well as the triangular portion 
 between the St. Lawrence and the Ottawa. It would convert the latter 
 river into an inlet as far as Roche Capitaine, upwards of 200 miles above 
 Montreal, and carry the present inlet of the Saguenay beyond Lake St. 
 John. The waves of such an ocean would wash the base of the Middle 
 Silurian escarpment from the valley of the Hudson to the upper end of 
 Lake Ontario. If the drift were removed from the supposed valley in the 
 surface of the palaeozoic rocks between Georgian Bay and Lake Ontario, 
 a depth of 136 feet in this valley beneath the level of Lake Huron would 
 so far lower the surface of Georgian Bay as to constitute it a part of the 
 Ontario sea, and cause the emergence* of the sub-aqueous ridge of the 
 Middle Silurian escarpment between Cabot's Head and the Great Manitou- 
 lin Island, making dry the narrow channels on each side of Lacloche 
 Island. Lakes Huron and Michigan, lowered to a level beneath the bed of 
 the St. Clair River, would escape by a cascade into Georgian Bay through 
 the deepest part of the Manitoulin Strait ; or if any part of the strait were 
 sufficiently profound, the lakes would be lowered equally with Georgian 
 Bay and communicate directly with the Ontario sea, while Lake Erie would 
 be left to escape by its present exit. 
 
 There are no evidences that this condition of circumstances has Middle saurian 
 existed, and the statement is made merely to illustrate relative levels ; escar P ment - 
 but the face of the Middle Silurian escarpment in some parts appears 
 to shew traces of having suffered the operation of destructive causes 
 greater than those now existing, perhaps when the continent was even 
 more deeply submerged than would be sufficient to bring the ocean 
 through the valleys of the Hudson and Mohawk. The waters of the 
 Nottawasaga and the Humber, flowing hi the same line in opposite direc- 
 tions, are separated, as has already been said, by the central drift ridge. 
 The valley of the former river is broad, and on the west side it is bounded 
 by an escarpment of red marl and sandstones, with a strongly marked 
 band of grey sandstone above them, and crowned by the Middle Silurian 
 
14 GEOLOGY OF CANADA. [CHAP. I. 
 
 limestone, which constitutes the summit. From the margin of the stream 
 in the centre of the valley, a gentle rise over a breadth of twelve or thirteen 
 miles reaches the foot of the escarpment, and after a short and sharp 
 ascent over a portion of the red and grey strata, the solid limestone pre- 
 sents precipices rising at once or in successive steps to the summit. From 
 the west side of the valley the main trunk of the river is supplied by many 
 tributaries, and the west branch of the main stream itself takes its origin 
 upon it. But though the summit or edge of the escarpment exhibits the 
 range of highest points on the valley, and the dip of the strata is westward, 
 a direction opposite to the flow of the tributaries, the water-shed which 
 divides these from the streams that empty themselves into Lake Erie and 
 the southern part of Lake Huron is from three to nine miles west of the 
 escarpment, lying on the back of the calcareous strata, which form its 
 upper part. It is by these ravines, cut clean through the solid limestone 
 and far down into the softer red marls below, that the waters of the 
 its ravines and intermediate land find an outlet to the valley. These ravines afford scenes 
 of the wildest and most picturesque confusion. Great blocks and fallen 
 masses of the limestone, which in many places is seen towering 200 feet 
 above, lie scattered over the bottom of the gorge, while others constitute a 
 talus at the base of the precipice, as if to form it a whole cliff had been 
 shaken into mighty fragments, among which are holes and interstices so 
 numerous, large, and deep, that jt is dangerous to pass along. Great 
 impending masses of the perpendicular cliffs themselves, comprising occa- 
 sionally an acre, cracked off from the main body of the rock, dip slightly 
 in towards the ravine, and the rents which separate them from the strata 
 in place, with a width of from twenty to thirty feet, are sometimes so 
 profound, that a great pine tree, 120 feet in length, which, blown over by 
 the wind, has fallen obliquely into the crevice, will be seen hanging head 
 downwards, still attached by some unbroken part of its roots to the edge 
 of the chasm, the bottom of which is hid in darkness below the other 
 extremity. The rents appear to be generally in the natural joints of the 
 rock ; their sides are quite smooth and even, and while a main one will 
 separate an acre from the mountain, many minor ones running parallel, 
 usually in two directions, will divide the area into several rhomboidal parts. 
 Some of the tributaries may run through ten miles of their course in these 
 ravines, and though their turbulence and velocity is usually so great during 
 freshets that one of them is appropriately termed the Mad River, the 
 quantity of water which they convey cannot be considered sufficient to have 
 produced the effects observed ; and this is corroborated by the circumstance 
 that dislocated masses are not wanting in those parts of the escarpment 
 which exist between the tributaries and face the general valley. Not only 
 in the valley of the Nottawasaga, but in many other parts, the escarpment 
 has the aspect of an ancient sea-cliff, and when the plain at its foot is seen 
 
CHAP. I.] GEOGRAPHICAL DESCRIPTION. 15 
 
 from a favorable spot on the summit, the great extent of surface over which 
 the eye wanders without perceiving any undulation, and the even unbroken 
 straight line of the distant horizon, almost deceive the imagination into the 
 belief that they still belong to a sea instead of to a fertile wooded land. 
 
 From the summit of the escarpment, the surface has a general slope to Rivers of west- 
 Lakes Erie and Huron, in a curve corresponding with their positions. ei 
 The highest part appears to be the Blue Mountains in the neighborhood 
 of Melancthon, and from the back of them descend three of the principal 
 rivers that drain the area, the Saugeen, the Maitland, and the Grand River ; 
 the first two running generally transverse to the stratification into Lake 
 Huron, and the last into Lake Erie, following the strike and curving round 
 the extremity of Lake Ontario. Another of the principal streams is the 
 Thames, which has its main sources west of the valley of the Grand River, 
 on the axis of the turn alluded to, and flows between Lakes Erie and Huron, 
 and parallel with the nearest coast of both, into Lake St. Clair. The 
 bearing of the Thames and the curve of the Grand River are both related 
 to the same geological form. The turn in the stratification is due to a low 
 anticlinal arch, a shallow valley on the crown of which guides the course 
 of the Thames : the course of the Sydenham, a stream running parallel 
 with the Thames at a short distance northward, is influenced by the same 
 anticlinal. The effect of this anticlinal is traceable for nearly a thousand 
 miles, in the course of which it runs under the city of Cincinnati on the 
 Ohio. 
 
 The plains which stand between the valleys of these rivers keep a pretty Heights on 
 uniform level of about 1200 feet above the sea for a considerable distance Tru 
 westward, in the latitude of Toronto. The Grand Trunk railway from 
 Toronto to Sarnia rises to the upper plain through a breach in the escarp- 
 ment, forming a valley for a tributary of the Credit, and, after passing over 
 the water-shed and reaching to within nine or ten miles of the base of 
 the Middle Silurian shield near Georgetown in Esquesing, the level of the 
 road at Rockwood is 1200 feet above the sea ; at Guelph (thirty-five feet 
 above the Speed, a tributary of the Grand River) it is 1057 feet ; crossing 
 the Grand River it is 997 feet, and near Petersburgh in Wilmot 1235 feet ; 
 but northward of this, between the Canistaga and Smith rivers, both 
 tributary to the Grand River, there is said to be a ridge 200 feet higher. 
 At Hamburgh and Stratford the road is 1207 feet, and continues at this 
 level to St. Mary in Blanchard, on the west branch of the Thames ; at Lon- 
 don it is 802 feet, and the land is not higher than this at any place between 
 London and Sarnia. The Buffalo and Goderich railway, which crosses the 
 Grand Trunk at Stratford, rises to a summit-level of 1209 feet in Fullarton ; 
 and on the dividing line between the townships of Tucker-Smith and Hibbert, 
 where it is about seventeen miles from the nearest coast of Lake Huron, the 
 road is 1050 feet above the sea. The line of these two roads from Rock- 
 
16 GEOLOGY OF CANADA. [CHAP. I. 
 
 wood to Hibbert sweeps partially round the Blue Mountains in Melancthon 
 in an irregular curve, at a distance varying from fifty to seventy miles, and 
 the curve would be still farther continued were a line of equal elevation 
 followed from Hibbert northward. From this curved line the surfaces of 
 the interspaces on the one hand appear to ascend gradually with the 
 beds of the streams, though rather more slowly, until they culminate in a 
 flat broken-edged semi-dome 1600 feet above the sea, to the highest point 
 of which allusion has already been made as overlooking the valley of the 
 Nottawasaga; while on the other hand the land descends rather more 
 rapidly towards the lakes, and to that part lying between them which 
 extends from the neighborhood of London to the entrance of the Detroit 
 River into Lake Erie. The rocks of this lower portion of the area are in 
 part softer than those of the higher country; they are of the Devonian 
 period, and it is chiefly out of them that have been excavated the depres- 
 sions which hold Lake Erie and the main body of Lake Huron, 
 surfece of the It would appear from what has been said that though the Canadian part 
 western Pemn- ^ ^ U pp er pi am? occupying about 10,000 square miles, has a general 
 smooth surface, it swells into a height which is not inferior in elevation to 
 some of the highest points in the more rugged Laurentian country betwe'en 
 Lake Huron and the Ottawa. Its palaeozoic strata have a dip conforming 
 in direction with the general slope of the geographical surface, and though 
 the inclination of the strata is greater than that of the surface, it is still so 
 small that by the eye it cannot be distinguished from horizontality. As in 
 the plain to the east of the escarpment, this part is thickly covered with drift, 
 largely derived from calcareous rocks ; and both areas, possessing soils of 
 remarkable fertility, are endowed with great agricultural capabilities. From 
 its relation to the great lakes nearly surrounding it, that portion of the coun- 
 try west of a line between Toronto and Georgian Bay is appropriately called 
 the Western Peninsula. It has a coast line of about 800 miles in extent ; 
 the only natural impediment to the intercommunication of all the ports of 
 which with one another, by vessels capable of navigating the ocean, is the 
 fall occasioned by the Middle Silurian escarpment. This obstacle is 
 obviated by the Welland canal, extending from the mouth of the Grand 
 River on Lake Erie to Port Dalhousie on Lake Ontario. It has a length 
 of twenty-eight miles, and by means of twenty-seven locks, accommodating 
 vessels of 350 tons burden, it overcomes a total difference of level of 333 
 feet. By its establishment, and that of the various railroads which within a 
 comparatively recent period have been carried through the country, the 
 western peninsula has advanced in improvement with a truly wonderful 
 rapidity. 
 
 The southern peninsula of Michigan, lying between Lake Huron and 
 Lake Michigan, and comprising an area of about 40,000 square miles, 
 though in part composed of rocks of a different epoch, (about one third of 
 
CHAP. I.] GEOGRAPHICAL DESCRIPTION. 17 
 
 it in the centre being of the Carboniferous age,) offers no contradiction to peninsula of 
 the general horizontalit y of the upper plain. As described b y Dr. Houghton, Michi s an - 
 its rocks consisting for the most part of nearly horizontal strata of sandstones, 
 limestones and shales, give character to a beautifully varied succession of 
 hills and valleys, as also to a soil admirably adapted .to the purposes of 
 agriculture. It is surrounded by a belt of nearly level country, varying in 
 width from five to twenty-five miles, which gradually obtains a greater 
 elevation as we proceed to the interior. The rise culminates in a water-shed, 
 attaining in some parts a height of 1200 or 1300 feet above the sea, and 
 separating the streams flowing in opposite directions to the two great lakes. 
 From the manner in which the main streams interlock, it seems probable 
 that the differences of level on the plateau are not very sudden or very 
 considerable. The width of the peninsula, excluding the indentation made its waters. 
 by Saginaw Bay, may be considered about 180 miles ; and the winding 
 character of the water-shed is such that while a portion of the streams 
 which discharge into Saginaw Bay take their source about sixty miles from 
 Lake Michigan, some of those emptying themselves into the southern part 
 of Michigan rise about sixty miles from Lake St. Clair. Three lines of 
 railroad cross the water-shed in a breadth of nearly eighty miles, and the 
 following are the heights which they indicate : the Detroit and Milwau- 
 kee, the most northern, gives 765 feet near Corunna in Sheawassee ; the 
 Michigan Central, 1023 feet between Chelsea and Grass Lake ; and the 
 Michigan Southern, 1105 feet at Osceo in Hillsdale. 
 
 The rocks of the peninsula lie in the form of a basin ; so that the same its rocks, 
 formations which constitute the bottom of Lake Huron crop out under the 
 waters of Lake Michigan, and these same formations give to a portion of 
 the country south of the peninsula a surface somewhat lower than its more 
 northern centre. The distribution of the whole series of palaeozoic rocks 
 ia their relation to the great lakes of the St. Lawrence presents one of the 
 grandest instances to be met with of the guiding influence of geological 
 structure in producing geographical peculiarities. The arrangement of Geology of 
 the lakes is traceable to the arrangement of two distinct parallel zones of 
 strata, the softer members of which have yielded with comparative facility 
 to the wear producing the excavations holding the water. Erie, the main 
 body of Huron and Michigan, may thus be termed Devonian lakes, while 
 Ontario, Georgian Bay, its continuation in the channel north of the 
 Manitoulins, Green Bay, and the expansion of Superior, are Lower Silurian 
 lakes, while the land which separates the two aqueous ranges from one 
 another is a Middle and Upper Silurian ridge. 
 
 It has been mentioned above that the shielding limestone of this ridge 
 composes the horns of Green Bay. In its progress southward from them 
 it constitutes the west side of Lake Michigan, and sweeps round the 
 coal basin of Michigan to the western part of Lake Erie ; forming a 
 
 B 
 
18 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. 1. 
 
 nmetfcan rim to the basin, which, though but slightly raised, is sufficient to con- 
 5oai fields, gfttute a water-shed between tributaries of the St. Lawrence and 
 others of the Mississippi. A little south-west of Lake Michigan it bends 
 over a flat anticlinal arch, which separates the Michigan basin from the 
 great basin of Illinois and that of Iowa farther west, as it does at the 
 upper end of Lake Erie over the Cincinnati anticlinal, which runs between 
 the Michigan basin and the great basin of Appalachia, the Iowa, Illinois 
 and Appalachian depressions containing three of the largest coal areas 
 of the world. The Appalachian coal measures are separated from Lake 
 Erie by the upper members of the Devonian series, as are the Michi- 
 gan measures from Lake Huron on one side and Lake Michigan on 
 the other ; and on the south side of Lake Erie, within but a few miles of 
 its margin, these upper Devonian rocks give origin to the northern 
 tributaries of the Ohio. This river drains nearly all the plain between 
 Lake Erie and the Appalachian range, and with its affluent the Alleghany 
 runs for about 300 miles with the Appalachian coal measures, and then 
 about 400 more transverse to the stratification to the Mississippi, crossing 
 the Cincinnati anticlinal and the south part of the coal basin of Illinois. 
 Mississippi, Some of the eastern tributaries of the north part of the Mississippi take 
 RedEiver, their sources almost as near to the margin of Lake Superior as those 
 already mentioned do to the Devonian group of lakes ; so that from almost 
 the very margin of the whole of these great lakes, excluding Ontario, there 
 is a gradual descent in the general surface to the Gulf of Mexico, with 
 but few elevations, excepting perhaps near Lake Superior, exceeding 1000 
 feet above the sea. The source of that branch of the Mississippi which 
 goes by this name is nearly in the latitude of the west end of Lake Superior, 
 and the source of the Red River is in the same vicinity. These two streams, 
 flowing in opposite directions, preserve a general line parallel with the 
 Rocky Mountains from the northern end of Lake Winepeg to New Orleans, 
 nearly twenty-five degrees of latitude. The Missouri however is in reality 
 the main trunk of the Mississippi. It also for 700 miles of its course, from 
 about the forty-eighth parallel to the Kanzas, flows parallel with the upper 
 Mississippi, with a breadth of 250 miles between them hi which all the 
 Kocky Moun- main streams have pretty much the same bearing. But the upper part of 
 tain8 - the Missouri and all the western tributaries of the river, and the main 
 
 western affluent of Lake Winepeg descending from the Rocky Mountains 
 almost at right angles, shew the gradual rise of the land to this great 
 dominant ridge of the continent. The whole surface of the North Ameri- 
 can continent on the east side of this great dominant ridge has been 
 described by Sir John Richardson with considerable truth to be a vast 
 inclined plain, in which the Laurentide and Appalachian ranges are mere 
 roughened parts, presenting but a few points rising to a sufficient height to 
 disturb its uniformity. 
 
CHAP. II.] GEOLOGY OF CANADA. 19 
 
 CHAPTER II. 
 
 GEOLOGICAL NOMENCLATURE. 
 
 DIVISIONS OF THE NEW YORK ROCKS; THEIR NOMENCLATURE. PARALLELISM WITH EURO- 
 PEAN ROCKS. AZOIC ROCKS OB 1 NORTH AMERICA; THEIR NAMES. TABULAR VIEW OF 
 
 CANADIAN ROCKS. 
 
 In the nomenclature which has been adopted for the geological forma- Eocks of 
 tions of Canada, the system of local designations has been resorted to NewYork - 
 as the one generally considered to be most convenient. In the names 
 used we have been desirous of availing ourselves as much as possible of 
 those which have been applied to well established groups of strata else- 
 where, with a view of at once facilitating comparisons of equivalent masses, 
 and of rendering homage to those whose labors have aided us in under- 
 standing our own rocks. The investigations which had already been 
 made in the state of New York, when the Canadian Survey commenced, 
 had in some degree rendered the stratigraphical nomenclature of that 
 state classic in America, and, while the undisturbed condition of the masses 
 in that part of the state which furnished the local names rendered the 
 sequence certain, the formations passed from New York into Canada in 
 such a manner that there was no doubt of their equivalence on the opposite 
 sides of the boundary. For the subordinate groups of fossiliferous strata 
 it thus became extremely convenient to adopt the nomenclature of New 
 York. 
 
 As nearly all the designations of the fossiliferous groups are derived 
 from local names, it has not been deemed expedient to make any change 
 in respect to the few exceptions in which they are founded upon litho- 
 logical characters ; and it is only when a group has not been recognized 
 among the rocks of New York, or when a mass there destitute of organic 
 remains is replaced in Canada by one marked by fossils, that a Canadian 
 name is introduced. 
 
20 GEOLOGY OF CANADA. [CHAP. II. 
 
 The rocks met with in the Canadian portion of the area comprehended 
 in the topographical description of the previous chapter are designated as 
 follows in descending order : 
 
 CARBONIFEROUS. 
 20. Bonaventure formation. 
 
 DEVONIAN. 
 
 19. Portage and Chemung group. 
 18. Hamilton formation. 
 17. Corniferous " 
 16. Oriskany 
 
 UPPER SILURIAN. 
 
 15. Lower Helderberg group. 
 14. Onondaga formation. 
 
 MIDDLE SILURIAN. 
 
 13. Guelph formation. 
 
 12. Niagara " \ 
 
 11. Clinton " > Anticosti group. 
 
 10. Medina " ) 
 
 LOWER SILURIAN. 
 
 9. Hudson River formation, 
 
 8. Utica " 
 
 7. Trenton " 
 
 6. Birdseye and Black River formation. 
 
 5. Chazy = Sillery ? 
 
 . azy = ery ) 
 
 4. Calciferous = LSvis \ Queb 1C 
 
 3. Potsdam group. 
 
 Azoic. 
 
 2. Huronian series. 
 1. Laurentian system. 
 
 Rocks of Th e equivalent lines of demarcation between the great divisions of the 
 Great fossiliferous rocks being now sufficiently well established on the opposite 
 sides of the Atlantic, the European designations are applied to them as 
 used by the Geological Survey of the United Kingdom, except in the 
 case of the term Middle Silurian, applied to designate an intermediate 
 series of rocks, which are not well defined in Great Britain. Systems of 
 
CHAP. II.] GEOLOGICAL NOMENCLATURE. 21 
 
 nomenclature, different from the one here adopted, have been used in 
 Pennsylvania and in other parts of North America. A table showing 
 these, and setting forth at the same time the sub-divisions of the palaeozoic 
 rocks in various parts of the world, and their relation to the Canadian 
 series, will be given as a sequel to the description of our rocks, where it 
 will be more intelligible. 
 
 To the azoic rocks no local names have yet been applied in any part of Azoic 
 America except in Canada, and as these rocks are here more extensively Eocks - 
 exposed than anywhere else on the continent, while it would be very 
 inconvenient to describe the geology of the province without the use of 
 special designations attached to them, the names of the Laurentian and the 
 Huronian systems or series, which we have been accustomed to apply to 
 them, are allowed to remain unchanged,' particularly as they have been 
 recognized abroad, and have been made by other geologists a standard of 
 comparison both in America and Europe. 
 
 With each local designation it will be perceived that we have associated 
 the term series, group, or formation, in place of the lithological distinction 
 which usually accompanies the local designation in the New York nomen- 
 clature, such as sandstone, limestone, slate, or shale. The reason for this 
 is, that in a country extending like Canada for a thousand miles in the 
 strike of the strata, the mineral character of any division may differ very 
 much in different localities, and the lithological term become inapplicable 
 in some particular case. 
 
22 GEOLOGY OF CANADA. [CHAP. III. 
 
 CHAPTER III. 
 
 / THE LAURENTIAN SYSTEM. 
 
 LATOENTIAN SYSTEM. THE OLDEST KNOWN STRATIFIED ROCKS.ORTHOCLASE GNEISS. LIME- 
 STONES AND THEIR ASSOCIATED MINERALS. IRON ORES. CONTORTED STRATA. MADAWA8- 
 
 KA SECTION. CONGLOMERATE BEDS. ANORTHOBITES ; THEIR FELDSPARS AND ASSOCIATED 
 
 MINERALS. VEINS OF SEGREGATION CONTAINING PYROXENE AND FELDSPAR. METALLIF- 
 EROUS LODES. INTRUSIVE ROCKS ; DOLERITE, SYENITE, QUARTZIFEROUS PORPHYRIES. CHERT 
 VEINS. DISTRIBUTION AND STRUCTURE OF THE LAURENTIAN SYSTEM ; ITS PROBABLE 
 THICKNESS. SUPPOSED FOSSILS IN THE SYSTEM. 
 
 The rocks which compose the Laurentian Mountains were shown by the 
 Geological Survey, in 1846, to consist of a series of metamorphic sedimen- 
 tary strata underlying the fossiliferous rocks of the province. They have 
 since been recognized by Sir Roderick Murchison, as forming the so-called 
 fundamental gneiss of the Western Islands of Scotland and parts of Ross- 
 shire and Sutherlandshire, and the name of the Laurentian system, first 
 applied in Canada, has now been extended to them in Great Britain, where 
 as well as in this country they are the oldest rocks known, and lie at the 
 base of the sedimentary series. They are altered to a highly crystalline 
 condition, and are composed of feldspathic rocks interstratified with impor- 
 tant masses of limestone and quartzite. Great vertical thicknesses of the 
 series are composed of gneiss containing chiefly orthoclase or potash feld- 
 spar, while other great portions are destitute of quartz and composed chiefly 
 of a lime-soda feldspar, varying in composition from andesine to anorthite, 
 Anorthosite. and associated with pyroxene or hypersthene. This rock we shall distin- 
 guish by the name of anorthosite.* 
 
 Orthociase The orthoclase gneiss is generally of some reddish tint, arising from the 
 prevailing color of the feldspar, which varies from very pale to very deep 
 flesh-red, though it is often white and frequently of a bluish-grey. This 
 rock has in no instance been found destitute of quartz : hornblende is 
 seldom absent, and mica very often present. The quartz is generally white, 
 
 * Since all these varying triclinic feldspars are anorthic in crystallization, and ap- 
 proach more or less to anorthite in their composition, Delesse thus proposed to desig- 
 nate them by the common name of anorthose, as distinguished from orthose or ortho- 
 clase, and the rocks characterised by their presence as anorthosite. In accordance with 
 this we have adopted the generic name of anorthosite for these rocks. 
 
CHAP. III.] LAURENTIAN SYSTEM. 23 
 
 but often colorless and translucent ; the hornblende is usually black, but 
 sometimes green ; the mica is often nearly black, frequently brown, and 
 generally of some dark color. A great portion of the rock is fine grained, 
 and, though the constituent minerals are arranged in parallel layers, no 
 one constituent predominates in any layer to the exclusion of others ; but 
 even in their subordinate arrangement there is an observable tendency to 
 parallelism. A thick bed of reddish feldspathic rock, for example, will in 
 vertical section present a number of short dashes of black hornblende or 
 black mica all drawn in one direction, and apparently destitute of arrange- 
 ment except in regard to parallelism. The continuation of these lines will 
 be interrupted irregularly, and before one ends another will commence 
 above or below it, the lines interlocking among one another. Sometimes 
 these continuous black bands will run in the rock for considerable dis- 
 tances, or the rock will be barred by parallel streaks of white quartz or 
 white feldspar, in which as well as in the red part the dark and dotted 
 lines will continue. The same description of arrangement will be found 
 when the whole ground of the rock is white instead of red, and then the 
 red feldspar will occasionally constitute streaks. There is no end to the 
 diversity of arrangement of the component minerals, but there is a never 
 failing constancy in respect to their parallelism, which, however, though 
 never absent, is sometimes obscure. 
 
 Very large masses of this rock are frequently coarse grained. These Granitoid 
 are usually very feldspathic, the feldspar being in cleavable masses often gl 
 attaining an inch and sometimes more in diameter, while the mica and the 
 quartz, often accompanied by hornblende, and the former sometimes replaced 
 by it, are distributed among the feldspar in such a manner as to give a 
 reticulated aspect to the surface .of the rock. Beds of this character 
 are sometimes thin, but when thick, which they usually are, might on 
 first inspection be mistaken for intrusive igneous instead of altered sedi- 
 mentary masses. Upon a careful study of any such mass however it will 
 be perceived that this reticulated structure is accompanied by an obscure 
 arrangement of the meshes of the network into parallel lines, which will be 
 found conformable with the more distinctly banded portion of the strata. 
 
 There is as great a diversity in the arrangement of the masses as in the 
 minerals composing them. The greatest masses appear to be formed of the 
 coarse grained porphyroid gneiss above described. These rise into the 
 highest ridges and peaks of the orthoclase region, and generally constitute 
 the main body of rock separating one important band of limestone from 
 another. They appear sometimes to attain several thousand feet in thick- 
 ness, divided however at unequal intervals by thinner and less feldspathic 
 masses in which the stratification is more distinct. The quartz occasionally Quartzite. 
 presents masses of considerable volume, two of which, nearly pure, occur 
 in the district of the Rouge, a tributary of the Ottawa, one 400 and the 
 
24 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. III. 
 
 Hornblende other 600 feet thick. The hornblende often forms a massive rock : a band 
 of it in Blythfield has a thickness of 200 feet. Mica associated with 
 hornblende and with quartz characterises great thicknesses of hornblende 
 and micaceous schists. 
 
 Though there does not appear to be any special order in which the 
 masses succeed one another, beds of hornblende rock and hornblendic 
 schist seem often to be more abundant near the interstratified bands of 
 limestone than elsewhere, and in the same neighborhood there usually 
 occurs a more frequent repetition of beds of quartzite than in other 
 
 Pyroxene and parts. Near the limestones, pyroxene, which in other parts does not 
 
 garnet rocks. a pp ear fa fo e very abundantly disseminated, is occasionally met with, 
 forming massive beds. Pink or raspberry-red garnets are often thickly 
 disseminated in bands of micaceous or hornblendic gneiss and quartzite. 
 Although these are not confined to the immediate proximity of the lime- 
 stones, they are more commonly met with there than elsewhere, and it 
 generally happens that the limestone masses are limited on the one side 
 and frequently on both, by garnet-bearing rock. Near the Three 
 Mountains, about fifty miles up the Rouge, pink garnets are disseminated 
 through a gneiss consisting chiefly of a pure white crystalline orthoclase 
 feldspar, producing a rock of striking beauty. It is about 150 feet thick, 
 and runs along the upper side of one of the bands of limestone for a con- 
 siderable distance. A few miles from this, however, the bed passes into 
 a reddish and more quartzose garnet-bearing gneiss, and in a third position 
 becomes a garnetiferous quartzite. 
 
 Limestones. The masses of limestone are in general crystalline in a high degree ; 
 occasionally they are composed of an aggregation of rhombohedral crystals 
 of calcspar with faces an inch square. They are usually coarse grained, 
 but sometimes saccharoidal ; iJiough it rarely happens that they are so fine 
 in texture as to be entitled to the designation of compact. Their general 
 color is white ; they are often barred with grey in the direction of the strata, 
 and are occasionally wholly grey. They are sometimes partially salmon or 
 flesh-red ; but this tinge has not been seen diffused throughout a bed, or 
 extended to any great distance in it. It is seldom that beds are composed of 
 pure carbonate of lime : several accidental minerals are usually associated 
 with this, and they may vary in quantity and kind in different parts of a 
 group of strata both horizontally and vertically. The most frequent minerals 
 imbedded in the limestones are serpentine, pyroxene, tremolite, hornblende, 
 wollastonite, mica, graphite, apatite, chondrodite, quartz, scapolite, iron 
 pyrites, specular iron, with more rarely zircon, spinel, fluor spar, idocrase, 
 tourmaline, corundum, and copper pyrites. 
 
 Dolomites. Carbonate of lime and dolomite are frequently met with mechanically 
 mingled, giving rise to more or less magnesian limestones ; they often, 
 however, compose distinct beds interstratified with one another ; and in 
 
CHAP. III.] LAURENTIAN SYSTEM. 25 
 
 some parts great masses of nearly pure dolomite occur. The dolomite is 
 usually finer in texture than the limestone ; very little of it can be called 
 coarse grained. On Mazinaw Lake, in the township of Barrie, great masses 
 of it are saccharoidal and sufficiently pure to yield statuary marble, and in 
 Madoc and MacNab it is often compact. Its color is generally white, but 
 it is sometimes of a pale yellowish-red tinge, and when compact it has a 
 waxy lustre. The rock often weathers to some tinge of yellowish-brown. 
 
 It is not quite certain whether the accidental minerals characterise the 
 pure limestone and the dolomite equally, or whether there are marked distinc- 
 tions in the groups prevailing in each rock. Most of those which have been 
 mentioned however appear to be more abundant in the limestone than in 
 the dolomite. Serpentine is found associated with both rocks. It is Serpentine, 
 frequently disseminated in grams varying in size from the tenth to the 
 fourth of an inch: among these are occasionally scattered masses of 
 from six to ten inches in diameter, and sometimes the mineral forms 
 interstratified beds. When it occurs in grains .and larger scattered 
 masses, the grains, more or less closely aggregated, usually run in bands 
 parallel with the beds, and clearly mark the stratified character of the 
 rock. The colors of the serpentine are usually some tinge of green from 
 leek-green to oil-green and pale greenish-yellow ; sometimes the mineral is 
 resin colored, and occasionally masses of a pale yellowish-green are spotted 
 with crimson or blood-red patches from disseminated peroxyd of iron. 
 
 Another silicate of magnesia, which is met with in patches and occasion- Pyraiioiite. 
 ally in interstratified massive beds in the limestone, is pyrallolite or renssel- 
 aerite, a mineral closely allied to talc in composition. The color of the 
 mineral hitherto observed in Canada is usually a pale greenish-yellow, but 
 in the Laurentian series of New York, according to Emmons, it shews 
 various tints of grey and is occasionally black. It appears in general to 
 occur in the neighborhood of beds marked by serpentine, and aphrodite, 
 an allied mineral, is sometimes associated with it. 
 
 The limestone beds are sometimes characterised by grains of pyroxene Pyroxene, 
 disseminated in the rock in the same banded arrangement as the serpentine, 
 but not in such abundance, and occasionally there run with the stratification 
 masses composed of cleavable pyroxene associated with several other 
 minerals, making a very coarsely crystalline rock ; but these may some- 
 " times perhaps constitute veins of segregation, rather than beds. 
 
 Hornblende, in addition to being found in disseminated crystals, is Hornblende, 
 sometimes met with, more particularly in the form of tremolite, constituting 
 beds in the limestone and dolomite. These beds are sometimes many feet 
 thick, and the mineral occurs in them in parallel or radiating fibrous 
 masses, sometimes attaining eighteen inches in length, the interstices 
 among them being filled with the limestone or dolomite. 
 
26 GEOLOGY OF CANADA. [CHAP. III. 
 
 Mica and Mica and graphite very generally accompany one another in the calca- 
 
 graphite. reous j^^ an( j some Q f ^ese for many hundreds of feet in thickness are 
 seldom without them. It appears to be finely disseminated graphite that 
 occasionally gives to great masses of the limestone a grey color, and the 
 greater and less accumulation of it in different layers produces the bands 
 of darker and lighter grey that have been mentioned. Both the graphite 
 and the mica appear to be present in the dolomite as well as the limestone, 
 although perhaps not in so great abundance, and there are important masses 
 of dolomite which are almost wholly free from them. The chief colors of 
 the mica are blackish-brown and brownish-yellow ; but it is often golden 
 or brass-yellow, sometimes steel-blue, and frequently silvery or pearl- 
 white. The chief part of both the graphite and the mica occurs in small 
 scales. The graphite however is sometimes met with in patches or nests 
 subordinate to the stratification ; and when the mineral is found in quantities 
 available for economic purposes, it appears usually to be connected with 
 beds. Very large crystals of mica sometimes occur in abundance, enclosed 
 in pyroxene rock, accompanied with calcspar, apatite, iron pyrites, and 
 other minerals, the whole forming masses of a very coarse texture running 
 with the stratification. 
 
 pyrites. Crystals and grains of iron pyrites are often thickly disseminated in 
 
 both the limestone and the dolomite, and very frequently accompany the 
 mica and the graphite, arranged like them in parallel bands holding a greater 
 or less abundance of the mineral. Pyrites often characterises large 
 nodules and lenticular masses of gneiss or gneissoid pyroxenic rock 
 subordinate to the calcareous and dolomitic beds ; and strata of this 
 description, weathering to a rusty brown, and holding disseminated 
 graphite, very often limit the great masses of limestone and dolomite, and 
 afford a useful guide in tracing out their distribution. 
 
 chondrodite, Chondrodite, apatite, and most of the other accidental minerals belonging 
 apatite, fluor. ^ ^ ii mes t nes and the dolomites, present the same banded arrangement 
 as those already mentioned. The chondrodite in grains is often mingled 
 with grains of serpentine and pyroxene. The apatite, which is seldom 
 wholly absent from any great mass of the limestone, is generally in small 
 quantity, though it is found in some of the lime'stones of Elmsley, Burgess, 
 and Koss, in such proportions as may be economically available. In Eoss 
 it is accompanied by purple fluor spar. 
 
 oxydsof Specular and magnetic oxyds of iron are disseminated in scales and 
 
 iron. grains both in the gneiss and the limestone ; but there are also important 
 
 interstratified beds of these iron ores varying in thickness from a few feet 
 up to several hundreds, those of the magnetic oxyd being the thicker and 
 more numerous. Some of the thickest of these beds are interstratified 
 with layers of limestone, and as far as known most of them appear to be 
 
CHAP. III.] 
 
 LAURENTIAN SYSTEM. 
 
 27 
 
 either associated with the great limestone bands, or to be not far removed 
 from them in stratigraphical place. 
 
 Some of the bands of limestone are of great thickness, and passing to contorted 
 them from the gneiss there is occasionally an interstratification of smaller 
 calcareous beds. When one of these calcareous beds or a collection of 
 them is traced to some distance and then compared with the gneiss r 
 the stratigraphical relation of the two is readily made out, and it is 
 perceived that the limestone as a whole is conformable with the beds of 
 gneiss and parallel with those bands and streaks with which they are 
 marked. This relation however is not so evident when only small portions 
 are compared ; for it often happens\ that while an overlying or underlying 
 mass of gneiss will exhibit very regular and even lamellation, the subor- 
 dinate layers of it dividing the calcareous bed will display contortions 
 of the most complicated description, which appear more important in 
 proportion to the mass of limestone in which they occur. Where this is 
 great, the gneissoid beds, of several inches or a foot thick, which form the 
 subdivisions, will be bent and folded in a very extraordinary manner, or, 
 partially broken up into fragments, will be surrounded by the limestone. 
 
 The accompanying wood-cut (1) represents a section in the strike 
 of a calcareous bed between two and three feet thick occurring at the 
 Bagged Chute on the Madawaska, in Blythfield. The bed is inclosed 
 between masses of evenly laminated hornblendic gneiss, and is one of 
 several that succeed each other with considerable regularity, separated by 
 intervening layers of gneiss. Most of them present thin subordinate 
 layers consisting of quartz associated with feldspar and hornblende or mica, 
 being in fact nothing more than thin layers similar to the enclosing rock. 
 
 1. CONTORTED GNEISS BANDS IN LIMESTONE. SCALE ABOUT 5^. 
 
 I, I, Limestone including thin layers of gneiss, g-, g, Gneiss above and below limestone 
 
 These thin divisions are all more or less corrugated, while the thicker 
 masses above and below are comparatively even. The portion selected for 
 representation is somewhat more corrugated than the others, and the fold s 
 
28 GEOLOGY OF CANADA. [CHAP. III-. 
 
 very much resemble such as might be produced in parallel layers of paper, 
 were they placed in a viscid fluid to which some gentle movement should 
 be communicated. 
 
 Near the timber slide at the Chats two beds of gneiss of from six inches 
 to a foot thick, in limestone, shew a fold (2) which is supposed to be 
 similarly related to the gneiss limiting the mass. At a both of the beds 
 become broken into fragments, which are surrounded by the limestone. 
 
 2. GNEISS BANDS IN LIMESTONE. 8CALE ABOUT 
 ..'.'" 
 
 g, g, Bands of gneiss in the limestone, a, Broken parts of the gneiss bands. 
 
 Nodules in Fragments have occasionally been met with in the limestone which 
 
 appear to shew that thin quartzite beds have been folded and then twisted 
 spirally until one portion separated from another. Sometimes large 
 disjoined masses eight or ten feet in diameter, of a gneissoid character, 
 assuming somewhat the aspect of vast nodules, with parallel layers of the 
 constituent minerals, and much charged with pyrites, will be surrounded by 
 the limestone ; and several of these masses succeeding one another will 
 he found in the continuation of a bed of the same description. One 
 
 filling nssures -i 
 
 in gneiss. instance has been observed, where the limestone of a bed marked with 
 grains of serpentine appeared to have an uninterrupted connexion with 
 rock of identical character filling up a crack or fault in the gneiss at right 
 angles to the general direction of the strata. Notwithstanding these 
 irregularities however, it appears to be the case that the calcareous strata 
 taken in the large are parallel to the gneissoid beds, and alternate with 
 them in a well marked system of stratification. 
 
 Sf 01 ^ 11 . 011 , As an instance of the mode in which the beds succeed one another, the 
 
 tne Madaf ' 
 
 following section may be given, as measured at the High Falls on the 
 Madawaska, a tributary of the Ottawa, where the dip of the strata is 
 pretty constant hi direction, being from twenty-five to forty-five degrees 
 east of north, and varying in inclination from fifteen to thirty degrees. 
 
CHAP. III.] LAURENTIAN SYSTEM, 29 
 
 The beds are given in descending order : 
 
 Feet. 
 
 Grey speckled hornblendic gneiss of a schistose character, occasionally striped 
 with darker and lighter colors, caused by a greater or less preponderance 
 of black hornblende and blackish-brown mica ; some of the beds have long 
 white dashes on them, arising from the presence of white feldspar ; towards 
 the bottom some of the layers have thin lines of a reddish color, occasioned 
 
 by flesh-red feldspar, 32 
 
 Grey speckled micaceo-hornblendic gneiss of much the same character, 26 
 
 Grey hornblendic gneiss in three bands of five feet each, and reddish gneiss in 
 
 three bands of two feet each, 2 L 
 
 Measures concealed, with the exception of some reddish gneiss at the top, 23 
 
 Reddish micaceo-hornblendic gneiss, with black hornblende and brownish-black 
 
 mica, 3 
 
 White crystalline limestone, 3 
 
 Grey hornblendic gneiss, * 15 
 
 Measures concealed, 34 
 
 Reddish hornblendic gneiss not well displayed, 20 
 
 Measures concealed, 37 
 
 Reddish hornblendic gneiss composed of red feldspar, translucent colorless quartz, 
 and black hornblende, forming dotted lines upon the red feldspar ; there are 
 occasional layers of red feldspar without black dotted lines, and there are a 
 
 few irregular layers more large grained than the rest, 51 
 
 Reddish hornblendic gneiss ; black layers of an inch are of occasional occurrence, 
 the color being derived From the presence of hornblende ; the rock splits in 
 the direction of these layers ; iron pyrites occurs irregularly in patches com- 
 posed of groups of crystals, giving by its decomposition a rusty-brown color 
 
 to a portion of the beds, 84 
 
 Reddish hornblendic gneiss of much the same character as the last, 105 
 
 Black hornblendic gneiss and white crystalline limestone in alternating layers ; 
 the gneiss is composed of black hornblende, blackish-brown mica, and 
 greenish-white feldspar and quartz ; the limestone holds graphite and golden- 
 yellow mica in small scales ; the beds are irregularly arranged, and there are 
 
 occasional lumps weathering into knobs on the surface, 3 
 
 White crystalline limestone, much of it consisting of transparent colorless calc- 
 spar, with graphite and golden-yellow mica in small scales j lumps of a 
 rusty-brown color holding mica are irregularly displayed in the bed, and in 
 the weathering of the rock there appear raised lines of very small grains of 
 serpentine and tremolite ; these dotted lines run above and below the rusty- 
 brown lumps, giving place to and enclosing them, 2 
 
 Dark grey hornblendic gneiss with limestone similar to the last ; this and the 
 two previous beds come to a point in the direction of the dip r and appear to 
 be part of a lenticular mass filling up a hollow in the bottom of the reddisa 
 
 hornblendic gneiss previously mentioned, 
 
 Dark grey hornblendic gneiss with white crystalline limes-tone, as before, 4 
 
 Grey hornblendic gneiss with greyish-white bands of a quartzose character and 
 
 two bands of limestone with much black mica, 2 
 
 White crystalline limestone with bands of rusty-brown hornblendic gneiss in the 
 middle from six to eight inches thick ; there is more mica in the limestone 
 
 than before, and the upper surface of the bed is uneven, 4 
 
 Grey thin bedded schistose gneiss with more translucent colorless quartz and 
 more black mica than before ; the beds are separated by thin layers of lime- 
 stone, and there is a considerable amount of hornblende on the surfaces upon 
 
30 GEOLOGY OF CANADA. [CHAP. HI. 
 
 Feet. 
 which the limestone rests, which is made perceptible by being weathered 
 
 into relief in exposed parts, 12 
 
 Grey thin-bedded schistose gneiss, 12 
 
 Eeddish hornblendic gneiss similar to that previously mentioned, 139 
 
 White crystalline limestone holding scales of mica and graphite, and having at 
 the top a layer of dark mica two inches thick, and another near the bottom, 
 with a layer of green fibrous actynolite above and another below ; the layers 
 of actynolite are each two inches thick, and the fibrous structure is transverse 
 
 to them ; massive pyroxene is associated with one of the layers, 1 
 
 Reddish micaceo-hornblendic gneiss, 15 
 
 Grey schistose gneiss with more mica and quartz than the last, 34 
 
 Grey schistose gneiss, in some parts of the vertical thickness nearly black from 
 hornblende and mica ; a layer or two of white quartz is present in the mass, 
 and two or three feet at the top are composed of limestone, which disinte- 
 grates rapidly, probably from the presence of iron pyrites ; there are many 
 lumps of a harder description than the rest in the decomposing mass, and 
 
 much mica in its ruins, 33 
 
 Light grey gneiss dividing into beds of from three to eight inches ; it appears to 
 be more quartzose than usual, and some of the beds are nearly altogether 
 
 composed of translucent colorless quartz, 31 
 
 At this point there appears to be a disturbance of some kind ; approach- 
 ing it there is a mass of very large-grained rock with red orthoclase feldspar 
 and translucent colorless quartz without hornblende or micaj it indis- 
 tinctly crosses the beds, the ends of which become lost in it. 
 
 Measures concealed by soil and herbage, 49 
 
 Dark grey gneiss obscurely exposed, 21 
 
 White crystalline limestone with very few scales of mica and graphite, @ 
 
 Dark grey quartzite separated into layers by partings of mica, 10 
 
 Dark grey micaceous gneiss with two small bands of crystalline limestone, 13 
 
 Dark grey schistose gneiss with black bands, the color of which is derived from 
 the presence of much black hornblende ; mica prevails where the rock is 
 
 most fissile, , 25 
 
 Black schistose gneiss with much hornblende ; the lower part has much black 
 
 mica, with layers composed of white feldspar and translucent colorless quartz, 51 
 Grey micaceo-hornblendic gneiss with black streaks composed of mica, and black 
 
 patches of the same, 42 
 
 Measures concealed by soil and vegetation, 80 
 
 Light grey hornblendic gneiss ; the beds, which are from two to six inches thick, 
 are very quartzose, and have a few specks of green hornblende and black 
 mica with opaque white feldspar, and some few streaks showing red feldspar, 10 
 
 Measures concealed by trees and moss, 63 
 
 Reddish hornblendic gneiss, 39 
 
 Grey hornblendic gneiss interstratified with crystalline limestone, 15 
 
 White crystalline limestone, containing abundant small scales of mica and 
 graphite, and interstratified with irregular corrugated layers, of which some 
 
 are very quartzose and some dotted with lines of black hornblende, 19 
 
 Reddish hornblendic gneiss of much the same character as that previously 
 
 described, 56 
 
 Measures concealed by the river, 7 
 
 Reddish hornblendic gneiss, 17 
 
 Reddish hornblendic gneiss not well exposed, 18 
 
 Dark grey or nearly black thin layers composed chiefly of black hornblende, 
 with some black mica and some crystals of white quartz and feldspar ; 
 interstratified with limestone having corrugated layers and many patches 
 
CHAP. III.] LAUKENTIAN SYSTEM. 31 
 
 Feet. 
 
 and spots, displaying tremolite and serpentine, as well as some with horn- 
 blende and mica. Near the bottom there is an irregular layer of limestone 
 
 from one to two feet thick, 25 
 
 White crystalline limestone with a few dark corrugated bands of gneiss, 12 
 
 Dark grey gneiss, consisting of black hornblende, black mica, and white feldspar 
 
 and quartz, 25 
 
 1351 
 
 In this section the gneiss preponderates over the limestone, and none of 
 the calcareous beds are of great thickness ; but a little higher in the series 
 on Calabogie Lake, on the fourteenth lot of the first range of Blythfield, a 
 bed of white crystalline limestone upwards of a hundred feet thick is seen, 
 with hornblendic gneiss above and a mass of very black hornblende rock 
 below. The upper portion of this is schistose, and contains yellow mica 
 between the layers, while the lower portion is highly crystalline. This 
 mass of hornblende rock, which in some parts has the aspect and composition 
 of fine greenstone, and in others has a small quantity of quartz in it, may 
 be upwards of 200 feet thick, and is again underlaid by limestone. 
 
 In other instances the amount of calcareous rock greatly surpasses the Thickness of 
 gneiss. At the Chenaux, for example, a succession of white crystalline 
 limestone strata on the left bank of the Ottawa, near the boundary line 
 between Clarendon and Litchfield, presents a breadth of 600 yards, with 
 but a moderate interstratification of harder rock. The dip is about 
 N. 15 E. < 10 20, giving a thickness of 400 feet and upwards, of 
 which not much more than one fifth consists of gneiss ; and it is probable 
 that the section is but part of a larger series of the same rocks inter- 
 stratified with one another much in the same proportion. On the twenty- 
 fourth lot of the first range of Clarendon there is a considerable display of 
 similar rocks, the breadth of which, unless there be sharp undetected folds, 
 would give a thickness of 4000 feet, about two thirds of which consists of 
 crystalline limestone. 
 
 Notwithstanding the general highly crystalline condition of the Lauren- conglomerate 
 tian rocks, beds of an unmistakeably conglomerate character are occasionally beds< 
 met with among them. Limestones similar to those which have been 
 described are extensively exposed in Bastard and South Crosby ; their 
 color is usually white, but sometimes greenish-white, or white with grey 
 bars or stripes. Small scales of graphite are invariably disseminated 
 through the rock, with serpentine, mica, and iron pyrites, and in the 
 twenty-seventh lot of the third range of South Crosby chondrodite is of 
 frequent occurrence, the disseminated mineral alternating with bands 
 containing mica. On the twenty-fourth lot of the tenth range of Bastard section in 
 a bed of conglomerate is interstratified between two of the beds of lime- 
 stone. The dip of the strata at the spot is N. 50 E. < 30, and the 
 following ascending section shows the character and relations of the beds : 
 
32 GEOLOGY OF CANADA. [CHAP. III. 
 
 Ft. in. 
 
 Pure white highly crystalline coarse grained limestone, with small disseminated 
 
 scales of graphite running in the layers, and grains of mica, 5 
 
 Coarse colorless translucent granular quartzite, containing cleavable masses of 
 white feldspar, readily decomposing by the action of the weather into 
 kaolin, with patches of greenish chloritic limestone containing brown mica ; 
 in some parts the feldspar is replaced by a soft greenish- white sub-translu- 
 cent unctuous mineral having a somewhat columnar structure and a waxy 
 lustre, resembling indurated talc, and there are present occasional scales of 
 graphite and grains of copper pyrites with blue carbonate, 4 
 
 Finer and more calcareous granular quartzite, with cleavable masses of feldspar 
 
 and calcspar and scales of graphite ; green stains occur in patches, 2 
 
 Coarse conglomerate, of which the matrix is a fine grained quartzose sandstone, 
 somewhat calcareous, containing white feldspar, which occurs in the form 
 of grains and pebbles, associated with large and small well defined pebbles 
 of vitreous, milk-blue, translucent, and sometimes opalescent quartz. There 
 are also pebbles of fine grained homogeneous greyish sandstone more calca- 
 reous than the matrix ; some similar to these, but nearly white and more pul- 
 verulent, afford to chemical tests a small quantity of phosphate of lime, and 
 others of yellowish-grey sandstone are finely but distinctly laminated, the 
 laminae being shewn by intervening bands of a white color ; one of the 
 laminated pebbles is characterised by a layer of coarser pebbles in one of 
 the bands. The sandstone pebbles are fiat, and' lie on their flat sides in 
 the general plane of the stratification. Mica is disseminated in considerable 
 abundance, and there are a few scales of graphite, , 1 6 
 
 Fine grained calcareous sandstone, 2 
 
 Fine grained, very hard, crystalline arenaceous bluish-grey limestone, weather- 
 ing reddish, with a few scales of graphite, 4 
 
 Pure white, highly crystalline, coarse grained limestone r with scales of graphite 
 in some abundance, and rounded grains of mica, besides small amber- 
 yellow grains of chondrodite running in layers, 6 
 
 13 6 
 
 On the bridge-island in Hog Lake, on the eleventh lot of the thirteenth 
 range of Huntingdon, calcareous mica schist is seen dipping to the north- 
 westward ; and on the road in the same lot, farther north, there is white 
 crystalline limestone with mica and graphite. The observed strike of 
 these strata north-eastward would carry them into the lake. On the north 
 side of the lake, in a position which would appear to overlie the previous 
 mentioned exposures, are contorted gneiss and micaceous schists cut by 
 red syenitic veins. The dip of the, stratification is north-westward, 
 lomer Proceeding northward, gneiss occurs on the first lot of the sixth range of 
 ates in Madoc. Madoc, and white crystalline limestone beyond it in the same numbered lot 
 in the sixth and seventh ranges. In a field a little way north from the 
 village of Madoc, still in ascending continuation of the section, a ridge of a 
 somewhat micaceous schist occurs ; it is slightly calcareous, of a bluish 
 color, weathering greenish, and holds numerous fragments of rock different 
 in character from the matrix, all being without calcareous matter, and some 
 of them resembling syenite or greenstone. North from this ridge another 
 
CHAP. III.] LATTRENTIAN SYSTEM. 33 
 
 succeeds, consisting of micaceous schists, beyond which, for 300 yards, ridges 
 of a decided conglomerate, with distinctly rounded pebbles enveloped in a 
 matrix of micaceous schist, alternate with ridges of schist containing few or no 
 pebbles. The exact dip of the strata has not been satisfactorily ascertained ; 
 but crystalline calcareous beds, portions of which appear to be pure dolomite, 
 with small scales of mica, a few small grains of serpentine, and thin reticulat- 
 ing strings of magnetic iron ore, are found at the village on the south side of 
 the ridge, while black or dark bluish calcareoua*and pyritiferous schist is found 
 to the north of them, both of these usually exhibiting a northward dip. 
 
 On the fourth and fifth lots of the fifth range, still farther north, another 
 band of conglomerate occurs, associated with fine grained soft micaceo- 
 siliceous feldspathic schist. The matrix of the conglomerate weathers white, 
 and appears to be a dolomite. The pebbles, of which the largest may be 
 six inches in diameter, are chiefly quartz, but there are also pebbles or 
 masses of feldspar, and a few of calcspar. The quartz pebbles are for the 
 most part distinctly rounded, and their colors various, some being internally 
 bluish, some white, and others pinkish. The feldspar is red and white, and 
 the calcspar white. The dip of this rock appears to be southward of east, 
 but the slope is irregular, and may probably be thirty-five or forty degrees. 
 The beds may be a repetition of the conglomerate of Madoc village on the 
 opposite side of a synclinal. 
 
 It has been stated above, that in great vertical thicknesses of the Lau- 
 rentian rocks the chief constituent mineral is a triclinic feldspar, varying in rf 
 composition from andesine to anorthite. These anorthosite rocks in general 
 weather opaque white, and they are usually marked by the presence of 
 hypersthene and ilmenite. Sometimes, as in the township of Morin, they Triclinic feid 
 consist chiefly of labradorite. In this locality the rock is composed of a dorite^ypei 
 fine grained white-weathering feldspathic paste, of a purplish grey, and Athene, and 
 holding cleavable masses of a lavender-blue feldspar several inches in in 
 diameter. Many of these exhibit a fine golden-green and deep blue 
 opalescence, and the same hues occasionally emanate from points in the 
 paste. The rock is generally massive, and it is occasionally very difficult 
 to find any indication of those parallel planes which are so generally 
 present in the orthoclase gneiss. The large cleavable masses of labradorite, 
 however, as well as the hypersthene and ilmenite which occur in the rock, 
 are found to prevail in belts that appear to be parallel with one another, 
 and garnetiferous and pyroxenic micaceous bands occasionally indicate the 
 same arrangement. To these anorthosites belongs the hypersthene rock of 
 northern New York and of the isle of Skye. The hypersthene is .however 
 often replaced by ordinary pyroxene, or is wholly wanting in the Lauren- 
 tian system, giving rise to a purely feldspathic rock. 
 
 At St. Jer6me a belt of the crystalline limestone was found to exist on 
 the west side of the river. It was traced along its bank for a distance of a 
 
 c 
 
34 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. III. 
 
 St. Jerome ; 
 anorthosite 
 and ortho- 
 el ase gneiss. 
 
 Terrebonne. 
 
 Chateau Ri- 
 cher; ande- 
 eine. 
 
 mile and a half, bearing N. 12 E., with a breadth of apparently about 
 200 yards. The rock on the east side of it is composed to a large extent 
 of triclinic feldspar ; but holding a considerable admixture of other 
 minerals, it is not of so conspicuous a character as the anorthosite of 
 Morin. The minerals have a reticulated arrangement, as in the case 
 of the porphyroid orthoclase gneiss. Darker and lighter bands run 
 parallel to one another, the shades being occasioned by the greater or less 
 abundance of a fine grained greenish feldspar, weathering opaque white, 
 which occurs in spots surrounded by a darker colored net work, consisting 
 of dark green pyroxene and magnetic iron ore, with small disseminated clus- 
 ters of yellowish-red garnets. In this mixture large and small masses of 
 labradorite, some of them two or three inches in diameter, are irregularly 
 disseminated, and irregular veins or apparent segregations occur here and 
 there, composed of flesh-red orthoclase and translucent colorless quartz. 
 
 On the west side of the river, rock of a similar character is met with ; 
 but there is also seen an interstratified mass of reddish hornblendic gneiss, 
 the feldspar of which is orthoclase. The breadth of the mass is 200 
 yards, and it is marked by bands darker than other parts, from the presence 
 of more hornblende. Iron pyrites and molybdenite are observed in the 
 rock. On the west side of this mass of orthoclase gneiss, smaller bands of 
 a similar nature seem to alternate with those containing a triclinic feld- 
 spar, indicating a passage between the anorthosite and the orthoclase 
 gneiss. Beds of quartzite are also interstratified, and some of these were in 
 one place so filled with small garnets as to form a fine granular garnet rock. 
 The strike of the masses on each side of the limestone runs with it N. 12 
 E., and all dip to the westward at a high angle. 
 
 An anorthosite rock, resembling that of Morin in its opaque white massive 
 aspect, occurs at New Glasgow on the Achigan, in Terrebonne sei- 
 gniory ; the stratification, however, is well marked by bands of garnets and 
 pyroxene, and on the west side, by alternations of the rock with ortho- 
 clase gneiss. The strike is a little eastward of north, with a dip to the west- 
 ward, and the breadth which has been observed is about three quarters of 
 a mile, without, however, attaining the eastern limit of the belt. Similar 
 rocks have been observed in Rawdon and Chertsey, where they appear 
 to have a breadth of twelve miles. 
 
 A large development of triclinic feldspar rock occurs on the Sault a la 
 Puce, in the parish of Chateau Richer (Montmorenci), where it covers 
 a breadth of two or three miles across the strike, bounded by crystalline 
 limestone on one side and a quartzo-feldspathic rock on the other, resem- 
 bling the orthoclase gneiss. In this region there are several varieties of 
 the feldspar, in which the composition varies much, being sometimes that of 
 labradorite, andesine, and intermediate varieties, and at others approaching 
 that of anorthite. Hypersthene is met with throughout the rock in broad 
 
CHAP. III.] LAURENTIAN SYSTEM. 35 
 
 lamellar masses, which, though variable and irregular in their distribution, 
 exhibit a general parallelism. They are occasionally four or five inches 
 in diameter, by an inch or more in thickness. Titaniferous iron ore is also 
 found in the rock in grains and lenticular masses, occasionally an inch or 
 more in thickness. These occur in the granular base, generally near the 
 hypersthene ; but grains of the ore are occasionally found in the crystalline 
 feldspar. The hypersthene does not exceed a half per cent, and the titan- 
 iferous iron one per cent, of the mass. The latter mineral, however, in 
 other localities, may present a much larger proportion. In the parish of St. 
 St. Urbain, near Bay St. Paul, there is a mass of it ninety feet in width Umemte - 
 by about 300 feet in length, in a rock which is probably a continuation of 
 that of Chateau Richer. 
 
 Such are the chief varieties of rock composing the strata of the Lau- 
 rentian series as far as known ; there are other varieties to be noticed, 
 constituting veins and intrusive masses. The rocks composing the veins 
 are in general much more coarsely crystalline than those of the strata ; 
 but some of the more coarsely crystalline masses appear to coincide with 
 the strata, and it cannot yet be stated with certainty whether they are not 
 to be considered as part of them. Some of them have been casually 
 alluded to already in the description of the stratified masses, being those 
 composed of large cleavable masses of pyroxene, orthoclase, calcspar, and 
 mica, with apatite, sphene, and pyrites. There are masses however of a 
 somewhat similar character, which run transverse to the strata, and there 
 can be no doubt that these are to be considered veins of segregation. 
 
 One of this description occurs at the Ragged Chute, near the High veins of p yr - 
 Fall, on the Madawaska, in Blythfield. It has a breadth of not less than 
 150 feet ; its course is about N. 40 E., being transverse to the strata, 
 which consist of crystalline limestone, alternating with orthoclase gneiss. 
 The vein appears to be chiefly composed of pyroxene of a dull whitish- 
 green, associated with dark green hornblende, calcspar, mica, orthoclase, 
 quartz, and black tourmaline. The pyroxene constitutes the great body of 
 the vein ; its crystals are confusedly aggregated, and sometimes radiating 
 smooth cleavage faces, six inches in breadth, may be followed for a length 
 of fifteen inches or two feet. In the vicinity of Grenville there occurs Grenviiie, 
 in a micaceo-graphitic limestone, a coarsely crystalline rock composed of 
 orthoclase, wollastonite, dark green pyroxene, sphene, graphite and quartz, 
 with small quantities of serpentine, zircon, idocrase, and mica. 
 
 Veins are frequently met with composed chiefly of orthoclase in large Granite veins 
 cleavable masses, mingled with quartz, constituting a pegmatite, which, by J^^j^' 
 an admixture of mica, often passes into granite. One of this kind occurs and zircon, 
 on Allumette Lake, at Montgomery's clearing, about five miles above 
 Pembroke. The feldspar is a brownish-red orthoclase, and the quartz, 
 which is white, is in some parts so disposed in the feldspar as to imitate the 
 
36 GEOLOGY OF CANADA. [CHAP. III. 
 
 characters of Hebrew writing, making a graphic granite. Large crystals 
 of brown and black mica occur in the vein, but they are rare. The 
 breadth of the vein is from fifty to one hundred feet, and its course N. 70 
 W., which is transverse to the strike of the strata. 
 
 In the Roche Fendue channel of the Ottawa, in the township of Ross, at 
 the mouth of a deep recess, a vein of a similar character occurs. Crystals 
 of tourmaline were observed in parts of it, but no mica. Its breadth is nine 
 feet, and it stands up like a wall above the gneiss, nearly in the direction of 
 the strike, its course being N. 13 E., with an underlie to the eastward. 
 The dip of the strata is about S. 80 E. < 16. Another instance of a 
 granite vein holding crystals of tourmaline occurs at Carrying-place Bay, 
 on Charleston Lake, in the northern concessions of Escott and Lans- 
 downe. 
 
 On the west side of the river, at St. Jerfone, interstratified orthoclase 
 and labradorite rocks are cut by veins of a granite composed of very pale 
 flesh-red orthoclase, weathering white, and translucent colorless quartz, with 
 occasional crystals of dark brown mica. One of the veins is large and 
 very coarse grained, and they are all more or less characterized by the 
 occurrence of black tourmaline, and small zircons. 
 
 Aibitic Other veins intersecting the Laurentian rocks are composed of an 
 llte ' i albitic granite. One of these occurs on the nineteenth lot of the ninth 
 range of Bathurst, where the albite in part is that highly beautiful 
 opalescent variety which constitutes the peristerite of Thompson. A 
 mixture of cojorless transparent quartz is disseminated through a large 
 portion of the albite, which still so far predominates as to give a distinct 
 feldspar cleavage to considerable masses. 
 
 Another vein of this description is met with at Eel Creek, on the north 
 side of Stoney Lake, in Dummer, where the strata consist of white crystal- 
 line limestone, alternating with blackish-grey schistose gneiss, dipping S. 
 87 W. < 18. The strata are intersected by a set of parallel dykes or 
 veins of pale flesh-red syenite, the largest about three feet thick ; their 
 general course is about N. 18 E., and their underlie S. 72 E. < 45. 
 These are again cut by veins of a fine grained mixture of quartz and red- 
 dish-white albite, some of the albite being in large cleavable masses, 
 exhibiting a bluish opalescence. The vein holds occasional masses of fine 
 granular tourmaline, and is slightly calcareous in parts. 
 
 A third locality, presenting a rock of this description, probably in a vein, 
 is at the head of the Lake of Three Mountains, about forty miles up the 
 River Rouge, where masses of pure white albite, several feet in diameter, 
 and showing large striated cleavage surfaces, are mingled with masses of 
 translucent colorless quartz, some of them a foot in diameter, and large 
 crystals of greenish-brown and black mica. None of this albite was observed 
 to be opalescent. The strata in contact with the mass are crystalline 
 
CHAP. III.] LAURENTIAN SYSTEM. 37 
 
 limestone. In some localities orthoclase and albite are associated in the 
 same mass of granite. We conceive these feldspathic veins to be segregated 
 and not intrusive. 
 
 Pistachio-green epidote very frequently runs hi thin reticulating veins 
 in the orthoclase gneiss ; and when the feldspar of the gneiss is red, the gneis8 ' 
 mixture produces a beautiful ornamental stone. A locality of such gneiss 
 occurs in Ramsay, near Carleton Place, and another at the lowest fall of the 
 Mingan River, on the north shore of the Gulf of St. Lawrence. Where 
 veins of this description occur, the rock of the country appears to be 
 slightly shattered for a certain breadth in a particular direction, but its 
 fragments are very little displaced, and the epidote, without any other 
 mineral, runs in a net-work through the part affected by the disturbance. 
 
 Metalliferous lodes are occasionally found intersecting the Laurentian Metalliferous 
 rocks. The ores which have been met with in them are those of lead and lodes ' 
 copper, in the forms of galena and copper pyrites. These veins have 
 usually been found to intersect the crystalline limestones, in bearings 
 approaching northwest and southeast. The gangue, which holds the ores, 
 is usually either calcspar or barytes, or a mixture of both. The quantity 
 of copper in these veins appears as yet to be but small ; but the lead hi 
 some of them may be found profitable. Instances of those holding traces of 
 copper ore are met with in crystalline limestones, in the townships of MacNab 
 and Bastard, and in the augmentation of the seigniory of Lanoraie and 
 d'Autraye on the Assumption River, where the rock of the country is 
 micaceous gneiss. Veins holding lead ore are known in Bedford, Lans- 
 downe, and Fitzroy. They all intersect the crystalline limestone ; but it has 
 recently been ascertained that the age of these veins is much more recent 
 than the Laurentian epoch. 
 
 Some veins containing the magnetic and others the specular oxyd iron ores, 
 of iron have been met with in the Laurentian rocks, but they are of little 
 importance. One of the former occurs in Ross, opposite Portage du Fort, 
 ha which the magnetic oxyd appears in reticulating strings, transverse to 
 the strata of the crystalline limestone at the spot. The micaceous specular 
 oxyd occurs in what appears to be a vein at Hudson's Wharf, on the Lac 
 des Chats, at the junction of limestone and gneiss. The great iron deposits 
 of the system are in beds. 
 
 The intrusive masses of the Laurentian series consist chiefly of syenite intrusive 
 and greenstone. They occur in many parts of the country, but their rc 
 relative ages have been ascertained almost altogether by investigations in 
 the counties of Ottawa and Argenteuil. What appear to be the oldest 
 intrusive masses are a set of dykes of a rather fine grained dark greenish- 
 grey greenstone or dolerite, which weathers greyish-white, and consists of 
 greyish-white feldspar mixed with pyroxene, occasional scales of mica, and 
 grains of pyrites. Their width varies from a few feet to a hundred yards, 
 
38 GEOLOGY OF CANADA. [CHAP. III. 
 
 and they possess a well marked columnar structure. Their general bearing 
 appears to approach east and west, but the main dykes occasionally divide, 
 a branch striking off at an angle of from twenty to forty degrees. 
 
 One of these dykes cuts crystalline limestone on the thirteenth lot of the 
 fourth range of Grenville. Its breadth is about thirty yards, and it has 
 been traced across the limestone and gneiss for a mile and three quarters, 
 in which, with a few moderate zig-zags, it maintains a course of N. 85 E., 
 until it is interrupted by a mass of syenite on the eighth lot of the range 
 already mentioned. Across the limestone it forms a ridge ; but across the 
 gneiss it is usually found in a depression, sometimes a very deep one. 
 When it mounts the side of any hill which runs with the stratification, the 
 columnar structure gives it the aspect of a flight of gigantic steps, well 
 presenting the character from which the Swedish name of trap is derived. 
 The columns are so truly at right angles to the plane of the dyke that they 
 are a sure means of determining the underlie, which is towards the north. 
 A branch strikes off from the dyke on the eleventh lot of the range, and, 
 after proceeding about a quarter of a mile in the direction S. 30 E., it 
 turns S. 50 E., and continues for three quarters of a mile more, chiefly 
 across limestone, in a remarkably straight line, to the eighth lot, where, 
 having gradually diminished from the width of eighteen yards to five, it 
 seems to split up into a brush-like arrangement of small dykes, and is lost. 
 In a westerly direction from the thirteenth lot of the fourth range, the 
 main dyke has been traced between four and five miles, and in its whole 
 course from the syenite the bearing is about five degrees north of west. 
 
 Another dyke of the same character, with a width of twenty-five yards, 
 occurs in the eleventh lot of the fifth range of Grenville, and runs for about 
 a mile in the bearing N. 67 E., when it is interrupted by the same 
 mass of syenite as before, on the eighth lot of the same range. A probable 
 continuation of the dyke in an opposite direction is seen crossing the gneiss 
 on the fifth range, reaching the seventeenth lot, with a bearing N. 75 W., 
 and thence crossing the River Rouge. 
 
 From the sixth lot of the fourth range of Chatham Gore, where it cuts 
 the crystalline limestone, another of these dykes has been traced for 
 upwards of two miles to the first lot of the third range of Wentworth. Its 
 width varies from fifty to a hundred yards, but it appears to maintain a 
 very uniform course, and though an interval of seven miles is a long one 
 at which to recognise it again, yet an exposure of greenstone on the front 
 of the first range of Wentworth on the division between the twentieth and 
 twenty-first lots is sufficiently near the line to make it probable that it is a 
 continuation of the same dyke. At the latter spot it is from 110 to 120 
 yards wide, and about eleven chains to the westward it is cut off by the 
 syenite. It has been met with again, however, on the western side of it, 
 and traced across the north-west corner of Chatham into Grenville, and is 
 
CHAP. III.] LAURENTIAN SYSTEM. 39 
 
 probably continued to the twelfth lot of the ninth range of the latter town- 
 ship, where there is a dyke of the same character. The whole distance 
 from Chatham Gore is about fifteen miles, and the bearing about five 
 degrees south of west. 
 
 Still another of these dykes has been observed in the seigniory of Argen- 
 teuil, about a mile and a half from the North River, on the road from 
 Lachute to Chatham Gore. It appears to be about twenty-five or thirty 
 yards wide, and it bears N. 80 W. for about a mile and a half to the 
 town line of Chatham, which it crosses towards the rear of the ninth 
 range ; and although it would require a change in its course to bring it to 
 a dyke seen on the road between the seventh and eighth ranges on the 
 ninth lot, it appears probable that the two will be found to be the same. 
 Running westward from the latter spot, it comes against the syenite in 
 the eleventh lot of the seventh range, and is there cut off. 
 
 These greenstone dykes being always interrupted by the syenite when Doientes cut 
 they have been found to come in contact with it, it is plain the syenite y syer 
 must be of posterior date. This mass of intrusive syenite occupies an area 
 of about thirty-six square miles in the townships of Grenville, Chatham, 
 and Wentworth, and a glance at the accompanying map, shewing the dis- 
 tribution of the crystalline limestone in the counties of Ottawa and Argen- 
 teuil, will shew its shape and distribution. In its lithological character the 
 rock is very uniform, being composed for the most part of orthoclase, either 
 of some tinge of flesh-red or a dull white, with black hornblende, and a 
 rather sparing quantity of greyish vitreous quartz. The red tinge prevails 
 more on the west side, the white on the east. In the spur which runs into 
 Wentworth, mica is occasionally found accompanying the hornblende. 
 The rock is rather coarse grained in the main body, but dykes of it are 
 sometimes observed cutting the limestone and gneiss, in which the grain 
 is finer : these have not as yet been traced to any great distance from the 
 nucleus. 
 
 The syenite is cut and penetrated by masses of a porphyritic character, reisite porphy 
 which are therefore of a still later date. These masses belong to what has 
 been called felsite porphyry, hornstone porphyry, or orthophyre, having a 
 base of petrosilex, which may be regarded as an intimate mixture of 
 orthoclase and quartz, colored by oxyd of iron, and varying in colors from 
 green to various shades of black, according to the oxydation of this metal. 
 Throughout the paste, which is homogeneous and conchoidal in its fracture, 
 are disseminated well defined crystals of a rose-red or flesh-red feldspar, 
 apparently orthoclase, and, although less frequently, small grains of nearly 
 colorless translucent quartz. The larger masses of this porphyry have a 
 fine grained reddish-buff base, in which well defined crystals of flesh-red 
 feldspar of various sizes, from one-eighth to three-eighths of an inch, are 
 thickly disseminated. In addition to the crystals of feldspar, the base 
 
40 GEOLOGY OP CANADA. [CHAP. III. 
 
 often contains a multitude of fragments of gneiss, greenstone, and syenite > 
 varying in size from small grains to masses several feet in diameter. 
 These are occasionally so abundant as to give to the rock the character of a 
 breccia. When the base is green it is rather more compact, and it does 
 not usually contain so many imbedded crystals of feldspar. 
 
 The principal nucleus of this porphyry occupies a pear-shaped area, the 
 nucleus and sma ii en( j pointing south, on the third and fourth lots of the fifth and sixth, 
 ranges of Grenville, from which, on the eastern side, a portion projects 
 into the second lot of the fifth range. This mass is wholly surrounded by 
 syenite, and a large part of it constitutes a mountain or group of hills inter- 
 sected by one or two ravines. In about the centre of the mass on the 
 summit of one of the hills, there is a circular depression of about a hundred 
 yards in diameter, nearly surrounded by a tufaceous porphyritic rim of 
 about thirty feet in height. In this depression there is a turf bog 
 supporting a grove of good sized evergreen trees. On sounding the depth 
 of the bog with a boring rod, the rock beneath was found to present the 
 shape of a cup, with the depth of twenty-five feet in the centre ; so that, 
 including the rim, the depression would be about fifty feet deep, with the 
 exception of a break down to the level of the bog on the east side. The 
 nature of the rock constituting the rim gives to the depression in some 
 degree the aspect of a small volcanic crater. But if it be the remains of 
 one, it can only represent some deep-seated part of the vent ; for there can 
 scarcely fail to have been here a great amount of denudation of the ancient 
 Laurentian surface, while the ice grooves in the neighborhood shew that 
 there has been much erosion over the whole country in comparatively recent 
 times. In this vicinity some entangled beds of gneiss occur, one of which, 
 running N. 80 W. for upwards of a hundred yards, is completely sur- 
 rounded by the porphyry. 
 
 From this porphyritic nucleus one or two porphyritic dykes can be traced 
 cutting the syenite for short distances, and some of a similar character are 
 met with at such a distance as to make it probable that there are other 
 porphyritic nuclei. One of these dykes about seven yards wide, con- 
 taining beautiful red feldspar crystals set in a black base, occurs on 
 the south side of the road, between the seventh and eighth ranges of 
 Chatham, on the eighth lot. Its bearing S. 85 W. would carry it to 
 the south of the porphyritic mass above described, from which the position 
 in which the dyke cuts the gneiss is removed seven miles, though it is not 
 more than one mile from the syenite. 
 
 Another dyke of this aspect is seen in the ninth range near the line 
 between the thirteenth and fourteenth lots, but in addition to the elements 
 mentioned it holds disseminated grains of transparent colorless quartz. 
 Its course appears to be S. 44 W.,and it intersects a mass of porphyritic 
 rock of the same color and texture as the porphyry of the pear-shaped 
 
CHAP. III.] LAURENTIAN 'SYSTEM. 41 
 
 nucleus, which, however, like the dyke, contains grains of vitreous quartz. 
 Grains of this mineral are also observed in another porphyritic mass, 
 whose course is N. 10 W., about a quarter of a mile from the front of 
 the twenty-fifth lot in the seventh range. A porphyritic dyke is 
 observed on the road between the sixth and seventh ranges on the twenty- 
 third lot. It encloses grains of quartz and crystals of flesh-red feldspar, 
 some of them half an inch in diameter, in a reddish finely granular base. 
 Of the tufaceo-porphyritic rock a lenticular mass crosses the seventh 
 and eighth lots close upon the rear of the fifth range of Grenville. It has 
 a length of nearly half a mile by a breadth of about 150 yards in the 
 middle, and lies between gneiss on the north and syenite on the south. 
 
 In the vicinity of the pear-shaped porphyritic intrusion there are met veins of 
 with two veins of a special character, cutting the syenite, that deserve to 
 be noticed. They consist of a white, yellowish-brown or flesh-red cellular 
 chert, the colors in some cases running in bands parallel to one another, 
 and sometimes being rather confusedly mingled, giving the aspect of a 
 breccia. The cells are unequally distributed, some parts of the veins being 
 nearly destitute of them, while in others they are very abundant, and of 
 various sizes from that of a pin's head to an inch in diameter. On the 
 walls of some of these cells small transparent crystals of quartz are im- 
 planted, and in some there are the impressions of cubical forms, resulting 
 probably from crystals of fluor spar which have disappeared. The stone 
 has the chemical characters and the composition of flint or chalcedony. 
 
 One of these veins is on the north half of the first lot of the sixth range 
 of Grenville, where it was traced for about a hundred yards running about 
 east and west, and the other in the south half of the first lot of the sixth 
 range, belonging to Mr. James Lowe, who was the first person who drew 
 attention to it as affording buhrstone. On his ground the vein has been 
 more examined than elsewhere ; it appears to run in a very straight 
 nearly east and west bearing, and stands in a vertical attitude, while its 
 breadth varies from about four to seven feet. Where the vein is banded 
 the colors run parallel with the sides. The attitude and associations of the 
 mass clearly shew it cannot be of sedimentary origin, and its composition, 
 taken in connection with the igneous character of the district, suggests the 
 probability that it is an aqueous deposit which has filled up fissures in the 
 syenite, and is similar in its origin to the agates and chalcedony which, in 
 smaller masses, are common in various rocks. 
 
 For a distance of perhaps 200 yards on each side of these veins of chert, 
 while the quartz of the syenite remains unchanged, the feldspar has been 
 more or less decomposed, and been converted into a sort of kaolin. Aa 
 this process involves a separation of silica from the feldspar, it is not 
 improbable that it has been the source of the veins of chert. 
 
42 GEOLOGY OF CANADA. [CHAP. III. 
 
 Ages of these The intrusive rocks which have been described have a date anterior to 
 
 intrusi 
 rocks. 
 
 the deposit of the Silurian series. None of a similar character have been 
 
 met with breaking through this series, and the relations of the base of the 
 Lower Silurian group along the foot of the hills composed of the syenite 
 are such as to make it evident that the Silurian beds in some places overlie 
 eroded portions of the intrusive rock. But all these intrusive masses are 
 cut by a set of dykes whose relations to the Silurian series are not so 
 certain. These dykes are composed of a finely granular base, with an 
 earthy fracture, consisting of feldspar and pyroxene, and having a dark 
 brownish-grey color. In this base are imbedded rounded masses of black 
 cleavable augite, varying in size from a pin's head to several inches in 
 diameter. These are associated with various sized nodules of calcspar 
 filling cells that do not attain the diameter of the largest masses of augite, 
 and with small scales of mica, grey in fresh fractures, but weathering brass- 
 yellow on the sides of cracks and joints. Small crystals of sphene and 
 grains of titaniferous iron occur in the rock. 
 
 One of these dykes, having a width of from three to ten feet, is traced 
 from the first lot of the sixth range of Grenville, near Mr. Lowe's buhrstone, 
 where it cuts the syenite, to the third and fourth lots of the same range, 
 where it cuts the pear-shaped mass of porphyry ; thence it crosses to the 
 eighth lot of the fifth range, where it cuts both syenite and porphyry, and 
 farther to the tenth lot of the same range, where it intersects the quartzite 
 and the limestone. The whole distance is upwards of two miles and a half, 
 and the bearing S. 82 W. Another dyke of this description intersects the 
 limestone on the thirteenth lot of the same range, and is traced for half 
 a mile, running east. These dykes bear a striking resemblance to some 
 of the dolerites which intersect the Lower Silurian group in the neighbor- 
 hood of the mountain of Montreal, and may possibly be of the same age, 
 but none of them have yet been traced continuously from the Laurentian 
 into the Silurian rocks. 
 
 Extent of The description which precedes will give some notion, of the chief rock 
 Laurentian masses O f the Laurentian series. Stretching on the north side of the St. 
 
 system. 
 
 Lawrence from Labrador to Lake Huron, this series occupies by far the 
 larger portion of Canada, and its strata probably possess a very great 
 thickness. To determine the superposition of the various members of 
 such an ancient series of rocks is a task which has never yet been accom- 
 plished in geology, and the difficulties attending it arise from the absence 
 of fossils to characterise its different members. Bands of the crystalline 
 limestone are easily distinguished from bands of the gneiss, but it is scarcely 
 possible to know from local inspection whether any mass of limestone in 
 one part is equivalent to a certain mass in another. They all resemble 
 one another lithologically, and, although masses dipping in the same 
 direction are met with running for considerable distances rudely parallel 
 
CHAP. III.] LAURENTIAN SYSTEM. 43 
 
 with one another, it is scarcely ever safe to take for granted that they are structure of 
 stratigraphically distinct. The dips avail but little in tracing out the 
 structure ; for in the numerous folds of the series the dips are frequently 
 overturned, and the only reliable mode of pursuing the investigation and 
 working out the physical structure is patiently and continuously to follow 
 the outcrop of each important mass in all its windings as far as it can be 
 traced, until it becomes covered up by superior unconformable strata, is 
 cut off by a great dislocation, or disappears by thinning out. A labor such 
 as this, in a district without roads and the topography of which is yet little 
 known, with a surface much broken by the unequal wear of its rocks, and 
 still covered by forest, must necessarily require much time. 
 
 An attempt has been made to work out the structure of a small portion Map of the 
 of the Laurentian country in this way. It comprehends a part of the ^e 8 * 01168 - 
 counties of Ottawa, Argenteuil, Montcalm, and Two Mountains, and the 
 accompanying map displays the distribution of the limestones in that area, 
 as far as known. In this investigation a single band of limestone, which 
 has been termed the Grenville band, varying apparently in thickness from 
 60 to 1000 feet, and averaging perhaps 750 feet, emerging from beneath 
 the Silurian rocks, has been traced from Grenville to the Iroquois Chute, 
 fifty miles up the valley of the Rouge. It presents the general form of a 
 trough, but its distribution is so complicated by subordinate undulations 
 that in a triangular area, of which the base extends about twenty-five miles 
 between the Petite Nation seigniory and Lachute, and of which the apex 
 is at the Iroquois Chute, the line of calcareous outcrop measures upwards 
 of 200 miles. The arrangement presented by the outcrop appears to 
 depend upon two sets of undulations, the axes of the one running in bearings 
 approaching north and south, and of the other in bearings nearly east and 
 west, the latter apparently related to the oldest system of dykes. 
 
 The north and south undulations appear to be the more important and the Ottawa and 
 more numerous of the two, giving to the lines of outcrop in that direction N ' ort ^ River 
 the greater number of repetitions and the longer stretches. For about 
 twenty-five miles from the Ottawa and North Rivers the bearing of these 
 axes is about N. 10 E., and they preserve a considerable degree of 
 parallelism ; but the investigation has not yet been sufficiently extended to 
 determine whether they continue in that direction, or whether they turn a 
 little to the westward of north for some distance in their farther progress, 
 nor is it yet certain in what positions will be found the main axes of the 
 series. The most important anticlinal observed appears to start in Chatham 
 from the intrusion of syenite which has been mentioned, and, crossing the 
 town line of Chatham and Wentworth about half-way between Lake Louisa 
 and the west branch of the North River, to gain a position towards the west 
 side of Howard ; but beyond this its course has still to be ascertained. 
 
 The deepest part of the trough to the westward of this anticlinal, as far 
 
44 GEOLOGY OF CANADA. [CHAP. III. 
 
 as the investigation has proceeded, appears to be around the point where 
 the line between Wentworth and Harrington comes upon the south side of 
 the township of Montcalm. In this neighborhood a bed of limestone, 
 passing through Proctor's Lake, overlies the Grenville band ; but being only 
 fifteen feet thick, it has been traced out no more than two or three miles. 
 On the east side of the axis this bed has not been observed ; but a more 
 important one, supposed to be higher in the series, and to average 500 feet in 
 thickness, has been followed through Howard, Morin, and Mille Isles to St. 
 Jerfone', where it sinks beneath the unconformable Silurian strata. What is 
 supposed to be the same band again emerges about twenty miles to the north- 
 eastward in Rawdon, and runs northward obliquely across the township. 
 
 The synclinal between Rawdon and Mille Isles appears to be occupied 
 by the anorthosite rocks already described as made up of triclinic feld- 
 spars, associated with more or less pyroxene or hypersthene, and gneissoid 
 in their structure. Of this anorthosite there is probably a great vertical 
 thickness ; for although it has been traversed at about right angles to the 
 strike for nearly twelve miles in Rawdon and Chertsey, the summit of it 
 has not been ascertained, nor is it yet known whether it is succeeded in 
 ascending order by limestone or by orthoclase gneiss. Between St. Jerfane 
 and the most eastern exposure of the Grenville band of limestone at 
 Lachute, the anorthosite appears gradually to pass into orthoclase gneiss, 
 and this in its various lithological modifications is the only rock met with 
 above and below the Grenville band of limestone in the triangular area 
 explored up the valley of the Rouge to the Iroquois Chute. 
 
 It has been stated above that for twenty-five miles from the Ottawa the 
 bearing of the axes of the northward anticlinals and synclinals is about 
 N. 10 E. The bearing of the most important synclinal form examined 
 beyond this distance is about N. 10 "VV. Upon it runs a trough-shaped 
 development of the Grenville limestone from the north part of Arundel to the 
 Iroquois Chute, where the limestone seems to come to a point. The widest 
 part of the trough is at Hamilton's farm, on the plain of the Three Mountains, 
 where a section at right angles to it shews two important bands of crystalline 
 limestone coming from beneath the Grenville band on each side, with heavy 
 masses of orthoclase gneiss between. The outcrop of the lower of these 
 two sheets runs through Trembling Lake on the east side and through three 
 small lakes on the west. The upper one passes through Long Lake and Great 
 Beaver Lake on the east, and Green Lake on the west, and it is divided 
 into three subordinate sheets by the interposition of two bands of garnet- 
 bearing gneiss and quartzite. In this part garnet-bearing gneiss overlies 
 the Grenville band, and above it a great bed of quartzite, 600 feet thick, 
 which has already been alluded to, forms Quartz Mountain, an isolated hill 
 which rises from the plain of the Three Mountains. Orthoclase gneiss rises 
 from beneath these three bands of limestone on each side of the trough, 
 
CHAP. III.] LAURENTIAN SYSTEM. 45 
 
 and on the east side it constitutes Trembling Mountain, the highest hill 
 for some distance around, being, as mentioned in a previous chapter, about 
 2060 feet above the sea. 
 
 From what has been said, it will be observed, that in the present state of FourUme- 
 the investigation, without counting the Proctor's Lake bed, which is too small 8tono bands< 
 for separate consideration, there appear to be four important bands of 
 crystalline limestone in the Laurentian area of which the structure has 
 been partially examined. The wrinkled condition of the strata is such 
 that there are in some parts four and five anticlinals in the breadth of a 
 mile, the effect of each of which is perceptible in the geographical distri- 
 bution of the strata, and this renders it very difficult to determine with 
 precision the volume of rock in which the four calcareous bands are 
 inclosed ; but according to the best estimate arrived at, it appears probable 
 that the following would be an approximation to the thickness of the various Section, 
 constituent parts of the mass arranged in ascending order : 
 
 Feet. 
 
 1. Orthoclase gneiss composing Trembling Mountain ; though the mass has not 
 
 been especially examined nor any geographical position shewing its inferior 
 limit ascertained, yet the general aspect of the mountain induces the suppo- 
 sition that it must be of great thickness, and it is presumed that it will 
 exceed the volume here given, 5000 
 
 2. Crystalline limestone of Trembling Lake, 1500 
 
 3. Orthoclase gneiss between the limestone of Trembling Mountain and that of 
 
 Great Beaver Lake, 4000 
 
 4. Crystalline limestone of Great Beaver Lake and Green Lake, including two 
 
 bands of interstratified garnetiferous rock and hornblendic Orthoclase 
 gneiss, which may equal half the amount, 2500 
 
 5. Orthoclase gneiss intermediate between the limestone of Great Beaver Lake 
 
 and Long Lake, and the Grenville limestone on the Rouge at the Iroquois 
 Chute, the lower part having several bands of garnetiferous gneiss and 
 quartzite, and the upper part much coarse grained porphyroid orthoclase 
 gneiss, 3500 
 
 6. Crystalline limestone of Grenville, in some parts interstratified with a band of 
 
 gneiss. The thickness appears to vary from about 1500 feet to 60 feet, and 
 may be estimated at about 750 
 
 7. Orthoclase gneiss between the limestone of Grenville and Proctor's Lake lime- 
 
 stone, 1580 
 
 8. Proctor's Lake limestone, 20 
 
 9. Orthoclase gneiss passing gradually into anorthosite between Proctor's Lake 
 
 limestone and the Morin band. This would probably include the quartzite 
 of the Quartz Mountain, the orthoclase gneiss above it, and the gneiss of 
 
 passage, 3400 
 
 The nearest geographical approach of the Grenville and Morin limestones 
 that has been ascertained is about two miles ; the present estimate of their 
 stratigraphical separation is 5000 feet, which is not perhaps extravagant. 
 
 10. Anorthosite above the Morin band of limestone ; the thickness is wholly 
 
 conjectural, 10000 
 
 32750 
 
46 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. III. 
 
 Anorthosites 
 
 st. John. 
 
 Labrador. 
 
 How this portion of the series is related to the rocks displayed in other 
 P ar ^ s f the Laurentian area, is yet unknown. As already stated, 
 a considerable breadth of anorthosite rock occurs at Chateau Richer. 
 This rock has also been met with in the parish of St. Urbain in the seigniory 
 of Beaupre*, and it appears to be largely developed on the Saguenay 
 between Chicoutimi and Lake St. John. Its strike there coincides with 
 the bearing of the river, and its breadth extends to the valley of Lake 
 Kinogami. Much of this rock in the immediate vicinity of Lake St. John 
 and in its tributary the Peribonka is of a dark violet-blue color, approaching 
 to black, and is almost entirely made up of a cleavable triclinic feldspar, 
 often having the characters of labradorite. This species takes its name from 
 Labrador, where it was first discovered, and appears to characterize por- 
 tions of the Laurentian series across the whole breadth of the province 
 Lake Huron, to Parry's Island on Lake Huron, where labradorite rock was observed in 
 place by Dr. Bigsby. Anorthosite rocks were observed by Prof. Hind 
 forming a range of hills on the Moisie River, and, from the specimens 
 brought thence by Mr. Cayley, appear to constitute a part of the Seven 
 Islands, where they were long ago remarked by Bayfield ; but whether 
 in any or all of these localities the strata are equivalent to the anorthosite 
 rocks of Mille Isles and Rawdon, can for the present be only conjectural. 
 Crystalline limestone is interstratified with orthoclase gneiss at the Falls 
 of St. Fe're'ol on the Ste. Anne (Montmorenci), and at Cape Tourmente. 
 Exposures of the rock are said to continue for fifty miles up the valley of 
 the Rouge above the part examined and described. On the north side of 
 the Ottawa the rock is met with in many places in considerable masses as 
 far as the Deep River, but none of it has been seen between that and Lake 
 Temiscamang. In the rear of Kingston a thick band of it, associated with 
 dolomite, and including orthoclase gneiss, has been traced northward for 
 twenty miles through the townships of Loughborough and Bedford, and partial 
 examinations have been made of exposures of the rock occurring at inter- 
 vals all the way from Loughborough to Balsam Lake. Between the Ottawa 
 and Lake Huron, crystalline limestone is largely developed on the Missis- 
 sippi, the Madawaska, and the BonnechSre, but none of it was seen on an 
 exploration up the Muskoko and down the Petewahweh. The garnet-bear- 
 ing gneiss, however, so frequently found in the vicinity of the limestones, 
 occurred in several parts of the Muskoko ; but on the Petewahweh the most 
 conspicuous masses, independent of orthoclase gneiss, consisted of intrusive 
 syenite, which in many parts appeared to be decomposing into a brick-red 
 soil. A band of crystalline limestone crosses the Meganatawan about thirty- 
 five miles from its mouth, and has been traced for about two miles in a 
 northerly bearing. Limestone occurs at the exit of Lake Talon on the 
 Mattawa, and in two places on Lake Nipissing ; one in a group of 
 islands at the extreme eastern end of the lake, and the other in Iron 
 
 Laurentian 
 
 in Western 
 Canada. 
 
CHAP. III.] LAURENTIAN SYSTEM. 47 
 
 Island, where the limestone is associated with specular oxyd of iron in 
 considerable quantity, accompanied by fluor spar. On the other hand the 
 Laurentian limestones have been observed by Mr. Blaiklock on the Mistia- 
 shini more than 100 miles north of Lake St. John. North of the Mattawa, 
 Lake Nipissing, the French River, and the shore of Lake Huron to She- 
 bahahnahning, the country has not yet yielded any exposures of crystalline 
 limestone, and all its Laurentian rocks appear to be varieties of orthoclase 
 gneiss. At the falls of the Recollet on the French River there occurs an 
 intrusive syenite, weathering to a brick-red earth similar to the rock on the 
 Petewahweh ; but the extent of the area which it occupies has not been 
 ascertained. 
 
 The area occupied by the Laurentian series in Canada, as already stated, Area and dis- 
 is supposed to be about 200,000 square miles. Its northern limit has not L^^f the 
 yet been satisfactorily ascertained, though it is supposed, from Lake Nipis- system, 
 sing eastward, to be beyond the boundary of the province. The southern 
 limit is well known : with the exception of a narrow border of Silurian 
 strata on the strait of Belle Isle, another at the mouth of the Mingan River, 
 and a third near the Seven Islands, with the addition of two narrow Silu- 
 rian strips running a few miles up the Murray Bay River and the Gouffre, 
 the north shore of the St. Lawrence is the southern boundary of this ancient 
 series of deposits from Labrador to Cape Tourmente. The distance is 
 about 600 miles ; in the first half the bearing is about west, and in the 
 second about south-west. In the next 200 miles the boundary runs about 
 west-south-west, and is distant from the St. Lawrence about thirty miles 
 in the rear of Montreal. Beyond this for a hundred miles it follows the 
 Ottawa, in a bearing more nearly west, with a narrow strip of Silurian rocks 
 between it and the margin of the river for the chief part of the distance. 
 Turning southward at the upper end of Lac des Chats, it runs in a very 
 irregular line between that lake and the St. Lawrence, which it again 
 reaches at the Thousand Islands, presenting in the interval several points 
 projecting into the Lower Silurian plain to the eastward. From the Thou- 
 sand Islands the Canadian part of the boundary runs in a pretty straight 
 line a little north of west to Matchedash Bay on Lake Huron, but, as has 
 already been stated, from the Thousand Islands the formation expands into 
 an area of 10,000 square miles in New York, the boundary of which has 
 been given. From Matchedash Bay the east and north shores of Lake 
 Huron complete the southern boundary, which terminates at Shebahah- 
 nahning. The western boundary, which is but imperfectly known, runs 
 about north-east from the place last named, and reaches the Wahnapitae 
 River about forty miles north of Lake Huron, from the mouth of the French 
 River. It follows the upward course of the Wahnapitae for about fifteen 
 miles, and continues its north-eastward course to the Sturgeon River, 
 reaching it at its junction with the Maskanongi. From this it gains Lake 
 
48 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. III. 
 
 Gneiss ot 
 Lake Supe- 
 rior. 
 
 Supposed 
 ibs*iils in the 
 Laurentian 
 limestones. 
 
 Temiscamang, three miles below the united mouths of the Metabechouan 
 and Montreal Rivers, and follows the west side of the lake for fourteen 
 miles ; it gains the east side about three miles above the point opposite to 
 those rivers, and follows this side to the head of the lake. How far north it 
 may run from this is riot yet ascertained. 
 
 Orthoclase gneiss, resembling that of the Laurentian series, is spread 
 over an area occupying a breadth of about four or five miles on the north 
 shore of Lake Huron, between the Mississagui and Thessalon Rivers. It 
 appears also to come upon a considerable portion of the coast of .Lake 
 Superior, giving place there to higher rocks between Gros Cap and Ma- 
 mainse, at Cape Gargantua, Cape Choyye, and for some distance on each 
 side of the Michipicoten River, as well as for some distance up the stream. 
 Newer rocks run in a narrow strip on the coast a few miles south of Otter 
 Head, and occupy about twenty miles on each side of the bight of Penin- 
 sula Bay, as well as about twenty miles up the Pic River. From this the 
 gneiss continues along the coast of the lake to Neepigon Bay, on the north 
 side of which it leaves a narrow border for the overlying strata. Crossing 
 Neepigon River about seven miles above its mouth, the limit of the gneiss 
 runs in a nearly straight line to the lower part of Thunder Bay, leaving to 
 higher strata the peninsula between Neepigon and Black Bays, and between 
 Black and Thunder Bays. From Thunder Bay it strikes into the land a 
 little north of the Kaministiquia River, and keeps on the north side of it 
 as far as Dog Lake, which is as far as the river has been examined. 
 
 Although the Laurentian rocks have hitherto been considered azoic, 
 certain forms strongly resembling fossils were discovered three years since 
 by Mr. John McMullen, then attached to the Geological Survey as an 
 explorer, in one of the bands of limestone belonging to this series at the 
 Grand Calumet. Any organic remains which may have been entombed 
 in these limestones would, if they retained their calcareous character, be 
 almost certainly obliterated by crystallization, and it would only be through 
 the replacement of the original carbonate of lime by a different mineral 
 substance that there would be some chance of the forms being preserved. 
 The specimens obtained from the Grand Calumet present parallel or 
 apparently concentric layers, resembling those of the Stromatopora rugo- 
 *a, except that they anastomose at various points. The layers are com- 
 posed of crystalline pyroxene, while the interstices are filled w T ith crystal- 
 line carbonate of lime. These specimens have called to recollection others 
 which were some years ago obtained from Dr. James Wilson of Perth, and 
 then regarded merely as minerals. They came from loose masses of lime- 
 stone, in that -vicinity, and exhibit similar forms to those of the Calumet 
 composed of dark green concretionary serpentine, while the interstices are 
 filled with crystalline dolomite. If both are to be regarded as the results 
 of unaided mineral arrangement, it would seem strange that identical forms 
 
CHAP. III.] 
 
 LAURENTIAN SYSTEM. 
 
 49 
 
 should be derived from minerals of such different composition. If the 
 specimens had been obtained from the altered rocks of the Lower Silurian 
 series, there would have been little hesitation in pronouncing them to be 
 fossils. Their resemblance to Stromatopora rugosa from the Birdseye and 
 Black River limestone, where this fossil has been replaced by concretionary 
 
 3, 4.6TJPPO8ED FOSSIL FROM LAURENTIAN LIMESTONE, GRAND CALUMET. 
 
 3. "Weathered surface of a specimen, natural size. 
 
 4. Vertical transverse section of 3. 
 
 silica, is very striking. In the specimens from the Calumet the pyroxene and 
 the carbonate of lime being both white, the forms, although weathered into 
 strong relief on the surface, are not perceptible in fresh fractures until 
 the fragments are subjected to the action of an acid, the application of 
 which shews the peculiar structure throughout the mass. 
 
 D 
 
50 GEOLOGY OF CANADA. [CHAP. IV. 
 
 CHAPTER IV. 
 
 THE HURONIAN SERIES. 
 
 SLATE CONGLOMERATE, QUARTZITE. DIORITE. SECTION ON LAKE HURON. SLATES OF LAKE 
 SUPERIOR. ROCKS OF THE THESSALON. JASPER CONGLOMERATE. INTRUSIVE GREENSTONE 
 AND GRANITE. METALLIFEROUS LODES. DISTRIBUTION OF HURONIAN ROCKS. THESSA- 
 1X)N BASIN AND FAULT. ROCKS OF THUNDEB BAY AND THE KAMINISTIQUIA. CONTACT 
 OF LAURENTIAN AND HURONIAN BOCKS. 
 
 siate congio- On Lake Temiscamang the Laurentian orthoclase gneiss is followed 
 by a slate conglomerate. The finer parts of this rock are dark grey, 
 weathering to dark green ; they are of a uniform grain, and, being at 
 the same time argillaceous and silicious, they present the characters of a 
 hard compact slate. Some parts not so fine in texture are a hard dark 
 grey sandstone, weathering to a dingy olive-green. In both cases the 
 rock frequently exhibits the character of a compact conglomerate, holding 
 pebbles and boulders, sometimes a foot in diameter, of the subjacent 
 gneiss, from which they appear to be principally derived. The boulders 
 display red orthoclase feldspar, translucent colorless quartz, green horn- 
 blende, and brownish-black mica, arranged in parallel layers which have 
 a direction according with the attitude in which the boulders were acciden- 
 tally enclosed. Some of the pebbles consist of a dark green feldspathic 
 rock shewing no crystallization, not so hard as most of the others, and 
 giving a white streak. Occasionally thick beds are composed of these 
 green pebbles, enclosed in a fine grained matrix of the same description of 
 material. Sometimes the rock has the semblance of porphyry, appearing 
 to contain opaque white crystals of feldspar ; but these are probably small 
 angular fragments of the mineral. 
 
 In the finer parts of the rock the bedding is sometimes indicated by 
 thin differently colored layers cemented together, without the slightest 
 tendency to cleavage in the bedding. The colors are usually different 
 shades of green, with sometimes the addition of reddish-brown or deep 
 flesh-red and black, giving a very beautiful and regularly striped rock. 
 Another form which the finer parts present is that of a very close grained, 
 compact, dark grey mica slate, cleavable with difficulty in the direction of 
 indistinct lines, and exhibiting on the planes of division, which are not very 
 even, a surface glimmering from the effect of very minute and closely 
 
CHAP. IV.] HURONIAN SERIES. 51 
 
 adhering scales of mica. A transverse fracture shews thin interrupted 
 whitish streaks interlocking among one another, and arising from the 
 presence of quartz. 
 
 Where there is a cleavage or jointed structure in the rock, the planes of 
 division cut evenly and smoothly through the pebbles of the conglomerate 
 without the slightest deflection ; and the pebbles are so thoroughly and 
 intimately united with the matrix, and so similar in hardness, that the blow 
 of a hammer never displaces them, but breaks through them and the 
 matrix as if the rock were perfectly homogeneous. The action of the 
 weather and friction also appear to wear both equally. 
 
 In no part where the rock was observed on the lake is there any 
 cleavage of that perfect kind which would render it fit for roofing slates ; 
 but specimens said to be obtained ^bout five miles up the Montreal River 
 make it probable that it must have such a cleavage in some parts of its 
 geographical distribution. The thickness of the rock has not been ascer- 
 tained ; with a dip of eight or nine degrees it rises into hills of about 400 
 feet in height, and its volume is very probably much more than 1000 feet. 
 
 To this succeeds a quartzite which appears to be of pretty uniform Quartzite. 
 character throughout the whole mass. It is in general of a pale sea-green 
 or greenish-white, weathering to a light yellowish-brown to a depth 
 seldom exceeding a quarter of an inch from the surface. Sometimes 
 it is brownish-green within, and in a few instances of a light grey 
 with spots of green. It appears to be composed of quartz and feldspar, 
 with occasional scales of silvery mica. This rock is in general 
 moderately fine grained, but coarse grained beds are now and then inter- 
 stratified, which approach the character of a fine conglomerate, with 
 pebbles of white translucent quartz. It is a strong and solid rock, resisting 
 well the general influences of the weather, and is generally thick-bedded. 
 The total volume seen of the deposit, as determined by the height of 
 hills which it composes in nearly horizontal layers, is between 400 and 
 500 feet. 
 
 On the Sturgeon, Wahnapitae, and Whitefish Rivers, there is usually 
 interposed between the Laurentian gneiss and the recognised Huronian 
 rocks, a mass of rather coarse grained greenstone or diorite ; but whether 
 this is an overflow constituting the base of the upper formation, or an 
 eruptive mass in the form of a dyke intruded at a later period, has not been 
 ascertained. The Huronian masses which follow the greenstone are fre- 
 quently found to be interstratified with igneous rocks of a similar character, 
 which are sometimes seen to cap the hills where the strata below are nearly 
 horizontal ; but there are also vertical intrusive masses of greenstone which 
 apparently differ from the intercalated layers only hi being generally of a 
 somewhat finer grain. Independent of the greenstones, the members of 
 
52 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IV. 
 
 section on the Huronian series on and near the three rivers mentioned, appear to be 
 Lake Huron. ag f oU(WB j n asce nding order : 
 
 1. Fine grained green silicious strata with thin bands of greenish quartzite interstrati- 
 
 fied ; these appear to be associated with fine grained bluish or black slates, 
 weathering very black, and occasionally with layers of a reddish color. In all 
 these slates copper pyrites and iron pyrites are frequently present. 
 
 2. Slate conglomerate, of which the matrix is always greenish in color ; sometimes the 
 
 matrix has a regular slaty structure, while at other times it resembles a massive 
 fine grained diorite ; it holds pebbles of whitish and red syenite in great profu- 
 sion, with occasional masses of green, brown, and red jasper, all rounded in form ; 
 toward the base of the conglomerate there appear green slates in very regular 
 laminae, cleaving with the bedding, and usually cut by two sets of parallel joints, 
 dividing the rock into rhomboidal forms. 
 
 3. A band of limestone usually much shattered and disturbed, and in general associated 
 
 with greenstone ; the prevailing color of the limestone when found in mass is a 
 pale whitish-grey, sometimes passing into a dark blue ; the band is frequently 
 brecciated, and often displays rough jagged edges, which appear to belong to 
 layers of hornstone ; portions of the band appear to be indurated calcareous shale, 
 and these occasionally contain fine grained silicious pebbles. 
 
 4. Slate conglomerate resembling that on the other side of the limestone ; with this is 
 
 ' associated green silicious slate, similar to that already mentioned, with some toler- 
 ably strong bands of quartzite towards the top. 
 
 5. White and very pale sea-green or greenish-white, close grained quartzite, with beds 
 
 of quartz conglomerate interstratified, and layers of talco-quartzose slate, some- 
 times of a dark green color, but more frequently of a pale flesh-red. The pebbles 
 of the conglomerate are chiefly small white opaque rounded masses of quartz, but 
 these are occasionally mixed with rounded masses of red and green jasper. 
 
 Slates on 
 Lake Supe- 
 rior. 
 
 On Lake Superior the Laurentian gneiss is succeeded by slates, generally 
 of a dark green without, and often dark grey in fresh fractures, which at the 
 base appear occasionally to be interstratified with beds of a feldspathic 
 character, of the reddish color belonging to the subjacent gneiss. Sometimes 
 these beds are a combination of feldspar and quartz, occasionally with the ad- 
 dition of hornblende, and in some of the beds the hornblende, preponderating, 
 gives them a general green color. Some of the beds have the character of 
 diorite ; others that of mica slate, and a few present that of quartzite. 
 Rising in the series the dark green slates become interstratified with layers, 
 holding a sufficient number of pebbles of different kinds to constitute con- 
 glomerates. The pebbles appear to be all derived from altered rocks ; 
 they greatly vary in size in different places, and occasionally measure a 
 foot in diameter. Where the slate conglomerates have been worn by the 
 action of the water, the pebbles are generally worn down equally with the 
 rest of the surface ; and though a very distinct picture of them is presented 
 on such a surface where the water or weather appears to have had an 
 influence in bringing out a well defined contrast in colors between the 
 
CHAP. IV.] HURONIAN SERIES. 53 
 
 pebbles and the slate, at the same time producing a contrast between 
 parallel bands of the slate on the terminal edges of the laminae, it yet 
 often happens, unless the pebbles are of white quartz, that they are very 
 obscurely distinguishable on fracturing the rock, both the pebbles and the 
 matrix having a grey color, and showing very little apparent difference in 
 mineral character. On some of these pictured surfaces small opaque 
 white feldspathic crystals occasionally spot the whole surface of the rock, 
 the pebbles equally with the slaty matrix. The rock has nowhere on the 
 lake been observed to display true slaty cleavage independent of the bed- 
 ding ; but it often exhibits a jointed structure, and the divisional planes 
 cut through the pebbles without the smallest deflection. 
 
 A considerable thickness of these conglomerate or pebbly slates is section of 
 exposed at the mouth of the river Dor, near Gros Cap, about five miles the 8lates - 
 above the mouth of the Michipicoten River. The strike of the rock is 
 very regular, being about east and west, while the dip is very highly 
 inclined, the beds being not more than from ten to fifteen degrees from a 
 vertical attitude ; but the slope is for part of the distance to the north and 
 for the remainder to the south ; there is not however supposed to be any 
 repetition of the measures, which are here given in descending order : 
 
 Feet. 
 
 Green slate rock, with a few scattered pebbles through some parts of it, becoming 
 in other parte sufficiently abundant to entitle the rock to the appellation of 
 a conglomerate slate : the sedimentary layers are not distinctly marked ; 
 the rock has a jointed structure, and the planes of division, which are very 
 even, cut clean through the pebbles without any deflection, 40 
 
 Green pebbly slate ; the edges of the laminae are better marked than in the pre- 
 ceding mass by different shades of green and grey or black, giving the rock 
 a ribbon-like aspect ; the pebbles, which appear to be chiefly gneiss, 
 granite, or syenite, are worn smooth with the rest of the surface ; they are 
 more numerous at the top than at the bottom, 300 
 
 Green slate rock, with a considerable number of pebbles towards the top, and 
 fewer in the lower part ; several hollows are worn at intervals running in the 
 strike, which are covered with sand ; the rock is probably softer in those 
 parts, and may be partially talcose, 550 
 
 Green pebbly slate, with large and small boulders of the same character as 
 before ; some of the boulders may be a foot in diameter ; iron pyrites is dis- 
 seminated in some parts of the mass, 1*70 
 
 Measures not seen, being covered by sand, 90 
 
 Green slaty conglomerate with large pebbles of igneous or altered rock ; the 
 colors of the edges of the slate layers are green, black, and red, and are very 
 distinctly marked, 15 
 
 Green slate rock with many pebbles ; the arrangement of the different colors of 
 the thin edges of the laminae sometimes partially conforming to the pebbles, 
 and running round them, gives to the smooth surface a ligneous aspect, like 
 a plataed surface of wood, shewing its fibres and knots, 30 
 
 Green slate rock with fewer pebbles, 40 
 
 Green slate rock with scattered large pebbles, 10 
 
54 GEOLOGY OF CANADA. [CHAP. IV. 
 
 Feet. 
 
 Green slate rock of the same character as before, with sometimes a greater and 
 
 sometimes a smaller number of pebbles, but all shewing some, 130 
 
 Green slate conglomerate, containing a collection of boulders, some of them a 
 
 foot in diameter, in the same slaty matrix as before, 5 
 
 Measures concealed by sand, 30 
 
 Green slate rock with many pebbles, some of them six inches in diameter ; some 
 of granitic character have a red hue ; the edges of the slate laminae are 
 green, black, and red ; many of the pebbles are of the same green as the 
 slate ; they appear of various shades of grey when fractured, 30 
 
 Green slate rock containing a larger number of pebbles in the middle than at the 
 
 top and bottom, 30 
 
 Measures concealed by the sand, 20 
 
 Green slate rock of a more pebbly character than before ; some of the pebbles are 
 six or eight inches in diameter ; the sedimentary layers are finely waved, 
 and the surface of the rock near the water's edge is very much pitted, yield- 
 ing in some parts to the action of the water more readily than others, 30 
 
 Green slate rock ; the bedding is very even and regular, and well marked by 
 different shades of black and green ; the character of the rock appears to be 
 somewhat talcose towards the top, but harder towards the bottom, and when 
 unweathered the laminae are very difficult to separate, 20 
 
 Green slate rock of much the same character as before, but perhaps somewhat 
 
 harder, 15 
 
 Green slate rock with even and regular bedding, slightly unctuous, and talcoid 
 in several of the divisions ; in general however the rock is very hard, and 
 splits with difficulty in the direction of the layers, 20 
 
 Green slate rock ; some parts of it have a few scattered pebbles, which are in 
 general flat or elongated in the direction of the strata ; ribbon-like stripes 
 in the direction of the laminae are very regular, and in some parts the rock 
 splits into rude slates, but on the whole it is very hard and close ; some 
 parts are unctuous on the surface ; the dip is here S. < 75, 90 
 
 Green slate rock with large pebbles and small boulders of granite or gneiss, 
 quartz, and a chert-like stone ; the general color gives to the rock a chlor- 
 itic or epidotic aspect ; crystallized epidote appears in some of the cracks 
 of the rock, 35 
 
 1?00 
 
 At the Dore* a much larger amount of the slate formation than is here 
 given comes in behind the preceding section ; but it was so covered with 
 trees and moss at the time of the examination, that it was found impossible 
 to follow out the details. Towards the lower part it assumes more the 
 character of the gneiss which usually succeeds it, and becomes interstrati- 
 fied with reddish-yellow feldspathic layers ; but sufficient data have not yet 
 been ascertained to determine what may be the total thickness of the slate 
 rock in this part, though it must probably attain several thousand feet. 
 
 Reddish-yellow feldspathic masses occasionally traverse the slate as 
 they do the gneiss beneath, and it is not quite certain how the similar 
 masses mentioned above as forming layers may be related to them. 
 Though running with these apparent layers, it is possible they may not 
 
CHAP. IV.] HURONIAN SERIES. 55 
 
 belong to the sedimentary portion of the rock, and their relation to the 
 strata may be merely accidental. Masses of translucent white quartz 
 varying in thickness from a few inches to several feet are found running 
 both with the strata and transverse to it. These appear more particu- 
 larly to belong to the slate formation, but they are supposed in both cases 
 to be veins. 
 
 In that part of the country on the north shore of Lake Huron which lies 
 between the Mississagui and St. Mary Rivers, where the Huronian series 
 has been more completely examined than elsewhere, the immediate contact 
 of the gneiss with the overlying rocks has not been observed. On the Kocks of the 
 coast line between the Mississagui and Thessalon Rivers, a distance of Thessalou - 
 about twenty-five miles, the gneiss extends from within about four miles of 
 the former to within about the same distance from the latter ; but it is 
 very much disturbed by intrusive granite and greenstone, and, although 
 there are great exposures of rock, it is very difficult to make out how the 
 stratified portions are related to one another. The gneiss extends to the 
 vicinity of a small stream about a mile and a half above Les Grandes Sables, 
 and what is supposed to be the lowest Huronian mass of that part occurs 
 about half a mile above the stream. It consists of a grey quartzite which 
 abuts against one mass of gneiss and runs under another, and appears to 
 be much broken by and entangled among the intrusive rock ; but judging 
 from a transverse measure in one part, its thickness would not be far from 
 500 feet. Farther west, after passing an exposure of stratified amygda- cwontic and 
 loidal trap which would apparently overlie the quartzite, the rocks for epld< 
 about two miles east of the Thessalon appear to consist of green fine-grained 
 chloritic and epidotic slate, alternating with masses that have the aspect 
 of trap, composed of blackish hornblende and greenish-white and reddish 
 feldspar, with a sparing quantity of mica. The slates and trap-like beds 
 alternate in thicknesses varying from two inches to thirty feet, but the 
 thickness of the whole has not been determined, though it probably exceeds 
 2000 feet. 
 
 The masses to the eastward, which overlie the slates, have been examined 
 in some detail, and the sequence and volume of the whole series, including 
 the quartzites and chloritic slates above mentioned, with bands of lime- 
 stone, chert, and jasper conglomerate, would appear to be as follows in 
 ascending order : 
 
 Feet. 
 
 1. Grey quartzite, thin bedded in some parts ; the thickness is very doubtful,.. 500 
 
 2. Greenish, red-weathering chloritic and epidotic slates, interstratified with 
 
 trap-like beds ; of this mass also the thickness is very doubtful, 2000 
 
 3. White quartzite, the color sometimes passing into grey ; the rock is princi- 
 
 pally fine grained, but the granular texture is often lost, and great masses 
 of it become vitreous quartzite. The rock on the other hand often becomes 
 coarse grained and assumes the character of a conglomerate from the 
 
56 GEOLOGY OF CANADA. [CHAP. IV. 
 
 Feet. 
 
 presence of pebbles, consisting chiefly of white quartz, varying from the 
 size of duck-shot to that of musket-balls. The beds, which are generally 
 massive, are frequently separated by layers of fine grained greenish-grey 
 silicious slate, and considerable masses of greenstone are frequently inter- 
 calated in different parts of the whole thickness, 1000 
 
 4. Slate conglomerate, composed of pebbles of gneiss and syenite held in an 
 argillo-arenaceous cement of a grey or more frequently of a greenish 
 color, the latter arising apparently from the presence of chlorite. The 
 pebbles, which are of reddish and grey colors, vary greatly in size, being 
 sometimes no larger than swan-shot, and at others boulders rather than 
 pebbles, measuring upwards of a foot in diameter ; the proportions of 
 these also vary much ; they sometimes constitute nearly the whole mass 
 of the rock, leaving but few interstices for the matrix, and sometimes 
 on the contrary, they are so sparingly disseminated through consider- 
 able masses of the matrix as to leave spaces of several feet between 
 neighboring pebbles, which may be still several inches in diameter ; with 
 the pebbles of gneiss and syenite are occasionally associated some of dif- 
 ferent colored jaspers and others of quartz. The matrix appears to pass 
 on the one hand into a grey quartzite by an increased proportion of the 
 arenaceous grains, and on the other into a thin bedded, dark greenish, 
 fine grained slate, which is sometimes very chloritic. A third form 
 assumed by the matrix is one in which it is scarcely distinguishable from 
 fine grained greenstone. In the slate the stratification is often marked 
 by slight differences of color, in the direction of which it is occasionally 
 cleavable ; the bands in other instances are firmly soldered together, but 
 in both cases joints usually prevail, dividing the rock into rhomboidal 
 forms which are sometimes very perfect. Very heavy masses of greenstone 
 are generally interstratified in the rock, which do not seem confined to 
 
 any one stratigraphical place, k 1280 
 
 Limestone. 5. Limestone, usually of a compact texture, but sometimes partially granular ; 
 the colors are green, drab, and dark grey, the latter two prevailing. Some 
 beds are occasionally met with of a dull white, with a waxy lustre 
 in fresh fractures ; these weather to a yellowish-brown on the exterior, 
 and appear to be dolomitic. The whole band is in general thin bedded, 
 and a diversity of character in the layers, probably arising from the pre- 
 sence of more or less silicious matter, causes the surface of weathered 
 blocks to present a set of bold but minute ribs of various thicknesses, 
 which when the beds are much affected, as they often are by diminutive 
 undulations, contortions, and dislocations, exhibit on a small scale a beau- 
 tiful representation of almost all the accidents that occur in stratification, 
 affording very excellent ready-made geological models, 300 
 
 6. Slate conglomerate of the same general character as that beneath the lime- 
 
 stone, but the pebbles not so large ; it is interstratified with beds of reddish 
 and grey quartzite and layers of fine grained greenish-black and light 
 olive-green silicious slate, some of which yield hones of a very fine 
 description ; considerable masses of greenstone are interstratified in 
 various parts of the deposit, 3000 
 
 7. Red quartzite, interstratified with masses of greenstone ; the quartzite is in 
 
 general granular and of moderately fine texture, but it occasionally 
 becomes a fine conglomerate. The color is sometimes only a light tinge of 
 red and at others a decided red, seemingly derived from minute and thickly 
 disseminated spots or from a diffused tinge of an orange-red, probably 
 due to the presence of iron ; but the spots are sometimes of a larger size^ 
 
CHAP. IV.] EFEONIAN SERIES. 57 
 
 Feet. 
 
 and so arranged as to give to the rock a speckled aspect. The rock is in 
 general thick bedded ; some of the beds shew oblique elementary layers, or 
 what is commonly called false bedding, and the surfaces of other beds 
 display well defined ripple-marks ; masses of greenstone are interstratified 
 in the deposit, some of them of great thickness, 2300 
 
 8. Red jasper conglomerates. The rock is sometimes a moderately fine Jasper con- 
 
 grained white quartzite, often with a vitreous aspect, but it very commonly 
 becomes coarse grained and assumes the character of a conglomerate, the 
 pebbles of which vary from the size of duck-shot to that of grape and 
 canister ; these pebbles are almost entirely either of opaque white vitreous 
 quartz or various colored jaspers ; some of them are lydian stone, some 
 hornstone, and other varieties, and many of them are banded, shewing 
 their derivation from a more ancient stratified rock. The pebbles are 
 often displayed at the top or bottom or in the middle of fine grained 
 beds ; they are sometimes arranged in thick bands, and blood-red jaspers 
 often predominating in a nearly pure white base produce a brilliant, 
 unique, and beautiful rock. Considerable masses of greenstone are inter- 
 calated in different parts of the group, 2150 
 
 9. White quartzite, very frequently of a vitreous aspect ; in considerable thick- 
 
 nesses of the rock the bedding appears sometimes to be so completely 
 obliterated, and the whole mass presents so great a uniformity of appear- 
 ance, that it becomes quite impossible to ascertain the dip or strike, or to 
 distinguish joints from beds, but in other parts massive beds are separated 
 by thin silicious layers resembling chert, and greenstones occur interca- 
 lated between different masses of the deposit, 29*70 
 
 10. Yellowish chert in thin and very regular beds, interstratified with layers of Chert and 
 
 green, buff, and grey silicious limestone, and green and pale drab compact limestone. 
 
 silicious slate, with a stratum of red and yellowish fine grained sandstone 
 
 at the bottom, 400 
 
 11. White quartzite, frequently of vitreous aspect, and occasionally mottled with 
 
 lead-grey patches, 1500 
 
 12. Yellowish chert and impure limestone, similar in its general aspect to the 
 
 previous chert band, 200 
 
 13. White quartzite imperfectly examined, 400 
 
 18000 
 
 The igneous rocks which, as overflows, it will be convenient to consider stratified 
 constituent parts of the stratified series, may be classed as a whole under gl 
 the denomination of greenstone or diorite. The masses are sometimes 
 very great, and in such cases the rock usually consists of a greenish-white 
 feldspar, and dark green or black hornblende. The feldspar however is 
 sometimes tinged with red, and the diorite then appears to pass into a syenite 
 by the addition of a sparing amount of quartz. These two forms of the 
 diorite are almost always highly crystalline, and in general not very fine 
 grained. Sometimes, 4 however, the greenstone displays a fine texture, and in 
 such cases a large amount of it, more particularly in the lower part of the 
 series, frequently holds much disseminated chlorite, giving a very decided 
 green color. Portions of it are found containing so great a proportion 
 of this mineral as to yield with facility to the knife, affording to the 
 
58 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. IV. 
 
 aborigines an excellent material for the manufacture of their calumets 
 or tobacco-pipes. In addition to the chlorite, epidote is a prevailing 
 mineral in this description of rock, associated with which an amyg- 
 daloid, already alluded to, is in one place seen, some of the cellules 
 of which contain quartz, others calcspar and bitter spar, and some 
 
 Amygdaloid. f e ^ specular iron. The amygdaloidal trap is very distinctly arranged 
 in layers, which, though they do not exceed two or three in number, give, 
 with beds of porphyritic greenstone containing large crystals of feldspar, 
 occurring near the amygdaloid, a stratified aspect to the whole of the 
 mass of trap associated with them. No such decided appearances of 
 stratification have been met with in the more crystalline greenstones. 
 They usually however display parallel planes of division in several direc- 
 tions, and it frequently happens that some of these parallel planes are only 
 moderately inclined ; but there have not been observed on the surfaces or in 
 the character of the rock any distinct evidences of stratification or of succes- 
 sive deposit, and no columnar structure at right angles to any set of planes 
 such as sometimes so clearly marks an overflow. It is therefore in most 
 instances only by a reference to its immediate relation to the sedimentary 
 rocks on each side that the general attitude of any band of the greenstone 
 can be made out. 
 
 Independent of the overflows, igneous rocks are connected with the 
 formation in intrusive masses. These intrusive masses consist of greenstone 
 and granite. The intrusive greenstones do not seem to differ much in 
 mineral character from those composing the overflows : they constitute 
 dykes which run in so many directions that it is difficult to determine the 
 prevailing ones. These dykes vary in breadth from a few inches to several 
 hundred feet ; they cut all the stratified rocks of the series, igneous as well 
 as sedimentary, splitting into branches which often join one another 
 
 Granite. and enclose great fragments and masses of strata. The intrusive granite, 
 in so far as observed, is in general of a decided red color, arising from 
 the presence of a largely preponderating quantity of red feldspar, which 
 is mingled with translucent white quartz : mica is not very abundant, and 
 hornblende sometimes accompanies or replaces it. From large masses of 
 the rock however both these minerals are often wholly absent, but epidote 
 in general forms a constituent, sometimes in great abundance. The intru- 
 sive granite occupies a considerable area on the coast of Lake Huron, south 
 of Lake Pakowagaming. It there breaks through and disturbs the gneiss 
 of the Laurentian series, and forms a nucleus from which emanates a 
 complexity of dykes, proceeding to considerable distances. As dykes of 
 a similar character are met with intersecting the rocks of the Huronian 
 series, the nucleus in question is supposed to be of the Huronian age, as 
 well as the greenstone dykes which are intersected by it. 
 
 Intrusive 
 greenstone. 
 
CHAP. IV.] HURONIAN SERIES. 59 
 
 The relations of these different intrusive rocks display a succession Dykes of dtf- 
 of events in the history of the Huronian series. There is of course ferenta g 68 - 
 a set of dykes cutting the sedimentary rocks, and giving issue to the 
 greenstone overflows ; it is difficult, however, to identify these, but 
 another set of greenstone dykes is seen cutting both the sedimentary and the 
 igneous strata. The intrusive granite, sending forth dykes, intersects the 
 preceding ones, and then another set of greenstone dykes cuts the intrusive 
 granite in its turn. Evidences of disturbance and dislocation accompany 
 all these successive intrusions, those connected with the granite being the 
 most violent. But there is another set of disturbances of still more recent 
 date, and it is to these that are due the metalliferous veins which give to 
 the country its value as a mineral region. 
 
 These metalliferous veins intersect all the rocks that have been mentioned. Metalliferous 
 They are probably themselves intersected by veins or cross courses, break- lodes< 
 ing their regular continuity ; but there is evidence that slips or displace- 
 ments of the country on opposite sides of the veins occurred at the 
 time when the fissures which gave rise to these were formed. Numerous 
 instances occur where granite and greenstone dykes cut by the metallifer- 
 ous veins are thrown considerably out of their course, and several examples 
 of this have been observed at the Bruce mines. 
 
 The metal which these veins hold in the greatest quantity is copper, in copper and 
 the forms of vitreous, variegated, and pyritous sulphurets. Iron pyrites mckelt 
 is sometimes associated with them, but in general not in large quantities. 
 Copper ore has in one instance been found accompanied by rutile, and in 
 another (at the Wallace mine) associated with an arsenical sulphuret of 
 iron and nickel, containing a trace of cobalt. The gangue or vein stone of 
 the copper ores is in general white quartz ; and there is very often present, 
 but not in very great quantity, a white compact yellow-weathering dolomite, 
 which in druses assumes the form of pearl spar ; carbonate of lime also 
 appears occasionally in the form of dog-tooth spar. 
 
 The veins vary in breadth from a few inches to thirty feet ; but when 
 of this last great breadth, or even much less, they usually contain a 
 considerable amount of brecciated wall rock mixed up with the gangue. 
 Many of them range from one to three and four feet, and their slope 
 or underlie varies from about fifty to ninety degrees. From such as may 
 be considered master lodes, innumerable branches of various sizes start, 
 some of which visibly diminish before proceeding far, and finally dis- 
 appear, while others maintain moderate widths with much regularity for 
 considerable distances, and many run to a junction with parallel lodes. 
 On Lake Huron the cracks and dislocations occupied by the main lodea 
 appear to be near to and parallel with the axes of anticlinal and synclinal 
 folds in the stratification, and no doubt were produced when the forces 
 causing the undulations were in operation. Hence these lodes, often for 
 
60 GEOLOGY OP CANADA. [CHAP. IV. 
 
 considerable distances, run with the strike of the formation. They are thus 
 in a rude way parallel to one another, and run in directions between west 
 and north-west, more nearly approaching the latter. 
 
 Distribution T ne quantity of copper contained in these lodes is very variable, ranging 
 from mere specks of ore in some to large workable amounts in others. In 
 regard to the productiveness of the lodes, it appears probable that it will 
 be different in the different rocks which these may intersect. The underlie 
 of the lodes being in general greater than the dip of the strata, they 
 must pass from one rock to another downwards, and, as the lodes preserve 
 somewhat regular courses, they will also pass from one to another horizon- 
 tally, from the effects produced in the geographical distribution by 
 denudation, where the strata, folding on anticlinal and synclinal axes, pre- 
 sent local transverse depressions or elevations. As far as observations 
 have extended, it appears that the copper is most abundant in the 
 greenstone, least so in the sandstone or quartzite, and more plentiful in 
 the slate when this is free from pebbles than when it becomes a conglom- 
 erate. In the quartzite rock the white quartz veins often appear nearly 
 destitute of ore, presenting but a few specks of the yellow sulphuret of 
 copper at intervals, and, when a vein holding much ore in the greenstone 
 can be traced to the quartzite, it seems gradually to lose its richness, and 
 finally presents little else than vein-stone, its breadth remaining undi- 
 minished. How the productiveness of the metalliferous veins may be 
 affected when they meet with any considerable body of the intrusive granite 
 has not been ascertained, since none of them have been observed cutting 
 the granite nuclei, and, though they have been found intersecting the 
 granite dykes, these are too narrow to produce any perceptible change in 
 the quantity or nature of the ore. / 
 
 In the Huronian country there is scarcely any considerable area wholly 
 destitute of cupriferous veins. Instances of these are known to occur at 
 the most southern part of the lower lakes of the Maskinongi, a tributary 
 of the Sturgeon River, at the Wallace mine near the mouth of the White 
 Fish River, where a crop trial has been made on a vein holding both copper 
 and nickel, at the mouth of the Spanish River, and in several parts of the 
 Mississagui. Crop trials have been made of lodes on Root River and 
 Garden River, and various places on and near Echo Lake, but the most 
 important lodes which have been tested are those of the Keating and 
 Cuthbertson locations at the Wellington and Bruce mines. From these 
 latter locations large quantities of ore have been obtained and exported. 
 The lodes here are near the axis of an anticlinal in the strata, and run 
 with the strike towards the north-west. 
 
 The Huronian rocks are not known to extend farther to the eastward 
 than the line between Lake Temiscamang and Shebahahnahning, which 
 has already been given in describing the boundary of the Laurentian series. 
 
CHAP. IV.] HURONIAN SERIES. 61 
 
 How far the Huronian series may spread continuously westward from the Distribution 
 north part of that line has not yet been ascertained. On Lake Huron 
 the rocks of this series occupy the coast from Shebahahnahning to the 
 mouth of the Mississagui Eiver ; and in the valley of the Spanish River 
 they appear to have a breadth northward from Lacloche of about ten 
 miles. The rock which there limits them on the north is probably a part 
 of the Laurentian gneiss, though it has been found difficult to distinguish 
 the gneiss in that part from an intrusive granite. 
 
 The distribution of the series between the Mississagui and St. Mary Map and sec- 
 Rivers is represented on the accompanying map, which is illustrated by tion> 
 a vertical section on a line running northward from St. Joseph Island, 
 through Thessalon Lake, to a distance of about fifteen miles from the shore 
 of Lake Huron. From these it will be perceived that in the area in 
 question the various masses which have been described as constituting the 
 series are arranged in the form of a trough, extending transversely from 
 the lower part of Echo River above Echo Lake to some point beneath the 
 unconformable fossiliferous rocks to the south-west. The longitudinal axis Thessalon 
 extends along the valley of the Thessalon from a rapid between five and trou s h - 
 six miles above its mouth to the south-west side of Thessalon Lake, and 
 proceeds thence towards St. Mary River, between Little and Great St. 
 George Lakes. The main trough is divided into three subordinate and 
 nearly parallel troughs by two anticlinal forms. The axis of one of them 
 passes a little south of Echo Lake, but the form appears gradually to die 
 away towards the south-east. The axis of the other anticlinal passes 
 through the Bruce mines, and proceeding westerly gradually bears rather 
 more westward than the axis of the main synclinal, the course of which 
 is about N. 30 W. 
 
 It will be perceived that the strata on the opposite sides of the axis in Great disio- 
 their eastward strike converge, but that the equivalent members of the cation> 
 series, instead of meeting on the axis, are carried past one another in such 
 a manner that the base of the chert and limestone band (10) on the north- 
 ward side comes against the middle of the upper slate conglomerate (6) 
 on the southward side, while the base of the same limestone band (10) 
 on the southward side is brought against the upper part of the white 
 quartzite (11) on the northward. This part of the white quartzite (11) is 
 not far from 1500 feet over the base of the limestone band (10), and there 
 must consequently be a downthrow equal to this on the north side of the 
 axis at that part. But between the base of the chert and limestone band (10) 
 and the middle of the upper slate conglomerate (6) there is a thickness of 
 rock equal to upwards of 9000 feet, so that the downthrow must gradually 
 increase to that extent in going nine miles to the eastward. 
 
 From the position where this great fault leaves the Thessalon, about six 
 miles above the mouth of the river, it appears to lose a portion of its 
 
62 GEOLOGY OF CANADA. [CHAP. IV, 
 
 southing in its progress eastward, and to come upon the most southern part 
 of Lake Wabiquekobingsing, where the lower limestone band (5) on the 
 north side is brought against what is considered to be Laurentian gneiss. 
 The course of the dislocation thence again turns more south, and farther 
 on it reaches the south-eastern part of Lake Pakowagaming, having gneiss 
 on the south, and the lower slate conglomerate (4) on the north side all the 
 way between the lakes. Its farther progress has not yet been determined. 
 If the same law applies to the fault to the westward of Lake Thessalon 
 as to the eastward, the downthrow on the northward side of it, after 
 passing a zero point, should change into an upthrow farther on. Near 
 R#ot River, in a position where we might expect the great fault, we find the 
 limestone band (5) with the slate conglomerates (4 and 6) on the south, 
 and the gneiss of Gros Cap on the north, in such a relation as would 
 answer these conditions ; but the dislocation in the intermediate parts being 
 comparatively small, its efiect has not yet been completely traced out. 
 
 On the line of section the dips of the strata vary in inclination from 
 eighteen to forty-five degrees ; but more to the eastward they gradually 
 diminish, and to the east and north of Lake Wahbiquekobing and Lake 
 Pakowagaming the attitude of the strata approaches the horizontal, the 
 slope being seldom over six degrees, and often not over two. The lower 
 slate conglomerate and its associated masses of greenstone are in conse- 
 quence spread over a very considerable area in that part, and pass beyond the 
 Mississagui Mississagui. On the opposite sides of this river, however, for some dis- 
 tance up, the dips, though small, are in opposite directions, and prove the 
 existence of a flat anticlinal arch, the axis of which is coincident with the 
 river for eighteen miles, from a point about six miles up from the mouth of 
 the river to an elbow below the junction of the Little White River. Beyond 
 this its course continues to the north-westward. 
 
 This anticlinal form limits the Thessalon trough on the north-east side, 
 and the parts examined beyond it are chiefly confined to the banks of the 
 Mississagui. For fourteen or fifteen miles above the mouth of the Little 
 White River, the rocks appear to belong to the lower slate conglomerate 
 and the greenstones associated with it ; and beyond this as far as the 
 river has been surveyed, the rock is either gneiss or syenite, with the 
 exception of two miles of slate conglomerate, which occur on the east bank 
 about four miles above the position where the upward course of the stream 
 changes from north-westward to eastward of north. On the Little White 
 River, about five miles up from the mouth, the lower band of limestone (5) 
 makes its appearance. It has been traced about two miles south, and it 
 here most probably constitutes a part of the western outcrop of a trough 
 which underlies an area to the eastward, around which it has yet to be 
 traced. 
 
CHAP. IV.] HURONIAN SERIES. 63 
 
 From the Thessalon westward the southern limit of the Huronian rocks 
 embraces the coast and all the islands immediately near, including the 
 Palladeau group ; it takes in, however, only the northern extremity of the 
 largest island, not very far south of the group ; and from it crosses to St. 
 Joseph Island, where it includes the promontory which is south of the 
 Island of Campment d'Ours, as well as a portion of the north side of the 
 northwestern extremity of St. Joseph Island. It includes a narrow strip 
 on Sugar Island, at the exit of Great Lake George, and, from a point about 
 half-way up the eastern side of this lake, leaves a margin bearing higher 
 rocks on the east and north sides of the lake, as well as upon the north side 
 of St. Mary River and Little Lake George. This margin appears to project 
 a short distance beyond the average width up the valley of Echo River 
 and that of Garden River ; and above Little Lake George it cuts off the 
 Huronian rocks and comes against the Laurentian gneiss, which runs out 
 into the promontory of Gros Cap. 
 
 On Lake Superior, Huronian slate conglomerates and jasper conglom- 
 crates occupy a position between Goulais River and Batchehwahnung 6eries on 
 Bay, intersected near the latter place by a great east and west syenitic nor. 
 dyke. Farther north, rocks of the series are spread over what appears 
 to be a triangular area, extending along the shore from eight to nine miles 
 on each side of Michipicoten River, at the mouth, and about the same 
 distance up the stream. A little farther west it presents a very narrow 
 strip running about twelve miles along the coast, and another one of 
 eight miles about five miles south from Otter Head. 
 
 Another locality in which these rocks have been observed in Canada Thunder Bay. 
 is Thunder Bay, where they occupy the coast for a distance of ten miles 
 immediately below the mouth of the Kaministiquia River on the north side, 
 leaning in a narrow strip against the gneiss of the lower series. It is not 
 improbable that they may present a narrow belt in the valley of the Kaminis- 
 tiquia. They occupy the coast for about seven miles on each side of the 
 New Pic River, while an interval from this to a point two miles beyond the 
 Old Pic River, including the coast of Peninsula Bay and Harbor and Pic 
 Island, is composed of trap. Beyond this the chloritic slates occupy about 
 fifteen miles of the coast, extending to the neighborhood of the deep cove 
 which receives the Pike River. It appears probable that the slates thus 
 flanking the trap on either hand may be the sides of a trough converging 
 to a point inland, the distance of which from the coast has not been 
 ascertained. The Slate Islands are nearly on the strike of the north- 
 western side of the trough, and they may probably derive their name from 
 being composed of slate rock ; but the islands have yet to be examined. 
 
 The upper part of the Kaministiquia River, between its sources and Kaministi- 
 Dog Lake, for the greater part of the distance passes through a vast swamp, qi 
 which is bounded on each side by low granitic ridges, probably belonging 
 
64 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IV. 
 
 Contact of 
 Laurentian 
 and Huron- 
 ian rocks. 
 
 to the Laurentian gneiss. The country around Dog Lake is of a moun- 
 tainous character, thickly covered with forests, chiefly of evergreens, and 
 among them are red and white pine. White and yellow birch are 
 abundant, some of them of large dimensions ; and it is chiefly from the 
 neighborhood of Dog Lake that the Hudson's Bay Company at Fort 
 William are supplied by the Indians with birch bark for the manufacture 
 of their canoes. 
 
 The water of this lake, of which the surface is probably about 1100 
 feet above the level of the sea, escapes through a deep narrow gorge, and 
 is precipitated over a succession of heavy falls, amounting altogether to 
 probably upwards of 200 feet, and occasioning the Great Dog Portage, 
 extending a mile and a half across a narrow neck of elevated land. 
 Between the Great Dog Portage and the Grand Falls the river flows over 
 a series of steps, each of them causing falls or strong rapids, with long 
 stretches of still water in the intervals, and six of them occasioning 
 both to upward and downward voyageurs, portages which vary in distance 
 from a few yards to more than a mile. The total fall in the distance is 
 probably 200 feet, 
 
 In the upward navigation of the river the first development of the 
 Laurentian series occurs at the second portage, about half a mile above 
 the Grand Falls. At the lower end of the portage, where the series makes 
 its appearance, the rock resembles a massive syenite, in some parts red 
 and in others whitish, but is probably a hornblendic gneiss in which the 
 lamellar arrangement of the constituent minerals is obscure, as the rock 
 gradually passes into such a gneiss. Resting on it conformably there 
 occurs a series of dark greenish-blue or greenish-black slates, the one rock 
 passing almost imperceptibly into the other. The section occupies 
 upwards of a quarter of a mile on the river bank, and at the upper end of 
 it, as well as at the head of the portage, the dip is N. 54 E. Parallel 
 joints are observed to cut the rocks, the directions of the two main sets 
 being S. 41 E. and S. 13 E. Numerous strong veins of white quartz 
 intersect the slates, sometimes occupying the joints, and the whole forma- 
 tion, both in the strata and in the veins, is highly charged with iron 
 pyrites. 
 
 At each rapid part of the river above the Grand Falls there is a 
 greater or less development of these rocks, most frequently presenting 
 the more distinctly stratified part of the gneiss. The best exposure of 
 the slates is at the Three Discharges, about four miles above the Grand 
 Falls, where the rocks are observed to pass from the gneiss to the slate. 
 The slates have a horizontal breadth at right angles to the stratifi- 
 cation of upwards of thirty-seven chains, with a dip N. 42 W. < 68 
 without any apparent irregularities. This would give a vertical thickness 
 of about 2300 feet. Towards the bottom, near the junction with the 
 
OHAP. IV.] HURONIAN SYSTEM. $5 
 
 gneiss, the slates are of a bluish and occasionally of a brownish color. 
 They are intersected by numerous parallel joints, which divide the mass 
 into rhomboidal forms of singular regularity. The middle and upper 
 portions of the section are usually of a pistachio-green resembling the 
 green of epidote, and frequently in part present a jaspery character. They 
 are hard and compact, usually with a conchoidal but sometimes with a 
 splintery fracture. The divisional planes are frequently covered with mica, 
 and in such cases the rock may almost be termed a mica slate. The whole 
 of the beds are charged with iron pyrites, and numerous veins of white 
 quartz intersect them. Imbedded in the slates are sometimes observed 
 masses of various irregular shapes, very rudely spherical, and along the 
 basset edges of the strata numerous pot-holes are worn, some of which are 
 not less than four yards in diameter. 
 
 Above this section and in continuation of it, the same rocks are still 
 exposed upon the banks, but in a more disturbed condition. Their color 
 is mostly pistachio-green, with occasional red shades running through 
 it, and iron pyrites is met with in almost every part of them. As far as 
 Dog Lake, the rocks, wherever they were seen, resembled in character 
 those which have been above described. About two miles above the Three 
 Discharges some very large boulders of a conglomerate character are met 
 with, containing blood-red jasper pebbles, and balls of iron pyrites in a dark 
 brownish or blackish matrix, having much of the trappean aspect belonging 
 to some of the varieties of the slate conglomerate. Though nowhere seen 
 in place in this neighborhood, it appears probable that this slate conglom- 
 erate may be a member or an immediate sequent of the slates above 
 described. The boulders rest upon these slates, and their form and size 
 indicate that they have not been far removed from the parent rock. 
 
 In several parts of this continent crystalline stratified rocks are met Azoic rocks 
 with, probably of Laurentian or Huronian age. Dr. Bigsby, in 1824, 
 described an extensive tract of gneissoid rocks in Rainy Lake and Lake 
 Lacroix, north of Lake Superior, having a general direction from N.W. to 
 N. by W., and dipping eastwardly. This gneiss was associated with mica- 
 ceous schists containing staurotide, beds of hornblende, chloritic slates 
 with octahedral iron, greenstone slates and syenite. Porphyritic granite 
 with beryl also occurs in the region. These gneissoid strata form part of 
 the great range of Laurentian rocks which have been traced from Canada 
 to the Arctic sea. They have been farther described by Dr. Dale Owen 
 in the region west of Lake Superior, where they are found upon the Mis- 
 sissippi, Chippewa, and St. Croix Rivers. Mica slates with staurotide are 
 here associated with quartzite, gneiss, hornblendic and syenitic rocks, 
 greenstones and granites, and are overlaid by sandstones of the Potsdam 
 group. Still farther west, in Kanzas and Nebraska, according to 
 Hay den, the Black Hills and the Laramie range consist of reddish por- 
 
 E 
 
66 GEOLOGY OF CANADA. [CHAP. IV. 
 
 phyritic granite, surrounded by nearly vertical strata of gneiss, micaceous, 
 talcose, and hornblendic schists, with quartzites and clay slates. Upon 
 these, at the base of the Black Hills, repose fossiliferous beds of the Potsdam 
 group. 
 
 issouri. Again, in Missouri, we have ancient crystalline rocks, consisting, accor- 
 
 ding to Mr. Swallow, of ranges of porphyry with syenite, silicious and 
 argillaceous slates, and what appear to be altered conglomerates. With 
 these are associated great masses of specular and magnetic iron ores, 
 sometimes schistose, constituting the famous Iron Mountain and the Pilot 
 Knob. In Arkansas also occur crystalline strata, consisting, according to 
 Engelman, of talcose, hornblendic, and silicious slates, often highly inclined, 
 and associated with beds of dark blue limestone, and at Magnet Cove with 
 iron ores and many fine crystallized minerals, among which are epidote, 
 garnet, mica, brookite (arkansite), schorlomite, and elaeolite. These rocks, 
 according to Engelman, probably extend into Texas. 
 
 Farther investigation will be necessary to determine how far these 
 ancient strata belong to the Laurentian system, and how far they are of 
 the age of the Huronian series. Both of these groups contain iron ore ; for 
 while the great ore beds in Canada, and on Lake Champlain, are Lauren- 
 tian, those of Marquette in northern Michigan, like that of the Wallace 
 mine in Canada, appear to be included in the Huronian series. 
 
 wfoundiand. In Newfoundland, Mr. Jukes has described wide areas of crystalline 
 azoic rocks. These are probably for the most part the equivalents of those 
 of south-eastern Canada, which will be shown in a subsequent portion of 
 this work to be altered palaeozoic strata. At Indian Head and at York 
 Harbor on the western coast, however, he observed dark-colored rocks 
 made up of labradorite and hypersthene, and of albite and hypersthene, 
 which resemble the anorthosites of the Laurentian system. We have 
 already stated that the Seven Islands are composed of anorthisite ; and 
 it may here be noticed, that, according to Bayfield, the same rock, with 
 a base of labradorite, forms the coast for several miles, towards Mingan. 
 
CHAP. V.] GEOLOGY OF CANADA. 67 
 
 CHAPTER V. 
 
 UPPER COPPER-BEARING ROCKS OF LAKE SUPERIOR. 
 
 ROCKS NEWER THAN THE HURONIAN SERIES; DIVIDED INTO TWO GROUPS. LOWER GROUP ON 
 THE KAMINISTIQUIA. BEDS OF TRAP. UPPER GROUP; ITS SANDSTONES, LIMESTONES, AND 
 AMYGDALOIDS, WITH NATIVE COPPER. WRINKLED SURFACE OF TRAPPEAN BEDS. INTRU- 
 SIVE ROCKS ; INTERSECTION OF DYKES. METALLIFEROUS VEINS OF THE TWO GROUPS. 
 COPPER AND SILVER. DISTRIBUTION OF THE LOWER GROUP; OF THE UPPER GROUP. 
 BATTLE ISLANDS. ISLE KOYAL. MICHIPICOTEN ISLAND. MAMAINSE. SANDSTONES OF 
 SAULT STE. MARIE AND SUGAR ISLAND; OF CAMPMENT D'OURS; ITS SUBJACENT HURON 
 
 IAN ROCKS AND OVERLYING LIMESTONES. LACLOCHE SANDSTONES. AGE OF THIS SERIES 
 OF ROCKS; PROBABLY LOWER SILURIAN. 
 
 The Huronian formation on Lake Superior is unconformably overlaid 
 by a second series of copper-bearing rocks, which may be conveniently 
 divided into two groups. Of these the lower consists of bluish slates or 
 shales, interstratified with sandstones and beds of columnar trap, and the 
 upper, of a succession of sandstones, limestones, indurated marls and con- 
 glomerates, also interstratified with trap, which is often amygdaloidal. 
 
 LOWER GROUP. 
 
 The base of this formation, where seen in Thunder Bay in contact Thunder Bay; 
 with the subjacent green slates or slate conglomerates, presents conglom- blmshslate8 - 
 erate beds, probably of no great thickness, composed chiefly of quartz 
 pebbles, with a few of red jasper and some of greenish chloritic slate, in a 
 greenish arenaceous matrix, consisting of the same materials in a finer 
 condition. These are followed by a set of very regular even layers of 
 chert, sometimes approaching a chalcedony, varying in color from nearly chert beds, 
 white, through different shades of grey to black, and in thickness from 
 less than half an inch to six inches and even a foot. These are 
 separated from one another by thin layers of dark grey dolomite, 
 weathering rusty-red, and present a striking ribbon-like appearance. 
 Occasionally thicker beds of dolomite occur, sometimes highly crystalline, 
 separating aggregated bands of the ribbon-like strata ; and these dolomitic 
 beds, as well as the chert bands, are sometimes interstratified with argilla- 
 ceous layers. 
 
68 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. V. 
 
 Carbonaceous 
 matter. 
 
 Shales and 
 limestones. 
 
 In the vicinity of disturbed parts the chert sometimes passes into 
 chalcedony and agate, and small cracks are filled with what appears to 
 be anthracite. Some of the chert bands appear to be made up of a 
 multitude of minute, irregular, closely aggregated sub-globular bodies, 
 floating as it were in the silicious matrix. Anthracite seems to be pres- 
 ent in the centre of some of these, leading to the supposition that the 
 color of the black chert, even where these shapes are not detected, 
 may be owing to the presence of carbon. In some parts of these oolitic 
 chert layers, small blood-red jaspery spots occasionally become inter- 
 stratified with the black ; and in pebbles scattered along t]je shores of 
 Thunder Bay, probably derived from such beds, the red spots become so 
 numerous as to produce a finely mottled or spotted jasper, in which 
 the spots are crowded together, but do not run into one another. In some 
 instances these oolitic layers exhibit small rounded grains of argillite in a 
 matrix of crystalline quartz. 
 
 Higher in the formation, argillaceous slates become interstratified with 
 argillaceous sandstones in such an altered condition that it is often difficult 
 at first sight to say whether the latter may not be trap layers. The 
 sandstones are sometimes slightly micaceous, and they are rather lighter 
 in color than the slates or shales ; and while the slates sometimes exhibit 
 the structure called cone in cone, the harder bands display spherical con- 
 cretions varying from a few inches to two and even six feet in diameter. 
 In some parts of the vertical thickness calcareous layers are occasionally 
 interstratified among the slates, but few of them are pure enough to be 
 entitled to the appellation of limestone. Iron pyrites occurs disseminated 
 in the deposit, and frequently characterises the cherty portion of it, 
 where it is sometimes present in nodules, and in thin, interrupted layers. 
 
 On the Kaministiquia the lowest part of this formation observed occurs 
 near the Grand Falls. Its immediate junction with the rock on which it 
 reposes is concealed from view, but appears to be indicated by the position 
 of a small lake or pond occurring just below the second portage, and of 
 the marshy ravines which run from it in the direction of the strike on each 
 side. The argillaceous slates visibly reach to within a short distance of 
 the pond, (probably brought into place against the Laurentian gneiss by a 
 dislocation,) and keep the river for a quarter of a mile to the Grand Falls, 
 where the strata are seen to slope to the south-east at a very small angle. 
 It is probable that the river flows on the formation all the way from this 
 point to its mouth. 
 
 The general color of the rock is here black, weathering to a rusty-brown. 
 Some of the beds being soft and shaly, are easily decomposed by atmos- 
 pheric influences, while the mass is for the most part a hard argillaceous 
 slate. The whole formation appears to be more or less calcareous, and 
 among the lower members thin beds of magnesian limestone occur, sometimes 
 
CHAP. V.] ROCKS OF LAKE SUPERIOR. . 59 
 
 alternating with thin beds of black chert, and sometimes holding irregularly 
 disseminated black chert nodules. Connected with the chert beds, a black 
 mineral resembling anthracite & frequently seen filling up small cracks, 
 and small jaspery veins are often connected with the rock. Spheroidal 
 concretions of singular uniformity, and sometimes of large size, are dissem- 
 inated through all that part of the formation over which the river passes, 
 and they are more conspicuously displayed among the more shaly portions 
 of the rock. A little above the lowest rapids there is a great accumulation 
 of these concretions, which have been known to the fur-traders for many 
 years under the title of the Devil's Pots. Some of these are six feet in 
 diameter, with a thickness of two feet, and they are found of all sizes 
 down to that of a pigeon's egg. They are usually more convex on the top 
 than on the bottom, bearing a strong resemblance to the stones used in the 
 game of curling. The lines of lamination are distinctly visible in these 
 concretions ; and in some instances, when riot removed from the parent bed, 
 the lines could be traced from the concretion to the partially enclosing rock. 
 They are always highly charged with iron pyrites, and their weight, when 
 they are even moderate in size, is in consequence great. 
 
 The rock is strongly marked by a jointed structure of a very symmet- 
 rical character, dividing the thinly laminated slates into rhomboidal forms of 
 great regularity. At the Grand Falls the direction of the principal joints 
 is S. E. .and W. S. W. The height of the Grand Falls from smooth water 
 below to smooth water above is about 119 feet. The rock is wholly of 
 these slates ; but the thickness here displayed is only a small .part of the 
 total volume of the formation, and belongs to the lower part. 
 
 In Thunder Bay and on the coast above it, trap bands, conformable with Becisofcoium- 
 the stratification, are interstratified in several parts of the formation ; but n! 
 they occur in greatest thickness towards the bottom, not far above the 
 chert beds, and at the summit overlying the whole of the mass. This 
 trap has a distinct crystalline texture, and has been in no instance observed 
 to be of an amygdaloidal character. It appears to be composed of black 
 hornblende and greenish-white feldspar of a corneous aspect, which frequently 
 occurs in large crystals, giving the rock a porphyritic character. Magnetic 
 oxyd of iron in minute grains is generally a constituent part of the' rock, and 
 seems occasionally to compose several hundredths of it, while quartz in small 
 quantity is often present. The only imbedded accidental minerals met 
 with in it are crystalline prehnite accompanied by calcareous spar, occur- 
 ring in the beds overlying the chert, and iron pyrites, which is seldom 
 wholly absent from any considerable mass of the rock. 
 
 In all cases the trap presents a very striking sub-columnar structure at 
 right angles to the plane of the stratification, and the crowning overflow 
 gives a peculiar aspect to the whole region occupied by the formation to 
 which it belongs. The overflow is from 200 to 300 feet thick, and the whole 
 
70 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. V. 
 
 White sand- 
 stones. 
 
 Conglom- 
 
 Limestones 
 and marls. 
 
 of the associated rocks, to the base of the formation, may possess a volume 
 of between 1500 and 2000 feet. Where the formation comes on the lake 
 it usually presents bold cliffs, sometimes attaining the height of 1000 and 
 even 1300 feet, in which the upper part, occupied by the trap, exhibits a 
 vertical columnar face, from the base of which the slates, mingled with 
 fallen fragments of trap, form a talus sloping down to the water's edge 
 at an angle of about forty-five degrees. 
 
 / 
 
 UPPER GROUP. 
 
 Reposing on the formation which has just been described, the first rock 
 met with in Thunder Bay, where the best development of the lower part 
 of the succeeding group occurs, is a white sandstone. The strata are in 
 general of a fine grit, and appear to be composed almost entirely of minute 
 grains of quartz in some parts, and in others small rounded grains of a 
 calcareous character are sparingly intermingled with them. Some beds 
 are coarser than others, and in these rounded pebbles of quartz and 
 occasionally of jasper are seen, seldom exceeding the size of buck-shot. 
 Of these white grits there may be a thickness of about 200 feet. 
 
 They are followed by sandstones, consisting of red and white layers 
 interstratified with one another, and associated with conglomerate beds 
 composed chiefly of pebbles and boulders of coarse red jasper, held in 
 white, reddish, or greenish sand as a matrix. As we ascend in this part of 
 the deposit, the beds appear to hold rather more calcareous matter than those 
 below, and some of the conglomerates enclose patches of limestone with 
 fragments of chert. It is difficult to estimate the thickness of these beds 
 from the difficulty of truly determining the rate of dip, but it appears that 
 at a very moderate computation they cannot be less than 500 feet. 
 
 These beds are succeeded by limestones of a reddish-white color, and 
 very compact texture (some of which would yield very good material for 
 burning into quick-lime), interstratified with calcareo-argillaceous shales 
 and reddish-white sandstones, the whole giving probably not under eighty 
 feet, with an additional fifty feet of reddish indurated marl at the top. 
 
 Succeeding these calcareous strata, after an interval of uncertain breadth, 
 not improbably filled with an additional quantity of the indurated marl, 
 red and white sandstones occur, with conglomerate layers. The red sand- 
 stones are often very argillaceous ; they are usually variegated with green 
 spots, and ripple-marks and crack-casts are displayed on the surfaces of 
 many beds. The sandstones and conglomerates become interstratified 
 with trap layers, and an enormous amount of trappean overflow crowns 
 the formation. 
 
 There appears to be some variation in the thickness of this overflow in 
 different parts of its distribution, as well as some diversity in the arrange- 
 
CHAP. V.] ROCKS OF LAKE SUPERIOR. 71 
 
 ment in regard to the interstratification of conglomerate layers. But stratified and 
 
 intrusi 
 traps. 
 
 sections examined in places widely asunder would not make the total mtrusive 
 
 volume fall far short of from 6000 to 10000 feet. The trap is in general 
 of an amygdaloidal character, less so at the bottom than higher up, while 
 at the top, in addition to the amygdaloid, there are met with intrusive 
 masses of a more solid and more highly crystalline character. These 
 appear in general to consist of greenstone, sometimes passing into well 
 marked columnar basalt, and they are associated with other masses of a 
 vitreous aspect, exhibiting the forms of pitchstone and pitchstone porphyry. 
 
 The stratification of the amygdaloidal layers is usually well marked, and 
 they do not in general appear to be individually so thick as the more 
 solid and crystalline beds. The rock, independent of the minerals filling 
 the cavities, has an earthy aspect in fresh fractures, but is probably a 
 greenstone. The minerals filling the cavities usually consist of calcspar, 
 quartz in various forms, agate being abundant, together with prehnite, 
 epidote, native copper, specular iron, and various zeolites : those ob- 
 served are red and white heulandite, stilbite, mesolite, laumontite, and 
 analcime. A chlorite-like mineral often occurs lining the walls of the cells. 
 The epidote and mesolite are met with associated with quartz and frequently 
 with specular iron, in the cells of the amygdaloid of Mamainse, the epidote 
 being occasionally, superimposed on the mesolite, and in one instance 
 perfect but minute dodecahedrons of cinnamon-stone garnet were ob- 
 served resting amidst crystals of the epidote. The cavities are of various 
 sizes and shapes : some containing agate, are six or eight inches hi 
 diameter, and others, of very irregular branching forms, are filled with 
 masses of native copper, sometimes weighing so much as eight or ten pounds. 
 Portions of native copper varying from the weight just given to grains no 
 heavier than snipe-shot, and abundantly disseminated through thicknesses of 
 one or more feet, occasionally keep the same stratigraphical place for con- 
 siderable distances, and constitute workable copper beds. Instances are occa- 
 sionally met with where the cavities, generally filled with calcspar, present the 
 shape of irregular vertical tubes of about a quarter of an inch in diameter, 
 running up into a bed for several inches, sometimes as many as twelve. 
 Near the base of the bed the tubes often approach to within half an inch of 
 one another ; but higher up two of them often join in one, and this may unite 
 with another which comes up singly from the bottom, or is perhaps the 
 result of the combination of other two or more, and so on. The combined 
 tubes appear to be a little larger than the original separate ones. None 
 of the tubes were seen to divaricate upwards. 
 
 On the surface of some of the beds partially concentric wrinkles, result- 
 ing from the flow of the volcanic matter when in a viscid condition, are 
 strongly marked. In one instance (5), on the east side of St. Ignace 
 Island, the courses indicated are N. 65 E. and N. 45 E., in two forms 
 
 . 
 
GEOLOGY OF CANADA. 
 
 [CHAP. V. 
 
 wrinkles on which inosculate on the same surface ; and on another and lower surface 
 
 beds of trap. near ^ game place ^ direction Q f & fl^ form ig g> 550 E j^ ^ 
 
 several directions, the parallelism of the separate beds, and the character 
 of the wrinkles, it appears probable that the general surface on which the 
 volcanic flow occurred was not far removed from horizontally. Another 
 instance was met with on the east side of the lake, where the direction of 
 
 5. WRINKLES ON A BED OF TRAP, ST. IGNACE ISLAND. SCALE ABOUT J-. 
 
 Columnar 
 dykes. 
 
 the flow indicated by the lines is about east, which is exactly contrary to 
 the dip of the highly inclined surface presenting it. 
 
 Though the last two described rocks, and indeed the whole series of 
 stratified deposits down to the gneiss, are all along the coast traversed 
 by a vast collection of dykes, yet in no instance have any of the overlying 
 or interstratified igneous masses been shown to have a direct connection 
 with these. There is often however a great similarity in the characters of 
 the dykes and some parts of the stratified traps, but these resemblances 
 are not always confined to the dykes and beds that are near to one another ; 
 and in some cases, while the dyke is found cutting one series of beds, the 
 stratified trap most resembling it is met with at a distance in another 
 series. 
 
 The dykes may be ranged under the heads of greenstone, porphyry, 
 and syenite ; but those of a porphyritic and syenitic character bear but an 
 insignificant proportion to the greenstone dykes, to which, in part at least, 
 the others are closely allied. The trap of the greenstone dykes is in 
 general more or less fine grained, often approaching to compact, and its 
 usual constituents are black hornblende and greenish-white feldspar, with 
 in most cases a greater or smaller quantity of magnetic oxyd of iron and a 
 small amount of iron pyrites irregularly disseminated. One of the porphy- 
 ries contains large crystals of feldspar disseminated through a base of green- 
 stone, the crystals often being spotted with small specks of hornblende. 
 Another of the porphyritic traps partakes of the character of a syenite. 
 In this a dark grey mixture of hornblende and feldspar, with magnetic oxyd 
 
CHAP> v.] ROCKS OP LAKE SUPERIOR. 73 
 
 of iron and iron pyrites, similar to the greenstone already mentioned, 
 incloses a multitude of irregular patches composed of red feldspar and of 
 quartz, generally hyaline, and rarely of an opaque white resembling 
 chalcedony. The quartz is also occasionally disseminated throughout the 
 matrix without the red feldspar. More rarely red feldspar occurs with- 
 out the quartz, and still more rarely small quantities of calcareous spar 
 are met with. The whole mass of the dyke however sometimes passes 
 into a uniform small grained mixture of red feldspar and green hornblende 
 with very little quartz, and ceases to have either a porphyritic or syenitic 
 aspect. A third variety of porphyritic trap, constituting some of the dykes, 
 consists of a very- fine grained mixture of red feldspar and quartz, holding 
 distinct and not very large crystals of the same minerals ; the quartz crystals 
 being colorless transparent hexagonal prisms, terminated by a pyramid 
 at each extremity, and rather uniformly disseminated through the mass. 
 No dyke of an amygdaloidal character has been observed. 
 
 The greenstone dykes, whether porphyritic or not, possess, without a 
 single observed exception, a well marked transverse columnar structure, 
 which is in general so truly at right angles to the plane of the dykes, that 
 their underlie can be correctly determined by it. This structure belongs 
 equally to them, whether their dimensions are great or small ; but the size 
 of the columns increases with the breadth of the dyke, which sometimes 
 attains 200 feet. The number of these dykes is very great : thirteen 
 of them, of good size, have been counted in the width of two miles, and 
 their parallelism for great distances is as remarkable as their number. 
 
 The directions of the greenstone dykes, as well as those of the other 
 
 6. INTERSECTION OF GREENSTONE DYKES, ST. IGNACE ISLAND. SCALE ABOUT -^, 
 C 
 
 a, a, a, Amygdaloidal trap. 6, 6, Dyke running with the stratification, 
 c, c, Dyke transverse to the stratification. 
 
 descriptions which have been mentioned, are in general two, one with the 
 stratification and the other transverse, changing with any important change 
 
74 GEOLOGY OF CANADA. [CHAP. V. 
 
 in the general strike ; and they appear to maintain what might be consid- 
 ered a continuation of these courses into the older sedimentary rocks, 
 with a less precise relation to their strike where stratified. The point of 
 intersection of the two sets of dykes has been seldom seen. In one 
 instance, however, (6,) on the island of St. Ignace, a dyke of eighteen 
 inches, coincident with the stratification, cuts another of nearly the same 
 breadth running transversely. Both of these possess a columnar struc- 
 ture, which has not been observed in the dykes of syenitic trap. 
 
 The dykes in general appear to be more durable than the rocks cut by 
 them, from which results a peculiarity in the geographical features of the 
 country. The destructive action of the water upon the coast is partially 
 arrested in its progress upon meeting with the dykes, and those which run 
 with the strike are in consequence often found to shield the shore for 
 considerable distances. They sometimes run out into long prongs or 
 promontories, with deep recesses behind them, or present a succession of 
 long narrow islands, which act as breakwaters in defending the neigh- 
 boring mainland ; and it frequently happens that a narrow breach having 
 been effected in a dyke, it will be found to be the entrance to a spacious 
 cove worn out on each side in the softer rock behind it. In almost all 
 these instances commodious harbors are the result, and it is mainly owing 
 to the presence of these dykes that so many such harbors exist on the 
 Canadian side of Lake Superior. 
 
 Metalliferous In addition to the dykes, a great many mineral veins intersect these 
 rocks. A very large number of these contain a greater or smaller 
 amount of various metalliferous ores ; and the indications which they pre- 
 sent are such as to render it certain that many parts of the country 
 characterised by them, will, sooner or later, rise into importance as a 
 mining region. The metals whose ores are met with are copper, lead, zinc, 
 and silver, with more rarely nickel, cobalt, arsenic, uranium, and molyb- 
 denum. 
 
 As in the case of the dykes, the mineral veins belong to two systems, 
 one coincident with the range of the rock masses, and the other transverse 
 to it. They are therefore parallel to the dykes. The cracks which the veins 
 occupy appear however to be of an age subsequent to that of the dykes, and 
 they sometimes run alongside of them, having the dyke for one wall and 
 the rock of the country for the other, while at other times they are wholly 
 independent of the dykes. As far as the investigations of the Survey 
 have gone, the transverse veins appear to cut those coincident with the 
 range of the rock, where the strike runs about south-west and north-east, 
 and from that to about west and east ; but on the east side of Lake 
 Superior, where the strata dip to the west or a little south of it, a sufficient 
 number of facts has not been ascertained to establish a rule with regard 
 to the intersection of the mineral veins. The displacements connected 
 
OHAP. V.] 
 
 ROCKS OF LAKE SUPERIOR. 
 
 75 
 
 with the transverse or northward and southward veins appear to be 
 greater in amount than those related to the eastward and westward veins ; 
 but it is not so certain that the dislocations connected with the dykes 
 follow the same rule. Some very important disturbances have been 
 observed in connection with those veins which are coincident with the strike 
 of the stratification. 
 
 In respect to the mineral contents of the veins, some differences exist 
 in the different parts of the series. In the upper group, which is so 
 much associated with amygdaloidal trap, the mineral veins vary in breadth 
 from a few inches to four or five feet. They are in general compo- 
 sed of calcareous spar and quartz, holding in greater or smaller quanti- 
 ties entangled fragments of the wall-rocks, and dark green saponite is 
 seldom absent. Laumontite is very often abundantly present with these 
 minerals, and sometimes exceeds them in quantity. Associated with the 
 veinstones, fluor spar occurs occasionally. Heavy spar is not unfrequently 
 met with ; and in some districts the latter occasionally forms the chief 
 earthy mineral in transverse or north and south veins. Prehnite, thom- 
 sonite, analcime, and apophyllite are frequently present, chiefly in east 
 and west veins; and wollastonite, orthoclase, and datholite are to be 
 enumerated among the minerals that occur. Some of the veins, both with 
 the strike and transverse to it, are almost entirely composed of chalcedony 
 and agate, where the rock of the country is allied to pitchstone or to 
 pitchstone porphyry; but these are seldom found to hold metalliferous 
 minerals. 
 
 When metals are present in the mineral veins, they occur chiefly in the 
 form of sulphurets, with the exception of the silver, which appears to be 
 usually in the native state, even when mixed up with the ores of other 
 metals, unless in the case of galena, where it is probably present as a 
 sulphuret. The copper also is frequently met with in a native state. It 
 usually however occurs in the forms of vitreous copper, variegated copper, 
 and copper pyrites ; but it is found also as a carbonate resulting from the 
 decomposition of the other ores where acted on by the weather at the 
 outcrop of a lode. The gangue in those lodes which carry vitreous 
 copper has usually a predominating quantity of calcareous spar or lau- 
 montite, and sometimes of heavy spar, while in those possessing pyritous 
 and variegated copper ores it appears to be of a more quartzose character. 
 Native copper is usually accompanied by prehnite, and often by epidote. 
 The silver is found associated with vitreous copper, native copper, and 
 galena, the last of which, with blende and iron pyrites, occurs in company 
 with the sulphurets of copper, and is sometimes met with in the calcareous 
 spar by itself. 
 
 The courses of the metalliferous veins of this upper group appear to be 
 different in different parts of the lake, although they preserve uniformity 
 
 Copper and 
 silver. 
 
76 GEOLOGY OF CANADA. [CHAP. V. 
 
 over considerable areas. On the north shore they run with the system of 
 veins coincident with the range of the rock-masses, partaking of an east 
 and west bearing. On Michipicoten Island they belong to the transverse 
 system, and run north and south ; while at the east end of the lake, besides 
 the principal lodes running eastward and westward transverse to the strati- 
 fication, there are others running northward and southward with the strike. 
 Veins of the In the lower group of this series the most conspicuous system of 
 er group. vemg cons i s tg O f those transverse to the stratification. They vary 
 in breadth from a few inches up to twenty feet and more, and are in 
 general composed of calcareous spar, heavy spar, and amethystine quartz. 
 Apophyllite is occasionally associated with heavy spar in some of the 
 veins, and dark green saponite occurs more or less in almost all. Several 
 of them are characterised by small quantities of vitreous, variegated, and 
 pyritous copper, iron pyrites, blende, galena, silver glance, and native silver ; 
 and on Prince's location, to the west of Fort William, one of the lodes, in 
 addition to all these metalliferous products, including a promising quantity 
 of the copper ore, holds cobalt and arsenic, with a little gold. The veins 
 coincident with the stratification and cut by these transverse veins, are in 
 % general rather thin. They often run side by side with the dykes, and seem 
 for the most part to consist of a breccia of the wall rocks, held together by 
 carbonate of lime and quartz, while saponite is frequently present. Green 
 and purple fluor spar are found in some of them, and prehnite associated 
 with thomsonite occurs in others. The only metalliferous minerals 
 observed accompanying them are iron and copper pyrites ; but it is doubtful 
 whether the quantity of the latter is sufficient to give promise of profit in 
 working them. One vein, coincident with the strike of the formation, 
 which occurs on the north-west side of Thunder Bay, appears however to 
 be an exception. It is of great breadth, perhaps not under sixty feet, and 
 in its general characters resembles the transverse veins ; its earthy min- 
 erals being calcareous spar, amethystine quartz, and heavy spar, while 
 at the same time it carries small quantities of iron and copper pyrites, 
 galena, and blende. 
 
 On Lake Superior, mineral veins, analogous to those which have been 
 described as belonging to this series of deposits, were found penetrating 
 the older rocks ; but the examination of these veins has scarcely been 
 sufficient to authorise any attempt to describe them. The veinstones 
 appear to consist chiefly of quartz and calcspar, with laumontite occasion- 
 ally ; and the metalliferous minerals, when any are found, are variegated 
 copper, copper pyrites, galena, blende, and molybdenite; but with 
 the exception of a district at the mouth of the Black River, nearly 
 opposite the Slate Islands, the lodes do not seem to be of such frequent 
 occurrence as in the higher rocks, nor are those which have been observed 
 of so important a character. 
 
CHAP. V,] ROCKS OF LAKE SUPERIOR. 77 
 
 The lower group composes the whole country, both islands and mainland, Distribution 
 between Pigeon Eiver and Fort William ; and the valley of the Kaministi- ^ lower 
 quia River, in the eastern part of its course, may be considered as the boun- 
 dary of its outcrop in this district. Eastward, on the main front of the lake, 
 it constitutes Pie Island and the promontory of Thunder Cape, reaching to 
 a point about six miles to the eastward of its extremity, where a transverse 
 dislocation lets down the succeeding group at least 1300 feet, bringing 
 it suddenly in to occupy the coast in the strike of the other. The lower 
 group however constitutes the whole of the bed of Thunder Bay, on 
 the north side of which the conglomerate layer at its base is seen to rest in 
 a nearly horizontal position upon the highly tilted chloritic slates of the 
 Huronian series beneath ; and in one spot it there evenly covers over, 
 without any disturbance, a step in these chloritic slates produced by an 
 ancient transverse fault. 
 
 On the same side, at the eastern extremity of the bay, the chert beds 
 belonging to the lower group occupy two miles of the coast. But the 
 whole volume of the group in this part appears to be gradually thinning 
 down ; for while between Thunder Cape (in which alone a vertical thickness 
 of 1300 feet is displayed) and the final outcrop of the base on the north- 
 western side of the bay there is a breadth of more than twelve miles, one 
 of no more than probably three miles would span the distance in the bight 
 of the bay between the Laurentian gneiss and the south-eastern cliffs, dis- 
 playing the lower white sandstones of the upper group, while the dip does 
 not increase in a ratio sufficient to preserve the volume which occurs to the 
 west. In corroboration of this, where a spur of gneiss comes upon Black Bay, 
 in the vicinity of Granite Islet, the bluish argillaceous slates are altogether 
 wanting, and the sandstones of the upper group are seen to come in con- 
 tact with the Laurentian rocks. And though the sandstones and the gneiss 
 to the eastward have been more than once detected in contact, the slates 
 have not again been observed in any place, with the exception of one, 
 where they form part of some of the islands in the Grand Detroit exit 
 from Neepigon Bay, to the north of the large centre island of the Battle 
 group, being those islands eastward of Simpson's Island. The thickness 
 of the slates there was not very important, and they probably do not 
 reach much farther in that direction. 
 
 Commencing at the Thunder Cape downthrow which has been mentioned, Distribution 
 the white sandstones at the base of the upper group constitute an 
 escarpment on the south-east side of Thunder Bay, and are displayed in 
 vertical cliffs rising to 200 feet above the water : they occupy about seven 
 miles on the same side, towards the north-eastern extremity of the bay. 
 The limestones and the indurated marls appear at a point about a mile 
 and a half eastward of the downthrow, on the south side of a tongue of 
 land separating Thunder Bay from Black Bay. Running parallel with the 
 
78 GEOLOGY OP CANADA. [CHAP. V. 
 
 sandstones, and dipping south-easterly at an angle of about three degrees, 
 they probably occupy the upper side of the latter bay. Here, however, 
 there is but little exposure of rock, a fringe of marshy land shielding much 
 of the coast. 
 
 Beds of red sandstone of a conglomerate character, associated with 
 layers of variegated red shale, are seen reposing on the gneiss of Granite 
 Islet. The conglomerate is composed of the ruins of the underlying rock, 
 and fills up the inequalities and worn fissures of the rock supporting it, 
 displaying a southern dip at an angle of about ten degrees. The variegated 
 shale is calcareous, and it is not improbable that a considerable part of 
 Black Bay may be worn out of the indurated marls. 
 
 The higher and more trappean part of the formation commences at Point 
 Porphyry ; and on Edward Island and other islands northward, grits and 
 conglomerates are found interstratified with trap layers. The same inter- 
 stratification is met with in the rocks bordering the south-east side of 
 Black Bay, while those fronting the lake on the south-east side of the 
 peninsula are composed almost entirely of various descriptions of conform- 
 ably overlying trap. This arrangement of the stratification, occupying a 
 belt of from seven to ten miles in breadth, (which on the lake front is carved 
 out into a multitude of deep coves, and includes a great collection of small 
 rocky islands,) runs in a north-easterly direction across Neepigon Strait, 
 from the mainland to St. Ignace Island. Gradually changing its direction 
 about the middle of this island to due east, it continues on through Simp- 
 son's Island, and farther to the eastern extremity of the Battle Islands. 
 Battle A high precipitous escarpment of red sandstone, with white bands and 
 islands. con gi omer ate layers, all interstratified with occasional beds of variegated 
 red shales, and having a pretty constant dip of eight or nine degrees to 
 the southward, keeps its place on the north side of each succeeding island 
 standing in the line, which curves a little to the south of eastward towards 
 the eastern extremity. A section from the gneiss through the large centre 
 island of the Battle group would shew in place both the blue shales and 
 the succeeding sandstones, apparently diminished in their proportions. 
 In the cliffs on the north side of the last island of the group the limestones 
 are displayed, associated with white sandstones and a conglomerate layer 
 beneath, resting on trap of a porphyritic character, and overlaid by more 
 porous volcanic products, the succession of the sedimentary part in ascend- 
 ing order being as follows : 
 
 Conglomerate and red sandstones, 30 feet. 
 
 Red and white shales and sandstones, TO " 
 
 Reddish or flesh-red limestones in beds of from two to twelve inches,. . 30 " 
 
 White sandstones, f " 
 
 200 
 
CHAP. V.] ROCKS OF LAKE SUPERIOR. 79 
 
 The isthmus which separates Black Bay from Neepigon Bay appears to 
 be entirely composed of sand and clay. But it seems not improbable, 
 from the direction which the spur of gneiss, already twice mentioned, 
 assumes in running out to Granite Islet in the first named bay, that an 
 undulation in the stratification connected with it in the superior rocks may 
 cross beneath the sand and clay, and carry its course betwe'en St. Ignace 
 Island and the two islands to the north, of which the western one is 
 called the Grange. No northern dip has been anywhere observed, but 
 this may be concealed by the loose material of the isthmus and the waters 
 of the bay ; and should such an undulation exist, or a dislocation represent 
 it, it is probable that the strata of the two islands would be a repetition of 
 those of St. Ignace. An escarpment of southward-dipping red sandstone 
 exists on the north side of them, and runs for the sandstone and the over- 
 lying trap on the mainland both to the east and the west ; while two miles 
 farther north, sedimentary strata, still dipping south at an angle of about 
 five degrees, underlie the perpendicular cliffs of columnar trap at the 
 mouth of the Neepigon River. These strata are very calcareous, and 
 probably belong to the limestones of the formation. The white sandstones 
 which are found at the base of the formation in Thunder Bay have not been 
 here observed to crop out. A considerable space however, probably upwards 
 of a mile, between the basset edge of the calcareous strata and the gneiss, 
 is occupied by a deposit of sand between sixty and seventy feet thick in 
 some places; but to the eastward the red sandstones of Grange Island 
 are seen reposing on the gneiss, without the intervention even of the 
 calcareous beds. 
 
 Where these beds and the sandstones associated with them are seen at 
 the outlet of the Neepigon, the overlying trap does not appear to be in a 
 perfectly conformable attitude. It seems to be more horizontal than the 
 sedimentary portion of the cliff. The slope of the beds, as stated, is about 
 five degrees ; and as they approach the base of the trap they appear to 
 become obliterated, some of them proceeding farther than others into the 
 igneous mass, but in such a manner that it is difficult to say where any 
 bed finally stops. 
 
 It seems not at all improbable that Isle Royal belongs in part to the 
 igneous portion of the upper group. Siscouette Bay occurs about mid-length 
 of the island, on the south side. The bight of this bay is at the foot of a 
 range of trap hills, whose course runs nearly north-east and south-west. 
 The area in front of them between Siscouette Bay and the south-western 
 extremity of the island is composed of red sandstone with conglomerate 
 layers. With a breadth of nearly three miles, they rest upon the trap, and 
 dip about south-east at an angle of ten degrees ; while the remainder of 
 the island in its whole length appears to consist of trap, much of which is 
 of an amygdaloidal character. The average breadth of this trap is about 
 
80 GEOLOGY OF CANADA. [CHAP. V. 
 
 six miles. The dip of the band appears to be greater than that of St. 
 Ignaee, and it is probably stated within the mark at fifteen degrees, the 
 bearing being to the south-eastward. The general strike is well marked 
 by the form of the island ; and the number of deep inlets which are worn 
 down in the softer beds at the lower or north-eastern extremity, the most 
 south-easterly of which is not under ten miles long, shews the great 
 parallelism of the different layers. The general position of the island and 
 the dip and strike would bring the whole mass to the front of St. Ignace 
 . Island, as if it constituted an addition to the volume of the formation ; but 
 it is perhaps a more probable conjecture that there is a trough between the 
 two positions, the northern slope of which is concealed by the waters of 
 the lake, and that Isle Royal constitutes only a repetition of the Neepigon 
 peninsula and archipelago. 
 
 Proceeding eastward, the mass of trap which has already been men- 
 tioned as flanked on both sides by the chloride slates in the north-eastern 
 corner of the lake, in the vicinity of Anse a la Bouteille and the Old 
 Pic River, may belong to the formation ; but of this there is some doubt. 
 In a straight line across from one side to the other on the coast, it occupies 
 a space of about fourteen miles. No rocks of a sedimentary character 
 have been observed to be associated with it ; but its stratification is very 
 distinctly marked, with a dip south-westerly of about twelve degrees. Its 
 character differs in different places ; but no portion of it was observed to be 
 amygdaloidal, except one bed, which exhibited a transverse columnar 
 structure. The rock in general appears to approach in character the 
 more solid and crystalline trap which overlies the amygdaloid towards the 
 lake front of the Neepigon and St. Ignace band. 
 
 On the upper or western side, the mass is brought into position by an 
 outburst through the chloritic slates, which are well displayed on the main 
 shore at a point nearly due north of the western extremity of Pic Island. 
 The trap there abuts against the chloritic slates. On approaching them, its 
 feldspar, constituting the predominant mineral, assumes a red color with 
 occasional opalescence, and strongly contrasts with the brilliant black 
 hornblende disseminated through it, while among its accidental minerals 
 the rock contains a few zircons. In the first hundred yards near the 
 junction, the slates appear to be shivered and broken into a very coarse 
 breccia, of which the interstices are filled with trap of this character, 
 while in the second hundred yards they are cut up by a number of 
 irregularly parallel, though somewhat ramified dykes of the same, having 
 a general northerly direction, which is that of the dingle marking the 
 course of the junction of the two rocks. At a distance from the junction 
 the trap is still coarse grained ; but the general color of the feldspar is a 
 dull green, with black hornblende, and magnetic oxyd of iron. The 
 columnar bed has occasional large patches of a red color, holding red 
 
CHAP. V.] ROCKS OF LAKE SUPERIOR. 81 
 
 feldspar, white quartz, and black hornblende ; but the general color of the 
 matrix in which these are imbedded, is a chocolate-brown, resulting from 
 the feldspar which constitutes the chief part of the mass, in which small 
 cells are filled with calcspar and red and white zeolites, while well defined 
 slender acicular crystals of black hornblende are abundantly disseminated 
 through it. The rock above and below is composed of brownish feldspar 
 and black hornblende, but it is not so compact as the other. It is large 
 grained, and the general mass of the country constituting the Old Pic 
 Point and Island appears to be composed of it. Fluor spar occurs as a 
 disseminated mineral in some of the beds. Judging from fragments on 
 the shore, there are some beds composed of white feldspar, with occasional 
 groups of orange-red grains of elaeolite, the whole studded with brilliant 
 black crystals of hornblende, forming a very beautiful rock. The general 
 mass of these igneous rocks weathers to a red, and from a distance may 
 readily be' mistaken for the gneiss which underlies the chloritic slates. 
 The hills which they form however are not quite so rugged as those result- 
 ing from the older rock. 
 
 Much to the south and a little to the east of this is Michipicoten Island, 
 another mass of trap belonging to the upper group. The strata of Islard 
 which it is composed have a general dip to the east of south, and the 
 inclination appears seldom to fall short of thirty degrees. The lower 
 strata towards the north side of the island, particularly as indicated at the 
 upper end, appear to be composed chiefly of amygdaloidal trap, with 
 occasional beds of trap conglomerates, red sandstones, and shales ; while 
 towards the south these are overlaid by a considerable amount of compact 
 earthy or sub-resinous red trap, assuming sometimes an obscure and 
 sometimes a distinct porphyritic character, by the display of ill defined 
 crystals of red feldspar or well marked crystals of transparent colorless 
 quartz. 
 
 Along nearly the whole of the south side of the island the trap assumes 
 a more resinous aspect, and, its color becoming black, it presents the 
 characters of pitchstone and pitchstone porphyry. Some of the beds 
 associated with these are of an amygdaloidal character, and exhibit large 
 agate veins, which run chiefly in the direction of the strike, but frequently 
 also transverse to it. 
 
 About three fourths of a mile out in front of the harbor, which is half- 
 way down the south side, a few narrow islands occur, presenting beds 
 of a peculiar character, amounting to between sixty and seventy feet, 
 dipping southward at an angle of twenty degrees. They are of a 
 general red color, spotted and patched with yellowish-white, and where- 
 ever a crack exists the rock is blanched to a small distance on each side 
 of it. The surfaces are uneven, and peculiarly marked with festooned and 
 finely wrinkled forms, composed of very thin close-fitting laminae with a 
 
 F 
 
82 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. V. 
 
 Cape Gargan- 
 tua. 
 
 ligneous aspect, having a thickness sometimes exceeding one or two inches. 
 The rock scarcely resembles a trap, nor does it bear the character of 
 indurated shale ; but it may perhaps be an indurated mixture of volcanic 
 mud and ashes, in which the wrinkles result from a partial flow. The 
 total volume of the formation developed in Michipicoten Island, at the 
 most moderate dip observed, would not fall short of 12,000 feet. 
 
 On the east side of Lake Superior, white and red sandstones are seen 
 at several points, as also beds of amygdaloidal trap, with coarse 
 interstratified greenstones. The sandstones, except when in the vicinity 
 of disturbances from dislocations, appear to be much less tilted than the 
 trap and coarse conglomerates. Both have a dip westward ; but the facts 
 ascertained are not yet quite sufficient to determine in what precise 
 relation the two rocks stand in regard to one another. About two miles 
 cape choyye. north of Cape Choyye a coarse grained bed, supporting some thickness of 
 sandstone colored red, with white bands, and dipping a little to the south of 
 west at an angle of about ten degrees, abuts against a precipitous cliff of 
 the older rocks, as if let down by a north-east and south-west fault. 
 
 About nine miles to the south of this, the peninsula of Cape Gargantua, 
 and some of the small islands immediately near, display amygdaloidal trap 
 disposed in beds dipping to the south of west at an angle of about forty 
 degrees, and resting unconformably on the gneiss. Farther on, Leach, 
 Lizard, and Montreal Islands, as stated by Bayfield, are composed of 
 sandstone, but the attitude of the strata has not yet been ascertained ; it 
 seems probable however that the flatness of their geographical surface 
 may be occasioned by the absence of any great slope in their constituent 
 strata. 
 
 To the south of Montreal Island, sandstones and amygdaloidal trap 
 occupy the lower side of the cove above Pointe aux Mines. The sandstones, 
 where first seen, are nearly in contact with the gneiss, against which they 
 appear to abut, as if brought in by a dislocation. Their dip, at an angle 
 varying from ten to twenty degrees, gradually changes from a direction N. 
 45 W., to N. 15 W. The trap, coming apparently from below, after an 
 interval of about one hundred yards, in which it is difficult to ascertain its 
 true attitude from its being worn down level with the surface of the water, 
 exhibits a decided dip S. 80 W. < 30 40, maintained for such a 
 distance across the measures as to yield a thickness of 3000 feet. This 
 trap is interrupted at Pointe aux Mines by a south-easterly dislocation 
 which brings up the Laurentian gneiss, of which the extremity of the point 
 is composed. From this point the line of demarcation between the gneiss 
 and the overlying unconformable rocks, as has already been indicated, 
 appear to run across in a south-easterly direction to Batchehwahnung 
 Bay, leaving the promontory of Mamainse between it and the lake. 
 
 Pointe aux 
 Mines. 
 
CHAP . v.] ROCKS OP LAKE SUPERIOR. 83 
 
 This promontory is composed of amygdaloidal trap and coarse interstrat- 
 ified conglomerates, whose pebbles and boulders consist chiefly of the 
 ruins of the subjacent slate, gneiss, and associated rocks. The general 
 dip of the strata which occupy this area is maintained with considerable 
 constancy in a direction rather south of west, at an angle of twenty or 
 twenty-five degrees, and the breadth across the measures is sufficient to 
 give a thickness probably of not far from 10,000 feet, of which about 1500 
 feet consist of conglomerate layers, one of them being 400 feet. On the 
 south side of the promontory, approaching Anse aux Crepes, irregularities 
 prevail, and sandstones in a disturbed condition approach the trap, but 
 keep to the lake side of it. 
 
 Between this point and Sault Ste. Marie, stratified amygdaloidal trap coast to sauit 
 has been observed in three places. The first is in the most eastern part ste ' Mane * 
 of Batchehwahnung Bay, where it. reposes on the gneiss with a dip 
 S. 80 W. < 42. The second is in a cove between two and three miles 
 to the east of the southern boundary of the same bay. The worn condition 
 of the rock renders the dip obscure, but it appears to be N. 60 W. < 22. 
 A hilly surface rises behind it belonging to the Huronian series. The 
 third position is at the extremity of Gros Cap, where there is but a small 
 quantity of the amygdaloidal, and where trap of a porphyritic character 
 appears to be associated with it. The dip is W. < 45. 
 
 The sandstones in the same distance constitute the promontory between 
 Anse aux Crepes and Batchehwahnung Bay. They probably underlie 
 also the large island of this bay, and, with the exception of the interval 
 occupied by the trap in the cove at the southern entrance of the bay, 
 compose the coast from a point three miles to the east of the cove round 
 to Goulais Bay, underlying the whole of Goulais Promontory and Maple 
 Island. A narrow strip of the rock is found also leaning against the gneiss 
 on the south side of Goulais Bay, extending seven miles along the coast 
 towards Gros Cap, and dipping gently to the north-westward not quite in 
 the direction of Isle du Parisien, which is also composed of the rock, with 
 a dip of two or three degrees in the direction of White-fish Point. 
 
 In every instance the geographical surface of the sandstones on the 
 east side of the lake is low and flat ; and their geographical position in 
 relation to the stratified trap would seem to indicate that they overlie the 
 latter, but whether conformably is not yet satisfactorily ascertained. 
 Their presence, as stated by Bayfield, in Caribou Island, seven leagues 
 south of Michipicoten Island, and more than twice as many east of Mont- 
 real Island, makes it probable that their spread may be considerable under 
 the waters of the lake, while sandstones occupy a great extent on the 
 south shore. The geologists of Michigan represent them to exist at 
 intervals from the vicinity of Point Iroquois to Grand Island, in which 
 latter spot they are capped by fossiliferous limestone. On this coast at 
 
GEOLOGY OF CANADA. 
 
 [CHAP. V. 
 
 St. Mary. 
 
 Campement 
 d'Ours. 
 
 the mouth of the Dead River, north of Marquette, there is a mass of very 
 ferruginous dolomite, of which the stratification is not very distinct ; but it 
 is overlaid by the sandstone which fills up inequalities in the surface of 
 the dolomite, and dips at a moderate angle to the south-west. The 
 dolomite is cut by what appears to be a vertical dyke, which, instead of 
 intersecting the sandstone, abuts against the bottom of it. 
 
 Sandstones of The same red sandstone, interstratified with greenish and whitish 
 layers, is observed in various parts of St. Mary Kiver, between Sault 
 Ste. Marie and Sugar Island. To the south-eastward of the lower end 
 of Sugar Island the boundary of the sandstone is covered by drifted 
 boulders or by over-growing moss and forest trees; yet there is evi- 
 dence in the character of the loose material that the formation extends 
 to the eastern side of Sugar Island, and that, striking into the island of 
 St. Joseph near the north-western extremity, its basset edge runs nearly 
 east, and comes out again on the north coast of the island, about two miles 
 south of the island of Campement d'Ours. On Campement d'Ours there 
 is an outlying patch of the rock resting in a nearly horizontal attitude on 
 Huronian quartzites. It has a thickness of about eighty feet, and consists 
 of whitish and brownish slightly calcareous sandstone, with a two-feet bed 
 of a pinkish color towards the top ; and both here and on the island of St. 
 Joseph the sandstone is overlaid by limestone well marked by fossils. 
 
 The sandstone is again seen at the east end of the North Channel on 
 the island of Lacloche, as well as on the point of the long promontory 
 that comes down towards the island from the mainland. The rock in 
 this neighborhood is from twenty-five to thirty feet thick, and consists 
 at the base of about ten feet of red and green shales, interstratified with 
 thin bands of green-spotted red sandstone, and followed by about sixteen 
 feet of drab and greenish-white slightly calcareous sandstone, in beds of 
 from four to six inches, separated towards the bottom by thin layers of 
 red and green shale. To these succeed between one and two feet of red 
 calcareous sandstone, holding a few of the fossils which characterize the 
 magnesian limestones immediately above, and thus constituting a passage 
 between the two deposits. A narrow strip of the sandstone runs east 
 along the south side of a ridge of Huronian quartzite through the island 
 of Lacloche ; it then spreads over a portion of the north-east corner of 
 that island, extending thence across the peninsula of the mainland oppo- 
 site, where it rests upon the edges of the tilted slates of the Huronian 
 series, and there constitutes the most eastern exposure of the rock obser- 
 ved on the lake. 
 
 The precise age of the upper copper-bearing rocks of Lake Superior is 
 a question attended with some difficulty. Mr. Whitney appears disposed 
 to regard the whole series from the summit of the sandstones of Sault 
 Ste. Marie to the base of the Kaministiquia slates as one group equiv- 
 
 Lacloche. 
 
 Age of the 
 series. 
 
CHAP. V.] ROCKS OP LAKE SUPERIOR. 85 
 
 alent to the Potsdam formation ; but the suspicion of a want of conform- 
 ity between the Sault Ste. Marie sandstones and the trappean rocks 
 beneath, would induce us to separate the two. The difficulty in coming 
 to a conclusion arises from the want of fossils ; none of a satisfactory kind, 
 it is believed, having been obtained, either on the north or the south side 
 of the lake, from beds whose relation to the well ascertained interstratified 
 igneous beds is undoubted. 
 
 There does not appear any reason to doubt that the red sandstones of 
 Lacloche and of Sault Ste. Marie are the same, and that the latter, extend- 
 ing with a low dip to the foot of Gros Cap Mountain, strike over to Point 
 Iroquois. The nearly flat sandstones met with between this promontory 
 and Grand Island, with the fossiliferous limestones overlying them in the 
 latter locality, appear to present conditions corresponding with those at 
 Campement d'Ours and Lacloche ; and the presence of similar sandstones in 
 the various low islands and peninsulas on the Canadian side, to the east and 
 the north, would seem to make it probable that the rock has a still farther 
 extension in those directions. At the same time, the contrast between 
 the general moderate dips of these sandstones and the higher inclination of 
 the igneous strata at Gargantua, Mamainse, and Gros Cap, combined with 
 the fact that the sandstones always keep to the lake side of these, while none 
 of the many dykes which cut the trappean strata, it is believed, are known 
 to intersect the sandstones (at any rate on the Canadian side of the lake), 
 seem to support the suspicion that the sandstones may overlie unconform- 
 ably those rocks which, associated with the trap, constitute the copper- 
 bearing series. 
 
 From the western extremity of Lake Superior, the trappean strata 
 appear to strike eastward with considerable regularity for 300 miles, until 
 they pass Michipicoten Island and reach the eastern coast. Here the 
 strike suddenly changes to a bearing at right angles to its previous course, 
 with an upward slope to the eastward sufficiently rapid to bring 10,000 
 feet of strata to the surface at Mamainse, in no very great distance across 
 the measures. This sudden change of strike, and its accompanying 
 phenomena, have much the aspect of a great dislocation, or it may be 
 a great undulation. Its effects are apparent for nearly a hundred miles 
 along the east coast of the lake, and at the extremity of Gros Cap are vis- 
 ible to within a few miles of the overlying red sandstone. 
 
 If the overlying red sandstone were of the same age as the trappean 
 formation and conformable with it, it ought naturally to be affected by the 
 disturbance ; and the very moderation of its dip should carry it a great 
 way to the south, on the east side of the displacement. There appears 
 however to be no irregularity whatever in the direction of the summit of 
 the sandstone, which is represented as proceeding in a straight line to the 
 westward, across St. Joseph and Neebish Islands, and thence into the 
 
88 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. VI. 
 
 Hemming- 
 ford; con- 
 glomerate 
 with shale. 
 
 Flagstones. 
 
 Blueberry 
 Plain. 
 
 rock is a very pale reddish fine grained sandstone, yielding excellent, 
 material for building, and large slabs for flagging and coping. 
 
 Hemmingford Mountain in Canada, close upon the boundary of the 
 province, though it does not reach the base of the formation, displays a 
 thickness of 540 feet of this rock. In a deep ravine on the south side 
 about 180 feet of a ( coarse grained sandstone are visible, in some parts 
 constituting a conglomerate, with rounded pebbles of white quartz varying 
 in diameter from an eighth to three quarters of an inch, while inmost parts 
 of the rock there are thinly disseminated flat pieces of black or green shale 
 one or two inches in diameter by an eighth of an inch thick. The general 
 color of the rock is grey, but greenish and reddish beds occur, and the 
 three colors sometimes follow one another in thin stripes with various 
 alternations. Some parts of the rock crumble in the weather to a yellow 
 or brown sand. One bed of about three inches thick, near the base 
 of the mass, contains a good deal of blackish-brown mica, with a few 
 silvery white scales of the same mineral. Above the strata of the ravine 
 the hill contains about 120 feet of grey sandstone, the lower half of which 
 is rather coarse grained, and below the same strata 240 feet. The dip is 
 northward, and, though at a very small angle, there would still be some- 
 thing to add to the thickness of the formation for that portion which comes 
 to the surface on the south of the province line. 
 
 About three miles north of this, on the third range of Hemmingford, 
 exposures of the rock present a grey color, with an occasional streak of 
 brown, and weather to a light grey or greyish-brown. The greater part 
 may be called a conglomerate, with rounded, translucent, white quartz 
 pebbles varying in size from an eighth of an inch to an inch in diameter, 
 and small masses of white or brown feldspar enclosed in a fine grained 
 matrix of quartz and feldspar -of much the same color. The beds are from 
 nine inches to two feet thick, and some of them are altogether composed 
 of the fine grained material. In the course of eight or nine miles to the 
 westward of these beds there are several exposures of sandstone. One of 
 these displays beds from an inch to a foot thick of pure silicious sandstone, 
 some of which would yield good flagstones of moderate size. The rock is 
 in general fine grained, with occasional pebbles as large as peas. In 
 another of the exposures, the rock is a light grey fine grained sandstone, 
 in beds varying from two inches to two feet, some of which have grains 
 the size of pin heads. Some of the beds are very slightly calcareous, a 
 few of them shew ripple-marks, and many of them fucoids. The rock in 
 many parts weathers to a pale brown or yellow, and a thin coating on 
 some of the surfaces is converted under atmospheric influences into a 
 yellow ochre. 
 
 On Blueberry Plain, on the line between Jamestown and Russeltown, 
 where there is an exposure of seven square miles of the rock, showing 
 
CHAP. VI.] POTSDAM GROUP. 89 
 
 however from its approach to borizontality no great thickness, the sand- 
 stone is in general light grey in color, many parts becoming opaque 
 white by exposure to the weather. The rock is in general fine 
 grained, but contains occasional white quartz pebbles of half an inch in 
 diameter. Some of the beds, on fracture, are seen to be much stained 
 with brown and yellow spots ; but the beds which bleach white are free 
 from these stains, and would answer the purpose of glass-making. Some stone for glass- 
 beds would yield tolerably good flagging-stones from two to four inches m 
 thick ; but the strata in the greatest part of the exposure are from one to 
 three feet thick, and many of them shew false bedding. 
 
 The upper part of the formation is in general a fine grained, white, 
 eilicious sandstone, some parts of which are sufficiently pure to yield an 
 excellent material for glass-making. It abounds in durable building stone, Fumace- 
 and in several places becomes of so free a texture as to furnish a stone h< 
 capable of resisting great heat without cracking or fusing, and thus to be 
 eminently adapted for furnace-hearths 'in the manufacture of iron. The interstrat- 
 formation attains a thickness ranging from about 300 to 700 feet, and at ifiedlime - 
 
 stones. J 
 
 the summit the sandstone becomes by degrees interstratified with beds of 
 magnesian limestone, and presents a passage to the succeeding formation. 
 It is stated by Professor Emmons, that connected with the summit of the 
 formation there is at Chazy a calcareous breccia formed partly of sandstone 
 and partly of fragments of a dirty grey calcareous rock. This is given by 
 him as one of the characteristics of the formation at its junction with the 
 succeeding one. To the east of Hemmingford Mountain, on the twenty- 
 ninth lot of the second range of Hemmingford, there occur, in an area 
 of which the diameter is less than half a mile, several exposures which appear 
 to be of a somewhat similar character. In one of these, fragments of grey 
 sandstone, some of which are calcareous and others not, accompanied by 
 white quartz pebbles, are imbedded in an arenaceous cement, and some of 
 the included fragments are a sandy limestone holding other fragments 
 of a less calcareous character. Beds of arenaceo-calcareous rock seem 
 to dip under the breccia, and the whole appear to be on the top of a bed 
 of sandstone which is seen within five paces of the mass. Several of such 
 patches occur not very distant from one another ; and the intervals, which 
 are always at a somewhat lower level, seem to be occupied by sandstone. 
 Within the area to the westward, a mound of breccia contains angular and Breccia, 
 rounded masses of grey bituminous limestone, weighing from a few ounces 
 to two and three tons, with others of sandstone ; the whole being included 
 in a matrix in some parts of black bituminous shale, and in others of black 
 bituminous limestone ; both of which, as well as most of the inclosed calca- 
 reous blocks, contain fossils, which appear to be of the Trenton forma- 
 tion. The rock seems to be folded into wedge-shaped masses, so that it 
 is very difficult to arrive at the means of establishing an average dip. The 
 
90 GEOLOGY OP CANADA. [CHAP. VI. 
 
 surface here rises into a mound of abeut thirty feet over the general 
 level of the neighborhood. On the east side of the area including these 
 brecciated masses, there occurs an exposure of about sixty feet wide, in 
 which the greatest confusion prevails, and brecciated limestone is seen abut- 
 ting against beds of sandstone, sometimes in such a manner that they might 
 be mistaken for a continuation of the same beds. Wherever the breccia 
 occurs, it is usually more or less raised above the general surface around ; 
 and throughout the whole area wherever a rock is seen in the intervals 
 among the mounds, it usually consists of sandstone apparently in an undis- 
 turbed attitude. In this attitude the sandstone extends nearly seven miles 
 to the eastward, and where it becomes covered by the succeeding rock no 
 breccia is observed. The presence and character of the fossils would 
 appear to indicate that the masses of breccia at Hemmingford are probably 
 connected with some complicated set of dislocations, rather than with any 
 continuous bed spreading over the sandstone. 
 
 Distribution. Resting on the gneiss of the Adirondack mountains, the Potsdam forma- 
 tion, in its distribution in New York, sweeps round from Keeseville on the 
 Ausable, a tributary of Lake Champlain, to Alexandria on the St. Law- 
 rence, in Jefierson county. In this distance of nearly 140 miles, the band 
 displays a breadth varying from about five to fifteen miles, with a general 
 northerly dip at a small angle. From this general line, through the effect 
 of a low anticlinal form, it is projected northward into Canada across the 
 
 Beauharnois. county of Beauharnois, and twenty miles farther across Lake St. Louis 
 into the county of the Lake of Two Mountains. On the province line, 
 from the summit on one side of the anticlinal to the summit on the other, 
 the formation occupies about forty miles ; but its breadth gradually diminishes 
 northward, and in the neighborhood of Beauharnois village it does not 
 exceed four miles. 
 
 Fossil tracks. From fifty to seventy feet below the top of the formation, the surfaces of 
 some of the strata are marked by the tracks which have been desig- 
 
 Proticimites. nated by the name of Proticlinites. A locality of these is in a field 
 on the land of Mr. He*nault, near Beauharnois. From this the sandstone can 
 be traced along the margin of Lake St. Louis for two and a half miles to the 
 mouth of the Beauharnois canal ; and by a careful admeasurement of dis- 
 tances and of the minute changes that occur in the very moderate dips 
 prevailing, it would appear that a surface shewing similar tracks in a field 
 about a quarter of a mile from the margin of the lake and on the north side 
 of the road, is in about the same stratigraphical place with the bed at 
 Renault's, while the positions of the two localities are equivalent in relation 
 to the outcrop of the overlying Calciferous formation on each side. 
 
 Another locality of the tracks is met with in the vicinity of Pointe du Grand 
 Detroit in Vaudreuil, and a bed of red sandstone occurring not far from it 
 probably occupies a lower stratigraphical position. This locality is about 
 
CHAP. VI.] POTSDAM GROUP. 91 
 
 twelve miles from that at the Beauharnois canal, and, like it, is on the west 
 side of the anticlinal axis. Another locality in which the same track-bed 
 is met with is on one of the islands of Ste. GeneVieve, between two and three 
 miles east of Ste. Anne, at the upper end of the island of Montreal. This 
 spot is about seven miles from the exposures at Beauharnois village, and 
 like them is on the east side of the axis. The locality at Ste. GeneVive, 
 which is not a mile from Isle Perrot, is marked by Scolithus, with which the 
 rock is in some parts completely honey-combed to the depth of three feet, 
 while it is also irregularly interstratified with calcareous bands. Ste. Anne 
 Point may be considered in the strike of the Ste. Gen^vieve locality, and 
 here we still find the sandstone marked by Scolithm ; while in Isle Perrot 
 opposite, thin bands of red sandstone occur similar to those of Pointe du 
 Grand Detroit. 
 
 At this part the breadth of the sandstone is about ten miles, extending Ca ivaire and 
 from Ste. Anne to a position in Vaudreuil ; but it gradually swells to about Rigaud 
 twenty miles towards the upper end of the Lake of Two Mountains, where 
 it occupies about equal spaces on the opposite sides of the lake. On the 
 left side of the lake there protrudes through the sandstone about fifty 
 square miles of Laurentian gneiss, constituting Mont Caivaire ; and on the 
 other side about a square mile of the same rock occurs, leaning against an 
 intrusive mass of trap, which there pierces the Potsdam formation and 
 composes Rigaud Mountain. 
 
 From Alexandria, on the St. Lawrence in New York, the Potsdam for- 
 mation reaches the Canadian side of the river, about twelve miles lower 
 down the stream, in the neighborhood of Brockville. From this it is trace- 
 able, by a multitude of exposures, running in a meandering course to the 
 vicinity of Perth ; the bays and promontories of its geographical distribution 
 being occasioned partly by inequalities in the surface of the Laurentian 
 gneiss supporting it, and partly by very gentle undulations in itself. In this 
 course its most western position is the northern part of Bedford township. 
 
 The cliffs below Brockville expose a sequence of from seventy-five to Brockville. 
 eighty feet thick, consisting of sandstone with interstratified dolomitic beds 
 at the top, and a coarse silicious conglomerate at the base. About two and 
 a half miles above the town an outlying portion of the formation comes in on 
 the river bank, and, occupying it for seven miles up, occasionally shews the 
 silicious conglomerate in unconformable contact with the Laurentian series 
 below. Many of the upper and finer beds of these exposures exhibit fucoids 
 on their surfaces, and the small cylindrical holes of Scolithus Canadensis. 
 Fragments of shells also occur in some of the interstratified calcareous 
 layers, but they have invariably been found to be too obscure to be identified. 
 
 At Charleston Lake there is an extensive development of the formation 
 on the north shore, and outliers occur on many of the numerous islands 
 which stud the lake. On one of these, commonly called Bluff Island, 
 
92 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. VI. 
 
 Lansdowne ; 
 
 Hematite. 
 
 a mile south-west of Charleston village, the following descending section 
 occurs : 
 
 Ft. in. 
 Sandstone, blood-red at the top and chocolate-red at the bottom, with nodules of 
 
 quartz, weathering brown, on the upper surface, 4 
 
 Thin bedded white, red, and chocolate-brown sandstone, 4 
 
 Red and greyish or white sandstone in alternating stripes, 4 3 
 
 Dark pinkish-brown sandstone, occasionally striped with blood-red, 5 7 
 
 Red and dark brown sandstone, 5 
 
 Blood-red coarse sandstone with concretionary nodules, 2 
 
 Dark brown, red, and yellow banded coarse grained sandstone, divided into thin 
 
 layers, 11 
 
 Red and yellow sandstone in alternating stripes in thin layers, 7 3 
 
 Red and yellow striped and mottled sandstone,' of a coarse grain, not well ex- 
 posed, 11 
 
 Red coarse sandstone with quartz pebbles scattered through it, 2 6 
 
 Dark yellow coarse sandstone striped and mottled with red ; the upper part is 
 
 red, and holds large quartz pebbles scattered through it, 3 6 
 
 A conglomerate bed with a matrix of dark brown and yellowish coarse silicious 
 sandstone, sometimes tinged with pink, holding pebbles and boulders, chiefly 
 of quartz, in irregular layers ; the largest boulders are one foot in diameter, 8 
 Dark brown coarse sandstone or fine conglomerate, with pebbles chiefly of white 
 
 quartz, resting on red talco-quartzose rock of the Laurentian series, 2 11 
 
 71 
 
 The infiltrating iron oxyd, which has stained the red talco-quartzose 
 rock at the base of the section, seems to have imparted its color to the 
 overlying mass ; and in some parts of the lake the color of all the lower 
 beds, both sandstones and conglomerates, is deep blood-red, which grad- 
 ually gives place in the ascending strata to white with red spots and stripes, 
 and then to white alone. On the eleventh lot of the eleventh range of 
 Lansdowne, at the head of one of the northern bays of the lake, there is a 
 section of about forty feet thick, consisting of white sandstone with shaly 
 and slightly calcareous layers at the top, and conglomerate below, which 
 is seen in contact with the Laurentian rocks ; but notwithstanding the pres- 
 ence of these, which are brought into place by the uneven surface of the 
 series, the white sandstones are at a higher level in the sequence than the 
 highest beds of the previous section. These white beds are therefore to be 
 taken as additional strata, and the two together would give a total thick- 
 ness of at least 110 feet. Fucoids, Scolithm Canadensis and Lingula acu- 
 minata are found associated together in abundance in the upper shaly 
 calcareous part ; but the last is sometimes rather obscure. 
 
 There is likewise a large display of sandstones and conglomerates in the 
 township of Bastard near Beverly, where the red color prevails near to the 
 contact with the older rocks. One exposure occurs on the line dividing 
 the twenty-fourth and twenty-fifth lots in the tenth range of the township. 
 near the town line of Lansdowne, where there is a cliff of sandstone of from 
 
CHAP. VL] POTSDAM GROUP. 93 
 
 twenty to thirty feet high. The rock lies in massive beds, occasionally 
 measuring four feet and upwards in thickness. They are all ferruginous, 
 and, passing upwards from a yellow or light brown into a deep red color, 
 they present small seams and patches of red hematite. On the ninth lot of 
 the twelfth range of Lansdowne also, the same rocks c6ntain patches of 
 hematite, a short distance from their junction with the Laurentian limestone 
 beneath. North from Beverly on the twenty-second lot of the ninth range Bastard 
 of Bastard, white sandstone beds, which must be higher in the series than fossils - 
 the preceding, contain fucoids, Scolithus Canadensis., and in a full state of 
 preservation, Lingula acuminata^ith some of the valves much less tapering 
 to the beak than others, the one being probably the upper and the other 
 the lower valve of the same species. Lingula occurs also in a cliff near 
 Newboro', a short distance from the town line of North and South Crosby. 
 From the neighborhood of Perth, where the sandstone is white, and 
 displays Protichnites, the outcrop of the formation proceeds northward, 
 and then, sweeping round to the head of Otty Lake, in Drummond, returns 
 southward in the townships of Elmsley and Montague, where the sand- 
 . stones are seen encircling a protruding mass of Laurentian gneiss, which 
 rises on the twenty-eighth lot of the sixth range of Montague. The out- 
 crop thence runs northward again to Otty Lake; following it towards the 
 lower end. From this it runs across Ramsay into Pakenham, where it 
 becomes overlapped by the succeeding formation. Westward of the village 
 in this township, however, it appears to surround a shallow synclinal out- 
 lying mass of Lower Silurian strata, which extends in a bearing westward 
 of north, from Ramsay nearly across Pakenham. 
 
 Between this and the Lac des Chats the formation is apparently over- Abse nce of 
 
 lapped by higher members of the Lower Silurian deposits ; and it does not sandstoue. 
 
 appear at the base of the various outliers of these higher formations 
 
 which occur from ten to fifty miles to the north-westward, occupying the 
 
 island of Allumettes, and parts to the east and the south of it. The formation 
 
 would thus appear not to have been deposited much farther north in this 
 
 part than the township of Pakenham. It is met with, however, to the 
 
 eastward, between Lake Chaudiere and a spur of Laurentian rock from 
 
 three to five miles removed from the right bank of the lake, and extending 
 
 from Lac des Chats to Nepean, a distance of twenty miles. The northern 
 
 side of this spur forms the surface over which the waters of the Lac des 
 
 Chats are precipitated into Lake Chaudiere ; and at the foot of the cascade 
 
 the Calciferous formation comes up against the gneiss. The two rocks 
 
 continue in contact for about four or five miles to the southward of east ; 
 
 but then become separated by the gradual emergence of the Potsdam 
 
 formation, which flanks the Laurentian rock in a narrow band all the way 
 
 from Tarbolton to Nepean, thence continuing eastward across this township, 
 
94 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. VI. 
 
 and running a short way into Gloucester, where, instead of the dislocation, 
 the Potsdam shews an anticlinal arch. 
 
 In Nepean the rock dips northward, and in that direction sinks beneath 
 the Calciferous formation ; but the south side of the band, after leaving 
 the gneiss, is brought by a dislocation against the Chazy and Trenton 
 formations, and the continuance of this dislocation on the south side of 
 the Laurentian spur accounts for the absence of the Potsdam in that 
 position. 
 
 The rock in Nepean is in most parts a fine grained pure white sandstone 
 fit for glass-making and well adapted for building. It here constitutes the 
 south side of a synclinal form, on the north side of which it rises in Hull 
 Dislocation, from beneath higher members of the Lower Silurian series. In Hull the 
 sandstone is observed about five miles north of the Ottawa and about two 
 miles east of the Gatineau, where it is brought into place by a dislocation 
 which branches in Osgood and Gloucester townships from the one pre- 
 viously mentioned, and, running somewhat west of north, crosses the Ottawa 
 at the Little Chaudiere Falls, and shews a downthrow on the east side. 
 The sandstone probably occurs on the west as well as the east side of the 
 dislocation, though it has not been observed there. 
 
 From this dislocation the rock runs eastward in a narrow band on the 
 north side of the Ottawa, across the townships of Templeton and Buck- 
 ingham, a distance of about twenty miles ; and a small anticlinal fold then 
 carries it to the south side of the river, where it tips a salient point in 
 Clarence on the axis of the anticlinal. Again passing to the north side in 
 Lochaber, near the mouth of the Blanche, it proceeds to within a short 
 distance of the North Petite Nation River. Hills of gneiss prevail on the 
 right bank of this stream, at the mouth ; and it would appear that an anti- 
 clinal fold or a dislocation runs from the corner of Lochaber to the valley of 
 the South Petite Nation River, carrying the Calciferous to the south side 
 and the Potsdam to the bottom of the Ottawa. An exposure of the Potsdam 
 Jiowever occurs on a peninsula on the north side, about seven miles below 
 the mouth of the Petite Nation, where the beds consist of fine grained 
 sandstone, the surface of one of which displays Protichnites. A little 
 below this, the river trenches to a small extent upon the Laurentian series, 
 the gneiss of which composes the most salient point of the township of 
 Alfred, on the south side ; and the only additional exposure of the Potsdam 
 known on the river is met with on the twentieth lot of the second range 
 of Grenville. 
 
 Lachute. A little beyond this the Calciferous formation, overlapping the Potsdam, 
 
 comes upon the Laurentian limestone ; but the Potsdam emerging again 
 farther on, is displayed at the Riviere du Nord, in an escarpment of 
 between thirty and forty feet of fine grained white sandstone at Lachute, 
 dipping to the southward at an angle of four degrees. The actual contact 
 
CHAP. VI.] 
 
 POTSDAM GROUP. 
 
 95 
 
 with the Laurentian series is concealed in a flat sandy valley, varying in 
 breadth from a quarter to half a mile ; but a bed with Protichnites, which 
 is at the summit of the escarpment, is computed to be about 250 feet over 
 the Laurentian rock, while it is followed by about seventy feet in which 
 sandstone marked by Scolithus gradually becomes interstratified with 
 calcareo-magnesian beds, constituting a passage to the formation above. 
 
 From this the outcrop turns to E. N. E., and follows the valley of the 
 Riviere du Nord for about twenty miles to the vicinity of St. Jerome, 
 approaching at Ste. Scholastique (which is about halfway) to within about 
 four miles of the sandstones which lean upon Mont Calvaire, at the extremity 
 of the anticlinal spur projected from Beauharnois ; the interval being filled 
 up by the Calciferous formation. From St. Jerfone, the course of the Pots- 
 dam becomes nearly N.E. ; and in this bearing it runs with considerable 
 regularity for about fifty miles, with a varying breadth of from two to four 
 miles, yielding in many places good material for building and for flagging. 
 Toward the eastern end of the distance the thickness of the rock appears 
 to diminish ; as about a mile N. W. of Cuthbert's mills on the Chicot chicot. 
 there is an exposure of fine grained white sandstone, characterized by 
 ProtichmteSy which is supposed to be near the summit of the formation, and 
 it is yet not far removed in this spot from the Laurentian gneiss. 
 
 In this vicinity, the Potsdam is suddenly brought against the Trenton 
 formation by a downthrow fault, of which the bearing is about N. 30 E. ; 
 and the sandstone is supposed to remain beneath newer members of the 
 Lower Silurian series, along the line of dislocation, for upwards of twenty 
 miles between the Chicot and Riviere du Loup en haut. Leaving this st. Maurice, 
 fault it reaches the St. Maurice Eiver at the Gres, where it yields a 
 material of freer grain than ordinary ; which has been found at the St. 
 Maurice and Radnor forges to answer admirably for furnace-hearths in the. 
 smelting of iron. On the St. Maurice, the gneiss occupies the left margin 
 from the Gres to a spot three quarters of a mile below the river Cachee ; 
 but for a part of the distance, near the mouth of the Cache'e and above it, 
 it is concealed by clay. The gneiss also occupies the right side to the 
 height of about twenty-five feet in the bank opposite the mouth of the 
 Cache'e, but to less than this farther up. Upon it reposes the Potsdam 
 sandstone, which, in an escarpment at the bend of the river in sight of the 
 fall, composes twenty feet of the cliff, while clay conceals what may be in 
 addition to this thickness at the top. The base, which is seen in contact 
 with the gneiss nearly on a level with the stream, is a four-feet bed of 
 conglomerate, composed of white vitreous quartz pebbles, some of them as 
 large as swan's eggs, and a few larger, in a matrix of fine white sand. 
 This fine white sand constitutes the beds above, and it is from them that 
 the furnace-hearths are obtained. On the right bank of the stream, a 
 little below the Cache'e, a quarry has been opened in a limestone rock of 
 
96 GEOLOGY OF CANADA. [CHAP. VI. 
 
 \ 
 
 an arenaceous character ; and it is probable that between this and the 
 twenty-five feet of gneiss which come to the water's edge, the Potsdam 
 beds may exist, though covered up by debris and vegetation. The total 
 thickness to be given to them would thus not much exceed fifty feet, the 
 dip being S. S. E., with not over one degree of inclination. 
 
 Between the St. Maurice and the Batiscan Rivers the rocks immediately 
 lying on the gneiss are covered over with drift, and their precise relations 
 are not known. Beyond this the contour of the Laurentian series, from 
 Ste. Anne de la Pdrade to Cape Tourmente, is much more irregular 
 and indented than higher up the valley of the St. Lawrence ; and six posi- 
 tions occur where it is projected forward from the general trend, namely 
 at Deschambault, Cap Sante', Pointe aux Trembles, Montmorenci, Sault 
 a la Puce or Chateau Richer, and the Riviere a la Rose. These six 
 Anticiinais. positions mark the axes of six folds or anticlinal forms ; and the zones 
 of rock which succeed, afiected by these folds, exhibit in their turn 
 a rudely corresponding set of projections. Some of the lower zones, how- 
 ever, are partially wanting ; and among them is the Potsdam formation, 
 which appears to be absent the whole distance, with the exception of one 
 st. Ambroise. place at St. Ambroise, where a few beds of the Potsdam sandstone occur, 
 in all about twenty feet thick. 
 
 Descending the St. Lawrence, no rock has been observed which could 
 be supposed to belong to the Potsdam formation before reaching Murray 
 Bay. A white translucent quartzite here occurs above White Point on 
 the west side of the bay, and at two spots on the east side ; one of them 
 within sight of the church just before reaching the Cape, which it is neces- 
 sary to double in proceeding along the beach to Les Ecorche's, and the 
 other close by Les Ecorche's. In these three localities the rock is ren- 
 dered cleavable, by the presence of silvery mica, into plates of from half an 
 inch to two or three inches thick, which appear to be conformable with the 
 stratification, and cracks in the quartzite occasionally present green stains 
 due to carbonate of copper. In these different localities, the rock succeeds 
 different descriptions of gneiss ; while a uniformity is preserved in the 
 character of the Silurian strata that succeed it, and it might be taken for 
 a mass belonging to this series. It appears doubtful however whether the 
 difierent exposures may not present distinct beds of quartzite belonging to 
 the subjacent gneiss. The thickness of the deposit at Les Ecorche's is 
 about forty-five feet.* 
 
 Lower Silurian strata are know to exist on one of the islands at the 
 entrance of the Bay of Seven Islands ; and there being a considerable area 
 of flat country between the coast and the Laurentian rocks, it is possible 
 
 * It has been ascertained, by Dr. Dawson of McGill College, Montreal, that these 
 quartzites really belong to the Laurentian series. 
 
CHAP. VI.] POTSDAM GROUP. 97 
 
 there may be an outcrop of the Potsdam formation resting upon them. No 
 examination, however, has yet been made to ascertain the fact. Between 
 the Calciferous formation of the Mingan Islands and the Laurentian gneiss 
 on the main shore there is room for the Potsdam ; and loose fragments of 
 both white and red sandstone with the characters of this formation, having 
 been met with on the coast, it appears probable that it is present, but it 
 has not yet been seen in place. 
 
 Bed and white sandstones. are known to occupy various localities on the Beiieisie. 
 north side of the straits of Belle Isle, such as Perroquet Island and Ance 
 aux Blancs Sablons, and there is little doubt that they belong to the Potsdam 
 formation. Such specimens of the rock as have been obtained are rather 
 coarse grained ; and some of these shew the existence of conglomerate beds, 
 in which the pebbles are half an inch in diameter, enclosed in a matrix of 
 red and white sand, the colors being arranged in parallel layers, and some- 
 times exhibiting false bedding. It would however be in vain to attempt 
 a description of the rock in this region until a larger number of facts have 
 been ascertained. 
 
 The Potsdam sandstone is thus traceable on its north-western outcrop Extent of the 
 from the straits of Belle Isle to Bedford, a distance exceeding 1000 miles. formatlon - 
 But there appears to be some doubt whether the deposit extends much 
 farther westward in Canada. Between Pakenham and Brockville the 
 outcrop of the sandstone rests on the east side of the low gneissic ridge 
 which connects the Laurentian rocks of the Adirondack area with the main 
 range in Canada, and causes a break between this outcrop and the next 
 exposure of the sandstone to the westward, which is upon the opposite 
 side of the low ridge ; the distance between the two outcrops in Canada 
 being about thirteen miles. 
 
 The formation is not largely developed on the west side of the ridge, 
 the greatest thickness of it observed at any one place being certainly not 
 over forty or fifty feet, while west of Knowlton Lake, in Loughborough, it 
 appears gradually to decrease in thickness, and eventually to die out alto- 
 gether. The largest spread of it in this part is in Storrington (formerly storrington 
 Pittsburgh) township, where it comes from under a limestone escarpment, 
 and terminates in an irregular outcrop running from Brass's Point on Lough- 
 borough Lake, in the ninth lot of the tenth range of Storrington, to the twelfth 
 lot of the eighth range on Vanluvin's Creek, a short way below Daly's 
 mills. The rock is for the most part of red and greenish colors, gener- 
 ally fine grained, having pebbles of opaque white quartz distributed scantily 
 and irregularly through it. In some parts it is of a pale greenish color, 
 with reddish or yellowish layers, and in others it is a nearly pure white 
 fine grained silicious sandstone. Some portions also are a brick-red and 
 very ferruginous, and others a coarse quartz conglomerate. 
 
 G 
 
96 GEOLOGY OF CANADA. [CHAP. VI. 
 
 an arenaceous character ; and it is probable that between this and the 
 twenty-five feet of gneiss which come to the water's edge, the Potsdam 
 beds may exist, though covered up by debris and vegetation. The total 
 thickness to be given to them would thus not much exceed fifty feet, the 
 dip being S. S. E., with not over one degree of inclination. 
 
 Between the St. Maurice and the Batiscan Rivers the rocks immediately 
 lying on the gneiss are covered over with drift, and their precise relations 
 -are not known. Beyond this the contour of the Laurentian series, from 
 Ste. Anne de la Parade to Cape Tourmente, is much more irregular 
 and indented than higher up the valley of the St. Lawrence ; and six posi- 
 tions occur where it is projected forward from the general trend, namely 
 at Deschambault, Cap Sante', Pointe aux Trembles, Montmorenci, Sault 
 a la Puce or Chateau Richer, and the Rividre a la Rose. These six 
 Anticiinais. positions mark the axes of six folds or anticlinal forms ; and the zones 
 of rock which succeed, affected by these folds, exhibit in their turn 
 a rudely corresponding set of projections. Some of the lower zones, how- 
 ever, are partially wanting ; and among them is the Potsdam formation, 
 which appears to be absent the whole distance, with the exception of one 
 St. Ambroise. place at St. Ambroise, where a few beds of the Potsdam sandstone occur, 
 in all about twenty feet thick. 
 
 Descending the St. Lawrence, no rock has been observed which could 
 be supposed to belong to the Potsdam formation before reaching Murray 
 Bay. A white translucent quartzite here occurs above White Point on 
 the west side of the bay, and at two spots on the east side ; one of them 
 within sight of the church just before reaching the Cape, which it is neces- 
 sary to double in proceeding along the beach to Les Ecorche's, and the 
 other close by Les Ecorche's. In these three localities the rock is ren- 
 dered cleavable, by the presence of silvery mica, into plates of from half an 
 inch to two or three inches thick, which appear to be conformable with the 
 stratification, and cracks in the quartzite occasionally present green stains 
 due to carbonate of copper. In these different localities, the rock succeeds 
 different descriptions of gneiss ; while a uniformity is preserved in the 
 character of the Silurian strata that succeed it, and it might be taken for 
 a mass belonging to this series. It appears doubtful however whether the 
 different exposures may not present distinct beds of quartzite belonging to 
 the subjacent gneiss. The thickness of the deposit at Les Ecorche's is 
 about forty-five feet.* 
 
 Lower Silurian strata are known to exist on one of the islands at the 
 entrance of the Bay of Seven Islands ; and there being a considerable area 
 of flat country between the coast and the Laurentian rocks, it is possible 
 
 * It has been ascertained, by Dr. Dawson of McGill College, Montreal, that these 
 quartzites really belong to the Laurentian series. 
 
CHAP. VI.] POTSDAM GROUP. 97 
 
 there may be an outcrop of the Potsdam formation resting upon them. No 
 examination, however, has yet been made to ascertain the fact. Between 
 the Calciferous formation of the Mingan Islands and the Laurentian gneiss 
 on the main shore there is room for the Potsdam ; and loose fragments of 
 both white and red sandstone with the characters of this formation, having 
 been met with on the coast, it appears probable that it is present, but it 
 has not yet been seen in place. 
 
 Eed and white sandstones, are known to occupy various localities on the Beiieisie. 
 north side of the straits of Belle Isle, such as Perroquet Island and Ance 
 aux Blancs Sablons, and there is little doubt that they belong to the Potsdam 
 formation. Such specimens of the rock as have been obtained are rather 
 coarse grained ; and some of these shew the existence of conglomerate beds, 
 in which the pebbles are half an inch in diameter, enclosed in a matrix of 
 red and white sand, the colors being arranged in parallel layers, and some- 
 times exhibiting false bedding. It would however be in vain to attempt 
 a description of the rock in this region until a larger number of facts have 
 been ascertained. 
 
 The Potsdam sandstone is thus traceable on its north-western outcrop Extent of the 
 from the straits of Belle Isle to Bedford, a distance exceeding 1000 miles. fonnation - 
 But there appears to be some doubt whether the deposit extends much 
 farther westward in Canada. Between Pakenham and Brockville the 
 outcrop of the sandstone rests on the east side of the low gneissic ridge 
 which connects the Laurentian rocks of the Adirondack area with the main 
 range in Canada, and causes a break between this outcrop and the next 
 exposure of the sandstone to the westward, which is upon the opposite 
 side of the low ridge ; the distance between the two outcrops in Canada 
 being about thirteen miles. 
 
 The formation is not largely developed on the west side of the ridge, 
 the greatest thickness of it observed at any one place being certainly not 
 over forty or fifty feet, while west of Knowlton Lake, in Loughborough, it 
 appears gradually to decrease in thickness, and eventually to die out alto- 
 gether. The largest spread of it in this part is in Storrington (formerly Storrington 
 Pittsburgh) township, where it comes from under a limestone escarpment, 
 and terminates in an irregular outcrop running from Brass's Point on Lough- 
 borough Lake, in the ninth lot of the tenth range of Storrington, to the twelfth 
 lot of the eighth range on Vanluvin's Creek, a short way below Daly's 
 mills. The rock is for the most part of red and greenish colors, gener- 
 ally fine grained, having pebbles of opaque white quartz distributed scantily 
 and irregularly through it. In some parts it is of a pale greenish color, 
 with reddish or yellowish layers, and in others it is a nearly pure white 
 fine grained silicious sandstone. Some portions also are a brick-red and 
 very ferruginous, and others a coarse quartz conglomerate. 
 
98 GEOLOGY OF CANADA. [CHAP. VI. 
 
 Near the road leading in a general easterly direction from Vanluvin's 
 mills to Dog Lake landing, in the twelfth lot of the ninth range of Storring- 
 ton, a cliff of sandstone exhibits the following section in ascending order : 
 
 Ft. in. 
 Grey moderately fine grained sandstone in a solid bed, holding angular pebbles 
 
 of white quartz, the largest of which is from six to seven iriches in length,. . 4 
 Dark grey rather coarse grained sandstone, with frequent very red stains, and 
 
 weathering of a rusty-red color, 2 
 
 Yellowish fine grained sandstone, 6 
 
 Dark grey rather coarse grained sandstone, mottled and striped with red and 
 
 yellow, holding pebbles of opaque white and bluish-grey quartz, usually 
 
 angular, sparingly disseminated through the bed, 2 
 
 Dark grey yellow weathering very hard silicious sandstone, striped yellow and 
 
 reddish, 6 
 
 Dark grey yellow-weathering sandstone as before, with spots of brick- red, 1 9 
 
 10 9 
 
 At intervals, the road for about eight chains east from this section 
 exposes flat surfaces of grey sandstone, sometimes rather obscurely ripple- 
 marked, and studded with quartz pebbles. Four chains to the south an- 
 other cliff arises, shewing strata supposed from their position to be higher 
 beds, which in ascending order are as follows : 
 
 Ft. in. 
 
 Grey and red coarse grained sandstone in alternate beds, 8 9 
 
 Red and white coarse grained sandstone, with small pebbles of white quartz dis- 
 tributed over the divisional planes of the bedding, 4 
 
 A confused mass of conglomerate, composed of large pebbles of quartz loosely 
 
 and irregularly imbedded in a sandy matrix, -. . . 8 
 
 Red and grey coarse grained sandstone in a set of thin beds, with small quartz 
 
 pebbles scattered over the divisional planes, 3 
 
 23 9 
 
 At the place where the conglomerate occurs, the dip, as Indicated in the 
 overlying beds, is S. 50 E. < 10, but that dip is only local. On the north 
 side of the road the rocks are very nearly flat, and no conglomerate re- 
 sembling the eight-feet bed in the above section is observed at all. At 
 Daly's mills, on the eleventh lot of the eighth range, there is an exposure 
 of about thirty feet of sandstone, the upper beds of which dip about 
 N. 16 W. < 10 12 ; and in the same stream, a little higher up, on 
 the twelfth lot of the tenth range, similar beds dip S. 66 E. < 15 ; but 
 the strata between are nearly flat, and these comparatively high angles of 
 inclination appear only near their junction with the inferior Laurentian 
 series, resting on which the unconformable Silurian beds seem almost 
 always to be slightly accommodated to the worn surface. 
 
CHAP. VI.] POTSDAM GROUP. 99 
 
 Between the area of Potsdam sandstone to which these sections belong, 
 and another north of it, there appears a position, just west of Vanluvin's 
 mills, where the formation is overlapped by the succeeding rock. The 
 northern area occupies both sides of the stream above the mills, and 
 extends to Loughborough Lake. 
 
 At Brass's Point, which belongs to this area, the sandstone is very 
 white and fine grained, and it is frequently penetrated by slender cylindrical 
 holes, for the greater part vertical. These are tinged of a dirty brown or. 
 rusty color, and contrast strongly with the white stone. They are supposed 
 to be Scolithus Canadensis. Below the white sandstone there is a fine silicious 
 conglomerate, and that is underlaid by grey sandstone, which is occasion- 
 ally seen resting on the gneiss, the whole thickness displayed not exceeding 
 six feet. At another point, on the south side of Loughborough Lake, in 
 the seventh lot of the ninth range of Storrington, a cliff exposes about 
 twenty feet of the sandstone sloping gently south-west towards the foot of 
 a calcareous escarpment, which rises abruptly on the south side of the 
 bay west from this point. At Knapp's Point opposite, and on a small island 
 near, there are similar strata. 
 
 To the west of Knapp's Point it is very probable that the formation is 
 again overlapped by the succeeding rock, as no exposure of the Potsdam 
 is seen for seven miles, though the superior rock can be traced without 
 much difficulty the whole way ; and on the north side of the lake, on the 
 thirteenth lot of the third range of Loughborough, it is seen to approach 
 close to the gneiss. 
 
 In the township of Loughborough the formation occurs occasionally in outliers in 
 outlying patches, resting upon gneiss or crystalline limestone. One O f Loughborough 
 these outliers is on the eleventh lot of the ninth range, at the northern end 
 of Eel Lake, where a cliff of about forty or fifty feet high is capped by red 
 or purplish and white silicious sandstone, arranged in layers of from six 
 inches to one foot thick, the whole thickness being about sixteen feet. 
 The lower part of the cliff is concealed by debris from the sandstone beds ; 
 but the outlier, which does not appear to exceed a few acres in extent, is 
 surrounded by gneiss. Other small outliers occur near the base of the 
 fossiliferous escarpment, on the fourth and fifth lots hi the rear of the 
 seventh or the front of the eighth range of Loughborough, some of which 
 occupy an area of about an acre, and rest immediately on the crystalline 
 limestone. 
 
 On the west side of Knowlton Lake, sandstone strata come from beneath 
 an escarpment of fossiliferous limestone, and rest upon crystalline lime- 
 stone. At the south end of the lake there is an exposed thickness of four- 
 teen feet of red and grey or greenish massive sandstone, in beds of from 
 three to four feet, over which the ground is level for about fifty yards, and 
 then rises rather abruptly on it the talus of the escarpment of the superior 
 
100 GEOLOGY OF CANADA. [CHAP. VI. 
 
 fossiliferous formation. One portion of the red bands here is very ferru- 
 ginous, almost passing into hematitic iron-ore. The unctuous powder re- 
 sulting from it imparts its color to the soil around, and the surface of the 
 hematitic bed is marked by concretionary ferrugino-arenaceous masses, 
 from one to three inches in diameter, giving it a mammillated character. 
 
 Lak Wlt n "^ ^ e north or lower end of Knowlton Lake, on a bold square-shaped 
 bluff, which comes out between the outlet and a long bay on the east side, 
 there is a considerable display of sandstone. The cliff rises at some points 
 to the height of sixty feet. The upper part is red or red and green, in 
 rather thin beds, some under three inches in thickness, and the upper sur- 
 face is mammillated as before. The lower beds are mostly massive, being 
 from nine to eighteen inches thick, and their colors are red, green, and 
 drab, in some parts alternating in very thin stripes. The lower part of 
 these beds appears to rest on a rather fine silicious conglomerate ; but the 
 latter being seen only just at the edge of the water, its relation has not 
 been satisfactorily ascertained, although the impression is that it belongs 
 to the Laurentian series below. The same measures come out at a little 
 distance north of the lake, on the second lot of the tenth range, and are 
 again seen on a small brook on the road between the ninth and tenth 
 ranges near the town line between Loughborough and Portland ; immediately 
 west of which the superior fossiliferous limestone rises in an escarpment, 
 without any intervening sandstone. Beyond, this no indication of the 
 Potsdam formation has been observed in Canada, unless eight feet of red 
 soft calcareous sandstone at Marmora, resting on the gneiss and succeeded 
 by certain beds of limestone without observed fossils for thirty feet upwards, 
 be supposed to represent it, or unless, as before suggested, a portion of 
 the upper copper-bearing series of Lake Superior be considered of the 
 Potsdam age. 
 
 organic The evidences of organic life in the Potsdam sandstone are but few. In 
 
 ms ', Canada fucoids exist in it in abundance, some of which have been 
 figured by Mr. Hall in the Palaeontology of New York. With these 
 there are associated Scolithus Canadensis, Lingula acuminata, Ophileta 
 compacta, a large Pleurotomaria allied to P. Laurentina, and fragments 
 of two species of Orthoceras, all in the upper part of the formation. In 
 addition to these, there occur three different descriptions of tracks, two 
 of which are supposed to have been impressed by molluscous animals, 
 and the third by some crustacean. The more remarkable of the former 
 has been named Olimactichnites, and the latter Protichnites. 
 
 Fucoids. The fucoids abound most in the upper part of the formation, and one 
 prevailing form of these marine plants presents a reticulating arrange- 
 ment of stems spreading over the surfaces of the beds, the meshes of 
 the net-work being four, five, or six-sided, and sometimes, when largest, 
 measuring fourteen inches in diameter ; while the rope-like stems which 
 
CHAP. VI.] POTSDAM GROUP. 1Q1 
 
 divide them are an inch wide, standing out half an inch in relief on the 
 sandstone. The mesh-like compartments are sometimes filled with a 
 green shale, and the forms much resemble crack-casts, and might be taken 
 for such, were not similar forms sometimes traceable on splitting open 
 closely fitting surfaces of sandstone when no shale is present between, and 
 were not smooth surfaces of an arenaceo-bituminous limestone in the suc- 
 ceeding formation met with, presenting thin black bituminous pellicles 
 arranged in similar reticulating figures, both large and small. It is not 
 improbable, however, that in some cases these forms may really be casts 
 of cracks. 
 
 7. SUPPOSED ANNELIDE BURROWS. NATURAL SIZE. 
 
 Scolithus Canadensis (Billings). 
 
 The upper part of the formation is abundantly marked over considerable Scolithus. 
 surfaces by Scolithus Canadensis, which, when the rock is weathered, is seen 
 on the surface of the beds in the form of small nearly circular holes, from 
 one twentieth to one fourth of an inch in diameter. These sometimes 
 penetrate vertically to the depth of several inches ; but in general, on 
 breaking up the rock, they are found to be more or less curved in different 
 directions, and often irregularly contorted and intermingled with each other. 
 They are not unfrequently somewhat prismatic, the transverse section 
 exhibiting three, four, or five sides. The casts of the interior of these 
 cavities in freshly broken or unweathered masses of the rock usually 
 appear as solid cylindrical or angular rods, composed apparently of grains 
 of sand cemented by a slightly calcareous matter, more or less tinged with 
 peroxyd of iron. The origin of these holes is not quite certain : some 
 suppose them to be the remains of fucoids, others of corals, while many 
 are of opinion that they were the habitations of small burrowing marine or 
 shore-frequenting animals. Whatever may have been their origin, they 
 
102 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. VI. 
 
 Lingula; Or- 
 thoceras . 
 
 characterize the upper part of the formation extensively. The original 
 specimens, upon which the genus was established, differ from those above 
 described in being straight and more decidedly cylindrical, and are there- 
 fore probably a distinct species, but at present very little is known 
 concerning the affinities of these fossils. 
 
 In Lansdowne and Bastard, in what we consider to be the beds of pas- 
 sage between the Potsdam and the succeeding formation, Scolithus and 
 fucoids exist in abundance, and are there found associated with Lingula 
 acuminata. At Beverley in the township of Bastard and in the township 
 of South Crosby small orthoceratites and Ophileta compacta occur, though 
 
 8. BBACHIOPODA. 
 
 Lingula acuminata (Conrad). Specimens showing the variations in form 
 and size ; a, b, c and e are ventral valves ; d is a dorsal valve ; /, g, 
 are young shells. 
 
 rarely, in beds which hold this same species of Lingula in vast profusion. 
 At Beauharnois, on the south side of Lake St. Louis, about twenty miles 
 above Montreal, Ophileta compacta occurs near the beds with JProtichnites. 
 
 9-11. GASTEROPODA ATO> CEPHALOPODA. 
 
 9. Ophileta compacta (Salter). a, view of the lower ? or flat side. 
 
 of the upper or concave side. 
 10. Fragment of an Orthoceras from Beverley. 
 11. Fragment of an Orthoceras from South Crosby. 
 
 b, cast 
 
 This name has been given to the foot-prints of an animal which Professor 
 Owen has pronounced to be some species of crustacean. 
 
 The first track discovered was met with near the mill on the St. Louis River 
 at Beauharnois ; and the late Mr. Abraham, editor of the Montreal Gazette, 
 was the first to draw attention to it, by a notice in his journal, in which he 
 compared it to the track of a tortoise. A plaster cast of the track having 
 been inspected by Professor Owen, the first examination by this 
 
CHAP. VI.] POTSDAM GROUP. 1Q3 
 
 celebrated comparative anatomist rather tended to confirm this opinion. 
 But the original stone having been subsequently submitted to him, as well 
 as two additional original surfaces and casts of a great number of other 
 impressions of the same order, several of these giving much clearer evidence 
 than the first specimen, Professor Owen was led to conclude that the foot- 
 steps could not have been imprinted by any quadruped, and that analogies 
 were most in favor of their having been produced by some species of 
 crustacean, but of a family wholly distinct from anything presented by the 
 crustacean forms of later geological periods or of the present day. 
 
 The track, when the specimens are most perfect, generally presents 
 a median groove more or less flat and of different proportionate widths 
 in different specimens, with a number of footprints on each side in 
 corresponding pairs. Certain sets or numbers of these pairs have 
 homologous repetitions throughout the whole length of the track, as if 
 they were the result of successive applications of the same impressing 
 instruments, and the numbers of corresponding pairs in the homologues of 
 different tracks are sometimes different, constituting something which may be 
 considered analogous to difference of species. The homologues in different 
 tracks appear to have sometimes seven and sometimes eight answering pairs 
 of pits, and it is difficult to say whether the pits are to be taken as impres- 
 sed by the extremities of so many legs, thus giving the animal fourteen 
 legs in one case and sixteen in the other, or whether some of the impressing 
 points are to be grouped in twos or threes, making some of the legs bifid 
 or trifid, and thus diminishing their number, as Professor Owen is inclined 
 to suppose. The impressions are generally of such a nature as to negative 
 the supposition that the impressing instruments were of a soft or padded 
 nature, and the depth and trenchant sharpness of the markings in the 
 bottom of some would seem to show the effect of hard horny points. 
 
 The groove in most of the tracks is so uniformly in the middle 
 between the footprints as to have favored the supposition that it might 
 have been produced by an immovable breast-plate or plastron; but in 
 one remarkable instance, at a bend in a track, the groove gradually 
 leaves the middle, and, while it seems impressed with more force than usual, 
 approaches and partly obliterates the footprints on the convex side, as if 
 the pressing part had been a tail, which when the body turned to one side, 
 interfered with the footprints in the rear on the other. A feature common 
 to all the grooves is that each repetition of the series of footprints is 
 accompanied with a deepening and shallowing of the groove, giving it the 
 appearance of a chain of shallow troughs, which, when the impression is 
 light, are separated from one another by intervals of an ungrooved surface. 
 The groove is often but faintly indicated, and occasionally is not percep- 
 tible. It frequently happens, when this occurs, that the footprints are 
 stronger and deeper than when the groove is more conspicuously impressed. 
 
104 
 
 GEOLOGY OF CANADA. 
 
 12-17. TKACK8 FROM BEAUHABNOI8. SCALE 
 
 [CHAP. VI. 
 
 I -.- 
 
 12. Protichnites lineatus (Owen). 15. Protichnites septemnotatus (Owen). 
 13. P. alternans (Owen). 16. P. octonotatus (Owen). 
 
 14. P. multinotatus (Owen). IT. P. octonotatus (Owen). 
 
CHAP. VI.] POTSDAM GROUP, 105 
 
 In some of the tracks, while the groove is straight, the exterior limits of 
 the footprints offer a congeries of segments of a circle convex on the out- 
 side ; but those on opposite sides of the groove alternate, the segment on the 
 one side starting from the middle of a segment on the other, and giving to 
 the whole series of footprints in the track a serpentining course, as if the 
 animal had waddled in its gait. In one of the tracks there are three nar- 
 row grooves instead of footprints on each side of the main one, as if the 
 limbs of the animal had been dragged along while the body was afloat. 
 
 In conformity with these various differences in the tracks, Professor Prof. Owen's 
 Owen has given separate provisional names to several of them, not for the n ' 
 purpose of indicating a positive specific difference in the animals which 
 impressed them, but for the convenience of reference. The generic term 
 is ProtichniteSj and the specific names are P. septemnotatus, P. octonota- 
 tus, P. multinotatus, P. alternans, and P. Uneatus. 
 
 The surfaces on which the tracks of these animals ' are impressed are 
 sometimes smooth, and sometimes beautifully ripple-marked. On the 
 latter the tracks have often beaten down the ripple-marks, and the sand of 
 the ridge has been dragged into the furrow, in such a -way as to show the 
 direction in which the animal was progressing. In all the tracks, with the 
 exception of P. Uneatus, there is a diverging arrangement of the succes- 
 sive answering pairs of footprints in each homologous set of impressions, 
 and the relation of this divergence to the direction of progress in the tracks 
 on the ripple-marked surfaces, gives the means of establishing the direc- 
 tion of movement in every other case. 
 
 The most abundant locality of these tracks is on the field of Mr. Renault, 
 about half a mile westward from that near the mill. There are four exposed 
 areas in the space of four chains. Before any specimens were removed, the 
 first area shewed ten tracks running in different directions, and sometimes 
 crossing one another ; they varied in width from four inches and a quarter 
 to five inches and a half, and their total length was 108 feet. The second 
 displayed eleven tracks, from five to six inches wide, measuring about 108 , 
 
 feet. The third shewed five tracks of from four to six inches wide, and 
 were altogether sixty-one feet long ; the fourth, five tracks from three 
 quarters of an inch to five and a half inches wide, and giving an aggregate 
 ength of eighteen feet. Another area in the next field had ten tracks of 
 from four to six and a half inches wide, with a total length of fifty-six feet. 
 
 The following is a section of the beds as they succeed one another in section at 
 descending order in the vicinity, the whole of them being fine grained : 
 
 Ft. in. 
 White sandstone, hard and compactly granular, with indications of closely 
 
 soldered elementary layers,. 6 
 
 White sandstone, with small ferruginous spots and indistinct traces of Scolithus 
 
 Canadensis at the top ; the joints in the top are stained with peroxyd of iron, 2 
 
106 GEOLOGY OP CANADA. [CHAP. VI. 
 
 Ft. in. 
 White sandstone, even-bedded and splitting into rectangular blocks, fit for 
 
 building purposes, 1 6 
 
 White sandstone with very regular cleavage and bedding, fit for building and 
 
 glass-making ; there are ripple-marks and reticulating fucoids on the top, 1 3 
 
 White sandstone with a smooth surface, 7 inches. 
 
 White sandstone with ripple-mark and tracks, 0-5 " 
 
 White sandstone with ripple-mark, 0-1 " 
 
 White sandstone with wind-mark, 0-1 " 
 
 White sandstone with a smooth surface and tracks, 0-2 " 
 
 l-f ff 
 
 White sandstone ; this bed is made up of beautifully regular parallel layers 
 of from two to four inches, closely fitting together, but distinctly marked 
 by very slight differences of color ; the joints are remarkably regular, and 
 the bed would yield excellent material for glass-making and building, and 
 
 perhaps for flagging, 3 
 
 White sandstone with broad ripple-mark on the top, measuring from eight to 
 
 ten inches between the ridges, 4 
 
 Light grey limestone in patches, passing into sandstone, and displaying abun- 
 dance of Scolithus Canadensis, 4 
 
 White sandstone, 5 4 
 
 White sandstone slightly calcareous, with a thin more silicious bed at the 
 
 top, covered over with iron stains, and marked by Scolithus,. 4 11 
 
 White sandstone marked on top by Scolithus, 1 1 
 
 White sandstone slightly calcareous, with ripple-mark and Scolithus } 1 6 
 
 White sandstone less calcareous, with Scolithus, 6 
 
 White calcareous sandstone ; the calcareous matter is more abundant in por- 
 tions, and the rock wears unequally, 2 
 
 White sandstone slightly calcareous, with Scolithus prevailing in a few inches 
 
 at the top, 2 2 
 
 White sandstone slightly calcareous, with a Scolithus bed at the top, 2 1 
 
 White sandstone slightly calcareous, Scolithus at the top, 6 
 
 White sandstone with a Scolithus bed at the top, holding calcareous patches, . 2 6 
 White sandstone with calcareous indications, and a Scolithus bed at the top,. . 2 6 
 
 Measures concealed, 10 
 
 Greyish calcareous sandstone, with two bands of limestone pebbles towards 
 the middle ; the top and bottom surfaces of the bed are marked with large 
 reticulating forms ; some of the meshes are fourteen inches in diameter, 
 and the stems from one and a half to two inches wide : the forms of the 
 meshes are sometimes four, sometimes five, and sometimes six-sided ; the 
 part included within the mesh is filled with clay or rather a crumbling 
 dark green shale, giving a brownish streak ; when the shale is removed the 
 stem-like portions stand out in relief to the height of half an inch. Geodes 
 or nodules of reddish calc spar occur in the bed, sparingly disseminated, 2 
 
 55 3 
 
 Ripple and ^ e ripple-marks which occur on surfaces so close to one another in 
 wind marks, succession among the track-beds, run in different directions, as if they 
 had been caused, not by a current in deep water running in one general 
 direction, but by a tide ebbing and flowing, and obeying the influence 
 of varying local accidental causes. On one surface is observed the 
 natural edge or termination of the ripple-ridges, with a track coming 
 
CHAP. VI.] 
 
 POTSDAM GROUP. 
 
 107 
 
 up to it and then ceasing, as if the wave had reached no farther and one 
 part of the surface had been dry, while the water, operating on another 
 close by, had obliterated the track in producing the ripple-mark. The 
 subjacent surface is again marked by ripples, and the succeeding one by 
 wind, as is shown by a multitude of slender straight parallel ridges, so well 
 known to all who have observed the effect of a strong wind on loose sand 
 or snow. This surface had been previously marked by ripples, and the 
 erosion, by the wind, of the ripple-ridges appears to have more or less 
 reduced each of them to a series of small separate mounds, ranged in the 
 line of the ridge. Behind all these mounds there are stains of peroxyd of 
 iron ; and it appears probable that the peroxyd may have been derived 
 from ferruginous grains, from which the lighter sand had been winnowed 
 by the wind. We may thus have a comparative measure of the strength 
 of the wind, which was sufficient to propel silicious sand, but insufficient to 
 carry along grains of iron ore. 
 About a mile from Perth, in a quarry on the sixth lot of the third range 
 
 18. TRACK FROM PERTH. SCALE ^y. 
 
 nites of 
 Perth. 
 
 18. Climactichnites Wilsoni (Logan). 
 
 of Drummond, belonging to Mr. Glen, Dr. James Wilson of Perth has 
 discovered, in association with Protichnites, the trail of what is supposed to 
 
108 GEOLOGY OF CANADA. [CHAP. VI. 
 
 have been some species of mollusk. A description of the track, which has 
 received the name of Climactichnitea, has been given in The Canadian 
 Naturalist and Geologist, vol. V. p. 279. It consists of a series of par- 
 allel ridges, resembling ripple-marks, about an inch and three quarters 
 apart. These are arranged transversely between two narrow, continuous, 
 parallel, beaded sinuous ridges, about six inches apart, giving to the whole 
 impression a form very like a ladder of ropes. The transverse ridges are 
 occasionally straight, but in general more or less curved, and there runs 
 along the track a ridge intermediate between the two side ridges, which, 
 although not so conspicuous as these, is seldom altogether wanting, but 
 appears to be most obscure when the transverse ridges are straight. The 
 intermediate ridge does not keep constantly parallel with the side ridges, 
 but occasionally runs in sinuous sweeps from within an inch and a half of 
 one side to within the same distance from the other ; and the most salient 
 part of the transverse ridges, when these are curved, appears generally, 
 but not always, coincident with its position. 
 
 The Potsdam, That portion of the Potsdam group which has here been described 
 appears to have been deposited in shallow water along the margin of the 
 Lower Silurian sea, and the wind-mark on one of the surfaces connected 
 with the track-beds at Beauharnois proves incontestably that these beds 
 were uncovered at the ebb of tide. In the eight localities in which 
 these tracks have been met with, extending on the strike of the formation 
 for about 400 miles, the beds on which they are impressed are always of 
 the same lithological character, and seem to stand in the same relation to 
 the summit of the formation, where this can be ascertained. We have 
 thus good reason to believe that all these beds were at nearly the same 
 geographical level at the same time. Three of the localities occur along 
 the foot of the Laurentide hills, from which the beds stretch out at a very 
 low angle into the Silurian plain in front. The hills, at no very great 
 distance from the outcrop of the Potsdam formation, rise to heights 
 varying from 500 to nearly 4000 feet; and while the sand at their 
 base lay between the ebb and flood of tide, the flank of the Laurentide 
 mountains must have formed the coast of the Lower Silurian sea. As has 
 already been stated, these hills extend from Labrador to the Arctic Ocean, 
 and we can thus trace out this ancient limit of the ocean for 3500 miles. 
 
 The thoroughly rounded form of the grains of sand composing a large 
 portion of the deposit, and the fact that all the material other than quartz 
 has been bruised up and washed out from so much of it, would seem to 
 make it probable that the formation accumulated slowly, and that the 
 Potsdam coast remained unchanged for a great length of time. The fact, 
 however, that the formation is in some places overlapped by the succeeding 
 deposit, would seem to show that a subsidence had commenced toward the 
 end of the epoch ; and the passage, by interstratification, with the succeed- 
 
CHAP. VI.] POTSDAM GROUP. 109 
 
 ing rock, which is so distinct in many places, appears to indicate that the 
 subsidence was slow and gradual. Its duration, and the area affected by 
 it, must be proved by the accumulation and distribution of the succeeding 
 formations. If it be assumed that the track-beds were deposited at about 
 the mean level of the sea, we have a bench-mark by which to know how 
 nearly they have been restored to their original position after their subsi- 
 dence and re-elevation, and what inequalities of level were produced over 
 the area including them, during the period of their movements. The pres- 
 ent heights over the summer level of Lake St. Peter,* of the various track- 
 bed localities which have been mentioned, are approximately as follows : 
 
 Beauharnois, east side of anticlinal, 80 feet. 
 
 Beauharnois, west side of anticlinal, 80 " 
 
 Vaudreuil, 83 " 
 
 Ste. Genevieve Island, near Ste. Anne, 75 " 
 
 Chicot, .' 160 " 
 
 Lachute, 145 . 
 
 Petite Nation, 130 " 
 
 Perth, 430 " 
 
 * Lake St. Peter is the highest part of been ascertained how much the latter is 
 
 the St. Lawrence affected by the action of above the mean level of the sea. The heights 
 
 the tide. At the flood of spring tides its of the great lakes of the St. Lawrence, and 
 
 surface rises ab'out six inches, not how- of most of the points in the interior, given 
 
 ever from any back flow in the lake, but in the first chapter, are calculated from the 
 
 from a diminution in the rate of its current summer level of Lake St. Peter as a datum ; 
 
 through the accumulation of the water far- but they are spoken of as above the level 
 
 ther down. The summer level of the lake of the sea, because, while the difference is 
 
 is a small but uncertain number of feet not great, such a datum is more readily 
 
 above high water at Quebec, and it has not understood. 
 
GEOLOGY OF CANADA. [CHAP. VII. 
 
 CHAPTER VII. 
 
 THE CALCIFEROTJS FORMATION. 
 Tare CALCiFEiiotrs SANDROCK; A MAGNESIAN LIMESTONE; PART OF A GREAT GROUP. GEODES ; 
 
 CONCRETIONARY LAYERS. CLAYSTONE, DISTRIBUTION OF THE FORMATION? ITS ABSENCE 
 IN SOME FARTS OF CANADA, MlNtf AS ISLANDS. FOSSILS J GABTEROFODB J ORTHOCER- 
 ATITE6. TRILOBITE8. 
 
 The name of Calciferous sandrock was given by the New York geologists 
 to the formation which immediately succeeds the Potsdam sandstone. 
 Calcareous sandstone beds mark the passage between the two ; but the 
 characteristic portion of the formation, at least in Canada, is a granular 
 magnesian limestone or dolomite, which, from its rough weathered surfaces 
 and its slight effervescence with acids, may have suggested the name of the 
 Calciferous sandrock. We purpose in the present chapter to describe 
 the extension in Canada of the formation which is thus designated in New 
 York. In the valley of the Upper Mississippi, where this formation is 
 greatly developed, it is known as the Lower magnesian limestone. Inves- 
 tigations now in progress tend to show that this Calciferous sandrock forms 
 part of a great series of strata, which in Eastern Canada are known as the 
 Quebec group, and that it is there represented by the limestones at Point 
 Lid vis. As mentioned in a previous chapter, it is supposed that a portion 
 of the upper copper-bearing rocks of Lake Superior is of the same age. 
 
 The typical Calciferous sandrock, which succeeds to the Potsdam in New 
 York and the adjacent parts of Canada, consists in the lower part of a dark 
 bluish-grey, crystalline, strongly coherent dolomite or magnesian limestone, 
 weathering yellowish-brown, and very often holding small geodes, generally 
 filled with calcareous spar, but sometimes containing quartz crystals, sul- 
 phate of barytes, sulphate of strontian, and sulphate of lime or gypsum. 
 The fossils have in most cases disappeared, leaving only their moulds in the 
 rock. The upper part of the formation is in some places a bluish-grey 
 calcareous argillite, weathering yellow or brown, and often having a bitu- 
 minous odor. The total thickness of the formation is supposed to be about 
 300 feet. 
 
CHAP. YII.] CALCIFEROUS FORMATION. 
 
 A short distance above Maitland, in the township of Augusta, the fol- section at 
 lowing ascending section* was measured, shewing the beds of passage : Maitland - 
 
 Ft. in. 
 
 White quartzose sandstone, with thin interstratified calcareous bands, 5 
 
 Brownish-grey calcareotts sandstone, 2 
 
 Measures concealed, 10 
 
 White sandstone with soft brown-stained vertical streaks, probably Scolithus 
 
 Canadensis, 5 
 
 White sandstone, calcareous in the upper part, 4 
 
 Pale grey limestone, with great quantities of fucoids on the upper surfaces of 
 
 the beds, , 3 
 
 Measures concealed, 6 
 
 Pale grey or drab colored sandstone in thin beds, 3 
 
 Bluish-grey silicious limestone, 6 
 
 Measures concealed, 6 
 
 Dark grey calcareous sandstone, 2 6 
 
 Grey quartzose sandstone, weathering brown, 2 
 
 Dark bluish-grey limestone, 3 
 
 Dark brownish-grey cherty limestone, in irregular layers, 2 6 
 
 Dark bluish-grey limestone with geodes of calcspar ; there are exposed on the 
 
 surfaces fucoids and many convoluted shells, 5 
 
 59 6 
 
 Gentle undulations in the strata occur descending the river from this, section ne 
 carrying the same measures to the vicinity of Battle Windmill, a little Prescott - 
 below Prescott. The dip of the measures is here nearly east, at an angle 
 of two or three degrees, and the following section is met with in continua- 
 tion of the previous one : 
 
 Ft. in. 
 
 Grey limestone, 3 6 
 
 Dark bluish-grey limestone, with occasional large concretionary balls, 2 
 
 Brownish-grey rather coarse textured limestone, with obscure convoluted shells, 4 6 
 Dark bluish-grey limestone, of a crystalline texture, sometimes tinged with red, 
 
 and separated into beds by thin layers of a very dark blue shale, 1 2 
 
 Dark bluish-grey limestone, with geodes of calcspar, 6 
 
 Brownish calcareo-arenaceous shale, 3 
 
 Dark bluish-grey limestone, 8 
 
 Pale grey compact limestone, with geodes of calcspar ; a thin division of green- 
 ish-brown shale lies between it and the previous bed, 10 
 
 Pale grey compact yellow-weathering limestone, rapidly disintegrating on the 
 
 surface, 8 
 
 Drab colored calcareous sandstone, probably magnesian, with a large quantity of 
 
 calcspar in geodes, 1 5 
 
 * The beds described as limestones in the were examined they were supposed to be, 
 
 sections here given, are in most, if not in as previously described by Prof. Emmons 
 
 all cases, dolomite ; and it is not improb- in New York, mixtures of silicious sand 
 
 able that some of those designated as cal- with limestone. Many of the dolomites of 
 
 careous sandstones may be of a similar this series, however, have a large admix- 
 
 nature, although at the time the sections ture of sand. 
 
GEOLOGY OF CANADA. 
 
 [CHAP. VII. 
 
 Ft, in. 
 
 Claystone. 
 
 Grey limestone, with many geodes of calcspar, and cracks lined with the same 
 mineral, ................. . ......................................... 
 
 Grey limestone, ........................................................ 
 
 Pale grey limestone, weathering of a decided yellow, and rapidly disintegrating 
 on exposed surfaces ; the bed is filled with concretionary masses, the concen- 
 tric layers of which are frequently interleaved with white calcspar, ....... 
 
 1 2 
 
 IT 8 
 
 Section at At the bridge on the Riviere a la Graisse, at Eigaud on the Ottawa, 
 there is an exposure of the upper part of the Potsdam formation and the 
 beds of passage. The dip is S. < 4, and the following is an ascending 
 section of the beds of passage : 
 
 Ft. in. 
 
 Light grey sandstone, dotted with many dark grey translucent grains. The sur- 
 face weathers into small pits, 2 
 
 Dark grey calcareous sandstone, 2 
 
 Dark grey sandstone. 1 3 
 
 Grey calcareous sandstone, 1 6 
 
 "Whitish sandstone; with two Scolithus beds at the top, 3 6 
 
 Grey hard close-grained calcareous sandstone, with geodes of calcspar, 2 8 
 
 Grey hard vitreous sandstone, 9 
 
 Grey fine and close grained sandstone, 6 
 
 Grey close grained limestone, probably magnesian, with geodes of calcspar, .... 1 6 
 Greyish and whitish sandstone, with bands of magnesian limestone weathering 
 
 reddish, 1 
 
 Greyish and whitish sandstone, with bands of limestone weathering yellow,. ... 1 7 
 
 Grey brownish-weathering magnesian limestone with geodes of calcspar, 3 2 
 
 Grey brownish-weathering magnesian limestone, with small geodes of calcspar, 8 
 Grey close grained yellow-weathering magnesian limestone, with large geodes of 
 
 calcspar, 2 
 
 Whitish sandstone, grey and calcareous in parts, 2 6 
 
 Grey sandstone slightly calcareous, with about one inch of coarse grained sand- 
 stone on the top, weathering like a Scolithus bed, 6 
 
 Grey sandstone with much calcareous matter at the top, 10 
 
 Grey close grained calcareous sandstone ; the surface weathering into grooves 
 
 and small pits, 1 6 
 
 Reddish-grey magnesian limestone, with a conchoidal fracture. It weathers into 
 
 fine grooves like ripple-mark, as if fucoids were running through it, 2 
 
 Grey close grained calcareous sandstone, with some bands more silicious than 
 others. It holds geodes of calcspar ; the surface weathers into grooves 
 and small pits. Between the layers there are coatings of hard sandstone. 
 
 The beds hold Helicotoma and Murchisonia, rather obscure,. 2 3 
 
 Reddish-grey magnesian limestone, with a few geodes holding calcspar, 2 
 
 Reddish-grey magnesian limestone, 5 
 
 40 8 
 
 On this part of the Ottawa the middle portion of the formation is con- 
 cealed ; but the summit is met with on the bank of the river above Carillon, 
 where about a hundred feet of arenaceous limestone and of a bituminous 
 
CHAP. VII.] 
 
 CALCIFEROUS FORMATION. 
 
 113 
 
 calcareous clay-stone terminate in a singular and extensively spread con- 
 cretionary layer, like that noticed in the section below Prescott. In some 
 large exposures of it on the Grenville canal, about half a mile below 
 
 19-21. CRTNOIDE^E AND BEACHIOPODA. 
 
 a 
 
 20 
 6 
 
 19. Crinoidal columns from the Calciferous formation. 
 20. Lingula Mantelli (Billings) ; a, ventral valve ; 6, dorsal valve. 
 21. Orthisina grandceva (Billings) ; a, ventral valve ; 6, ventral valve 
 shewing area and foramen. 
 
 Grenville village, surfaces of half an acre shew the concretions, consisting 
 of concentric layers seemingly cut horizontally in half and packed closely 
 together, some of them being two and three feet in diameter. 
 
 22. LAMELLIBRANCHIATA. 
 
 22. Conocardium Blumenbachii (Billings) ; a, side view ; b, posterior view. 
 
 The flat anticlinal mass of Potsdam projected northward from Beauhar- Distribution 
 nois into the county of the Lake of Two Mountains, divides the Canadian ^ he ] 
 portion of the Calciferous formation into two parts, which join over a 
 shallow saddle-shaped depression in the neighborhood of Ste. Scholastique. 
 
 In the geological map of New York, the eastern portion of this forma- 
 tion is represented as appearing near Keeseville, no very great distance 
 above the base of the Potsdam, where both are overlapped by the succeeding 
 member of the Lower Silurian series. The Calciferous there emerges with 
 a wedge-like point, and runs in a band of about two miles wide, to the 
 
114 
 
 GEOLOGY OF CANADA. [CHAP. VII. 
 
 t>rovince line ; but here the dip probably diminishes considerably, as the 
 formation in Canada spreads out on the east side of the Beauharnois 
 anticlinal to a breadth of six miles, and in some places more. With this 
 breadth, a little to the west of the Richelieu River it folds over an anticlinal, 
 the axis of which runs northward under Chambly. On the west side of this 
 the formation sweeps round the extremity of a synclinal in its progress to 
 Lake St. Louis, east of Renault's track-bed. 
 
 Lake st. Proceeding eastward from the track-beds on the east side of the Beau- 
 *"**- harnois anticlinal, white Potsdam sandstone, marked by Scolithus, and near- 
 ly horizontal in attitude, can be traced along the shore of Lake St. Louis 
 for about a mile ; there is then an interval of about a mile without any 
 exposure, beyond which the Calciferous makes its appearance. Thin inter- 
 stratified bands, more arenaceous than others, are still characterized by 
 Scoliihus, and more massive dolomitic ones by Ophileta compacta and 
 Madurea matutina. The strata are nearly flat, and, seen at intervals, 
 continue so for about six miles to the bridge over the Chateauguay River; 
 in the first two miles, these same two species of gasteropods are met with 
 hi several exposures, while the lithological character of the rock varies 
 but little the whole way. 
 
 Montreal Northward from this the formation passes across the upper end of the 
 island. igi ail (j O f Montreal, where the lower beds are characterized by Leperditia 
 Ann^a and Murchisonia Anna. It then crosses the upper end of Isle 
 Bizard, and the summit of the formation, turning more eastward, comes in 
 upon the north-west side of the upper part of Isle J6sus, leaving, through 
 the effect of gentle undulations, a broad expanse of the rock between the 
 island and the Rividre du Nord, marked near the village of St. Eustache 
 by Lingula Mantelli. North-eastward of this the breadth rapidly dimin- 
 ishes, and north of St. Lin is reduced to about two miles. Varying from 
 this to four miles, it follows the Potsdam band until it meets with the Chicot 
 downthrow, beyond which to the north-eastward it is not yet certainly 
 known for several hundred miles. 
 
 On the west side of the Beauharnois anticlinal, the Calciferous, following 
 the Potsdam in its sinuosities, completely surrounds the triangular Silurian 
 trough lying between the Ottawa and the St. Lawrence. Passing westward 
 from the track-bed on the west side of the anticlinal, the lower formation 
 can be traced with little interruption obliquely across the measures for a 
 distance of three miles up the St. Lawrence, where it becomes interstrat- 
 ified with calcareous and magnesian layers ; but at St. Timothy, three 
 miles farther up, sandstone beds holding Scolithm are still met with, and 
 Bathyurus conicus with Pleurotomaria calcifera occurs in the calcareous 
 ones. For three or four miles farther up the river the strata are con- 
 cealed by drift until reaching Grande Isle, wherQ quarries expose good 
 limestone beds resting horizontally on others of an arenaceous character. 
 
CHAP. VII.] 
 
 CALCIFEROUS FORMATION. 
 
 115 
 
 Law * 
 
 The fossils of these limestone beds appear to belong to the Chazy forma- 
 tion, of which the strata of the island may perhaps constitute an outlier. 
 The summit of the Calciferous must thus be on the mainland close by. 
 
 From this neighborhood the outcrop of the formation on the south side south side of 
 of the triangular trough runs chiefly on the south side of the St. Lawrence, 
 where it has a breadth, varying, in consequence of the smallness of the 
 dip, from ten to fifteen miles ; the greatest width being about opposite to 
 Williamsburgh, where it is wholly in New York. Notwithstanding the 
 width of the deposit, however, the only fossil species met with in Canada 
 in this part, in addition to those of St. Timothy, are Holopea ovalis and 
 Murchisonia arenarea, occurring in the township of Godmanchester. The 
 
 23-25. GASTEROPODA. 
 
 24 
 
 23. Ophileta compacta (Salter) ; a, view of the flat under side ; b, cast 
 
 of the concave upper side. 
 
 24. Maclurea matutina (Hall) ; a, view of under side ; 6, view of aperture. 
 25. Operculum of a species of Maclurea, perhaps M. matutina; a, 6, c, 
 
 exterior, side, and interior views. 
 
 great amount of drift covering the country prevents the summit of the 
 rock being seen on the Canadian side higher up the river : it is supposed 
 to be somewhere near Matilda, but the base of it has already been indi- 
 cated in the section at Battle Windmill. 
 
 From the neighborhood of Ste. Scholastique, where the inferior part of 
 the formation bends over the shallow saddle-shaped depression on the 
 Beauharnois anticlinal, the northern base runs to Lachute and the southern 
 to Rigaud, in which places they have already been indicated. The 
 summit of the formation, at right angles across the measures from 
 Lachute, occurs near the front of Chatham on the east side of the town- Chatham, 
 ship. The distance across is six miles, and the inclination of the strata 
 about seventy-five feet in a mile, which would give a thickness of 450 feet. 
 
116 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. VII. 
 
 The band in its progress westward from this, along its outcrop on the north 
 side of the triangular trough, diminishes considerably in its breadth 
 Grenviiie. towards Grenville, where, as has already been stated, it appears to overlap 
 the Potsdam for a short distance. Beyond this it seems to maintain a 
 pretty uniform breadth, following the Potsdam zone until it meets with the 
 Hull fault ; but in its progress it is often concealed wholly or in part by 
 the river, and passes to the south side of it only in Alfred, Plantagenet, 
 and Clarence. 
 
 Eigaud. At Kigaud, the summit, at right angles from the base, is concealed by 
 drift, but is probably about two miles east of the line between the eastern 
 and western divisions of the province. From Rigaud, the base of the 
 formation appears to pass close round the west end of Rigaud Mountain, 
 and then to turn south-east towards Beauharnois ; while the summit from 
 the vicinity of Rigaud on the one hand and Grande Isle on the other, is 
 projected 'twenty miles west of the mountain, through the influence of a 
 sharp anticlinal form, folding over the axis of which the rock presents a 
 low ridge running across Lochiel and two miles into Kenyon. The dip on 
 the north side of the anticlinal is sharper than that on the south ; and on the 
 crown of the arch two narrow exposures of Potsdam, each about a mile 
 long, protrude through the superior formation. They are about seven miles 
 apart, and the more easterly one is about six miles from Rigaud Mountain. 
 Dislocation. This fold thus divides the triangular trough into two subordinate syn- 
 clinals, and in its progress westward traverses the townships of Osgoode, 
 Gloucester, Nepean, March, Huntley, and Fitzroy, and comes upon the 
 Lac des Chats near the mouth of the Madawaska ; but in these townships 
 the strata on the axis of the fold have become torn asunder, and the fold 
 is represented by the dislocation which has already been alluded to as 
 bringing the Chazy and the superior rocks against the Potsdam in Nepean. 
 The fault which branches from this in Osgoode and Gloucester, and crosses 
 the north subordinate trough into Hull, brings up the Calciferous in Glou- 
 cester to abut against the Utica formation ; and from this position on the 
 south side of the trough, and a corresponding upthrow displacement 
 on the north, the two outcrops come to a point, joining at the base in 
 Bristol, and at the summit in the south part of Torbolton on the margin of 
 Lake Chaudire. The south outcrop is much the broader of the two ; it 
 flanks the Potsdam to within about four or five miles of Fitzroy Harbor, 
 but there, as has already been stated, overlaps it, and comes against the 
 gneiss, forming the Chats cascade. 
 
 On the west side of the Laurentian spur, the Calciferous, like the Pots- 
 dam, is concealed by superior deposits along the line of the main dislocation, 
 until reaching the division between the townships of Huntley and Fitzroy. 
 Here the Calciferous emerges with a wedge-shaped point from beneath the 
 Chazy and is carried by a synclinal form into MacNab, and back through 
 
CHAP. VII.] 
 
 CALCIFEROUS FORMATION. 
 
 117 
 
 Pakenham, Ramsay, and Beckwith. This trough, like the great one, is 
 divided into two subordinate synclinal forms by an anticlinal ; on the axis 
 
 27. GASTEROPODA. 
 
 <L 
 
 26 
 
 26. Pleurotomaria Ramsayi (Billings) ; a, side view ; b, view of base. 
 27. Pleurotomaria calcifera (Billings) ; a, common form ; 6, variety with 
 depressed spire ; c, view of spire. 
 
 of which, running parallel with the axis of the main fold, the Calciferous 
 
 is carried nearly to the west corner of Huntley, where it is pierced by an Huntiey. 
 
 ' 28. GASTEROPODA. 
 
 28. 'Pleurotomaria Laurentina (Billings) ; a, view of spire of small 
 specimen ; b, side view of the same ; the dotted line shows the 
 elevation of the spire in other specimens ; c, d, side views of other 
 specimens. 
 
 elliptical exposure of Potsdam, surrounding a protruding point of gneiss. 
 
 In Pakenham, within a ring of Potsdam, it constitutes the higher part of rakenham. 
 
118 GEOLOGY OF CANADA. [CHAP. VII. 
 
 the shallow outlying Silurian trough already mentioned ; and farther north 
 on the Lac des Chats it forms the rim of another outlying Silurian portion, 
 without any Potsdam coming from below it. Beneath the Allumettes 
 outlier and the adjacent ones, it appears, like the Potsdam, to be wanting. 
 
 Between Beckwith and Prescott, the base of the formation has been 
 given in tracing the summit of the Potsdam, but the summit of the Calci- 
 ferous between Gloucester and Matilda is by no means so certain. Between 
 the St. Lawrence and a line from Beckwith to Osgoode, there may be 
 upwards of 2000 square miles of the formation in an almost unbroken 
 sheet ; but the covering of drift in- this region is so general that compara- 
 tively few opportunities of observation occur, and this is particularly the 
 case in that part where the junction of the Calciferous and the Chazy may 
 be expected. To the west of the Potsdam in Gloucester, the Calciferous 
 appears to be brought against the Hudson River formation, both in Glou- 
 cester and Osgoode, by the branch fault which runs into Hull. To the 
 south-west of this, the exposures of the rock that have been met with 
 nearest to the supposed summit are at Spencer's mills on the Petite Nation, 
 and at Grant's mills lower down, in the first lot of the seventh range of 
 Edwardsburgh. In Oxford, the rock is exposed in the twenty-sixth lot of 
 the tenth range, and in the thirteenth lot of the eighth range, not far from 
 a denuded mass of quartzite belonging to the Potsdam formation or to the 
 Laurentian beneath. It occurs also near Kemptville, on the twenty-fourth 
 and thirtieth lots of the third and fourth ranges, and in South Gower on 
 the tenth lot of the ninth range. In Young, it is exposed on the eleventh 
 lot of the eighth and ninth ranges at Loyada Lake in the rear of 
 the township, and also in Kitley near the village of Kitley Corner. On 
 the Rideau canal it is seen at Smith's Falls, in a cliff of thirty feet, and at 
 Kilmarnock, Mirickville, and Nicholson's Rapids. The beds of the Cal- 
 ciferous formation have been extensively used in the construction of some 
 of the locks of the Rideau canal, and these in general afford good examples 
 of the stone. The stone has been used for building purposes at Brock- 
 ville and Prescott, and in the neighborhood of Brockville and at Mirick- 
 ville ; some of which yields good lime of a dark color, producing a mortar 
 of considerable strength. 
 
 None of this formation has been observed among the Thousand Islands, 
 and there is no certain fossil evidence that it occurs on the west side of 
 the low Laurentian ridge here crossing the St. Lawrence, either where the 
 Potsdam is present, or farther to the westward where it is absent. On the 
 west side of the ridge, following the Potsdam where this is present, and rest- 
 ing on the Laurentian series where it is wanting, there are generally met 
 with thirty or forty feet of strata almost destitute of organic remains, and 
 about the same amount with a few fossils insufficient to determine the age 
 
CHAP. VII.] 
 
 CALCIFEROUS FORMATION. 
 
 119 
 
 of the strata with certainty. The first well characterized beds which suc- 
 ceed these belong to the Birdseye and Black River formation. 
 
 It has already been stated that in the eastern part of the province the 
 formation is not recognized with certainty for several hundred miles Island8 - 
 beyond the position where it comes up against the Chicot fault. It does 
 not appear to succeed the Potsdam at St. Ambroise ; and it is not until 
 reaching the Mingan Islands, between 500 and 600 miles to the north- 
 eastward, that we have any of its characteristic fossils. At Bay St. Paul 
 and .Murray Bay, however, there is met with a calcareous sandstone 
 
 29-32. GA8TEKOPODA. 
 
 29. a, b, c, Pleurotomaria gregaria (Billings). 
 30. Eunema prisca (Billings). 
 31. Murchisonia linearis (Billings). 
 
 32. a, Murchisonia Anna (Billings) ; b, c, d, e,f, small specimens 
 supposed of the same species. 
 
 which in the latter place rests on the quartzite that has been mentioned 
 as occurring there. It probably belongs to a higher rock, but the Cal- 
 ciferous formation between that and the Mingan Islands may be covered 
 up by the waters of the St. Lawrence. 
 
 At the Mingan Islands and on the neighboring coast, there appears 
 an interesting exhibition of this formation extending from Mingan River 
 to Ste. Genevidve Island, a distance of about forty-five miles. It occupies 
 the inner range of islands and most of the coast, with the exception of a 
 projecting block of land at Clear Water Point, which is composed of the 
 succeeding deposit. The contact of the formation with the lower rock, 
 whether Laurentian or Potsdam, has not been seen ; but proceeding from 
 west to east, the summit appears to run outside of Harbor Island, and to 
 strike into the mainland in the' corner of the bay above Clear Water Point. 
 
120 GEOLOGY OF CANADA. [CHAP. VII. 
 
 From this it trends to Wood Island, so that the whole of Hunter's Island 
 and of Ste. Genevidve Island belong to this formation. 
 
 83 . GASTEROPODA . 
 
 33. Murchisonia arenaria (Billings). 
 
 The rock is here a brownish-yellow and yellowish-grey arenaceous mag- 
 nesian limestone, holding many geodes and irregular masses of yellowish- 
 white calcspar, and many nodules and patches of yellowish-white chert, which 
 sometimes replaces organic remains. The rock weathers to a dark yel- 
 lowish-brown, and presents a carious and fretted or honey-combed surface, 
 
 84. GASTEROPODA. 
 
 34. Subulites calcifera (Billings). 
 
 with a multitude of pits sinking to the depth of sometimes three and four 
 inches ; while the salient parts, which are tough and strong, often resemble 
 a confused and tangled collection of twigs ; sometimes the surface is worn 
 into rough deep fretted botryoidal shapes. The strata are in general 
 somewhat massive, and dip to the south at a small angle, probably not 
 exceeding a hundred feet in a mile. 
 
 In many parts, and particularly in the island of Ste. Genevive, there 
 are circular areas, varying in diameter from a few paces up to a hundred 
 
CHAP. VII.] 
 
 CALCIFEROUS FORMATION. 
 
 121 
 
 yards, around which the strata for a short distance dip suddenly and con- 
 siderably towards the interior, which is confusedly filled with amorphous 
 masses of rock of coarser and softer character than the strata around, and 
 yielding more irregularly and freely to the weather. In some places, where 
 partial sections of these are seen in the cliffs of the island, the areas appear 
 
 85-40. CEPHALOPODA. 
 
 37 6 
 
 35.Orthoceras Secki (Billings). 36. Siphuncle of O. : ? 37, a.O. 
 
 Montrealense (Billings) ; 6, c, sections of the same, showing the si- 
 phuncle. 38, a, b, c. 0. Lamarcki (Billings), with sections. 39, a, b. 
 0. sordidum (Billings). 40. O. deparcum (Billings). 
 
 to be connected with funnel-like forms, which suggest the idea that they Ecmains of 
 may be the effect of ancient springs, which rose to the surface through the 
 yet unconsolidated sediment, washing away the finer particles, and disturb- 
 ing and confusing the arrangement of the strata. 
 
 The Mingan development of the Calciferous formation, in a thickness 
 which may reach 250 feet, has added greatly to the number of species 
 
122 GEOLOGY OF CANADA. [CHAP. VII. 
 
 characterizing its fauna. On the island of Ste. Genevive, where chert 
 replaces some of the forms, in addition to Stenopora fibrosa ? and cruioidal 
 columns resembling some of those of the genus G-typtocrinm, there are met 
 with, Trochonema tricarinata, Madurea matutina, and the operculum of 
 another species not yet known, Helicotoma uniangulata, Piloceras Cana- 
 dense, Orthoceras multicameratum? 0. Becld, and Baihyurw Cylele. 
 
 41-43. CRU8TACEA. 
 
 41. Bathyurus amplimarginatus (Billings). 42. B. conicus (Billings). 
 43. B. Cybele (Billings). 
 
 On Hunter's Island, with Piloceras Oanadense occurs Holopea turgida. 
 In a bay near the Pointe des Morts, the rock, which is a tough yellowish- 
 grey arenaceous magnesian limestone, holds many specimens of Pleuroto- 
 maria Laurentina and Subulites calcifera. In the bay above Clear 
 Water Point there occurs a white limestone at the summit of the formation, 
 in which is found Conocardium Blumeribachii ; and in the same rock on 
 Birch Island, outside of Harbor Island, there are Pleurotomaria abrupta, 
 P. miser, Eunema prisca, and Murchisonia linearis. 
 
CHAP. VIII.] GEOLOGY OF CANADA. 123 
 
 CHAPTER VIII. 
 
 THE CHAZY FORMATION. 
 
 LIMESTONE OF GRENVILLE. SANDSTONES AND SHALES. PHO8PHATIC NODULES, WITH LINGtT- 
 L^B. MONTREAL LIMESTONES. DISTRIBUTION OF THE FORMATION. BEDS WITH ENTOMOS- 
 TRACA. OUTLIERS. HINGAN ISLANDS. 
 
 The limestone which overlies the Calciferous formation is designated 
 by the New York geologists as the Chazy limestone, from its occurrence 
 at Chazy, on the west of Lake Champlain. In Canada this limestone 
 becomes associated with sandstones and shales, and is here described as 
 the Chazy formation. Near Grenville, resting upon the band of concre- 
 tionary limestone, which is there the highest visible member of the Calcif- 
 erous formation, occurs about ten feet of a calcareous rock, having a 
 bituminous odor, and light or dark grey in color : much of it weathers to 
 a yellowish-brown. A three-feet bed of limestone at the base of this has 
 been quarried in several parts of Chatham and Grenville, for the purpose Grenvme 
 of burning into quicklime, and occasionally for building stone. The bed Umestone - 
 is fossiliferous, and contains Leperditia Canadensis, Isoschilina Ottawa, 
 and Beyrichia Logani, in great abundance, two or three inches of limestone 
 being hi some places almost made up of them. With these are associated 
 Pleurotomaria pauper, Helicotoma umbilicata, Murchisonia perangulata, 
 Cyrtodonta faba, Orthoceras Hisingeri, and Bathyurus Angelini. These 
 are considered the lower beds of the Chazy formation in this part ; but at 
 the Chute a Blondeau, about seven miles below Grenville, there is asso- 
 ciated with the strata a seven-feet bed of calcareous conglomerate, the 
 pebbles of which are of grey limestone, weathering to a lighter grey on the 
 exterior, while in the calcareous matrix are contained comminuted organic 
 remains. Four feet of dark grey yellow-weathering probably magnesian 
 limestone underlie this, and six inches at the bottom are marked by frag- 
 mentary remains of encrinites. 
 
 These calcareous strata are succeeded by about fifty feet of whitish 
 sandstone, in beds of from two or three to twelve inches, interstratified 
 
124 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. VIII. 
 
 and shales. 
 
 sandstones with bands of green shale, holding a vast collection of fucoids, of which a 
 bilobate species is the most conspicuous. Some of the sandstones are 
 porous and moderately fine grained, and yield good fire-stones, while others 
 are coarse, and, in addition to white quartz pebbles, some of them a quarter 
 of an inch in diameter, hold a multitude of black phosphatic nodules, 
 mingled with small fragments of Lingulce. The surface of some of the 
 
 a 46 6 
 
 44. Columnaria incerta (Billings) ; a, end view ; 6, side view. 
 45. Stenopora fibrosa (Goldfuss). 
 
 46. Bolboporites JLmericanus (Billings) ; a, view of the base showing the 
 small depression ; 6, c, d, side views. 
 
 sandstones display ripple-marks. From Grenville, where the beds have 
 been most exposed by the cutting of the canal, they are found to cross the 
 Ottawa to Hamiltonville in Hawkesbury, and to extend a mile and a half 
 back from the river. Half a mile beyond them a low escarpment appears, 
 the beds in which are composed almost entirely of Khynclionella plena, 
 
 47-49. BRACHIOPODA. 
 
 47. a, 6, Lingula Belli (Billings). 
 
 48. Lingula Huronensis (Billings) ; a, ventral valve ; 6, dorsal valve ; 
 
 c, transverse section ; d, longitudinal section. 
 49. Lingula Lyelli (Billings) ; a, ventral valve ; b, transverse section, 
 
 and afford good building stone. Many large loose angular blocks met 
 with before reaching the escarpment, have this species disseminated in 
 a somewhat arenaceous matrix, associated with small black phosphatic 
 
CHAP. VIII.] CHAZY FORMATION. 125 
 
 nodules and fragments of Lingulce ; and it is probable that there may be 
 some thickness of such beds between the sandstones and the more calca- 
 reous strata above. 
 
 In this neighborhood, the sandstones, although free, yield but an indifferent 
 material for building purposes, though some pretty good slabs from them 
 have been usefully applied as coping in some of the locks of the Grenville 
 canal ; but in the neighborhood of Pembroke, about 120 miles farther up 
 the Ottawa, some of the beds, of a foot in thickness, give an excellent free- 
 stone, well suited for purposes of construction. At the Allumettes Rapids 
 in this part, the sandstones rest upon the Laurentian gneiss ; and in a con- 
 glomerate bed at the base of them, dark brown phosphatic nodules occur 
 in abundance, with great numbers of Lingula Lyelli, and a few of some uodules - 
 species of Pleurotomaria or Holopea. The shells of the Lingulce are often 
 wholly or in part imbedded hi a paste of the phosphate, and, where 
 both valves are together, the interior of the shell is filled with it. The 
 Pleurotomarice are phosphatic casts of the interior of the shells. Some of 
 the nodules are two inches in length by nearly an inch in diameter, and 
 there appears little doubt that they are coproliles. By analysis it has been Lingui*. 
 found that the shells of the genus Lingula, both ancient and recent, unlike 
 most other shells, are composed chiefly of phosphate of lime ; and it is probable 
 that the phosphatic paste in which the shells are imbedded, is nothing more 
 than comminuted fragments of Lingulce, evidently the food of the animal 
 from which the coprolites were derived. These consist chiefly of phosphate 
 of lime, with small quantities of carbonates, and some organic matter, 
 which by heat evolves ammonia with an odor of burnt horn. They in- 
 clude a portion of sand and fragments of the shells of lingula, often of 
 considerable size. In this sandstone at Aylmer, where the rock is thinly 
 and irregularly bedded, Asaphus canalis occurs ; a specimen of this 
 species found there, without the head, would, if complete, measure about 
 eight inches in length. 
 
 The upper part of the formation is largely developed in the neighbor- Montreal 
 hood of Montreal, and is associated with beds almost filled by RJiyn- limestoues> 
 chonella plena, which appears to be most abundant at the top. Others are 
 made up of comminuted organic remains, in which fragments of cystideans 
 and crinoids largely prevail, giving to the rock a granular or crystalline 
 character, from the usual peculiar crystallization of these fossils. The 
 most common species among the cystideans are Malocystites MurcMsoni 
 and Palceocystites tenuiradiatus, while among the crinoids the fragments of 
 Blastoidocrinus carcliaricedens are very numerous. Associated with the 
 fragments of these two orders, Bolboporites Americanus occurs. It is 
 classed by Salter as a coral, but it presents the same crystalline peculiarity 
 as the crinoids and the cystideans. In the beds holding Rhynchonella plena, 
 Orthis platys is occasionally abundant ; and among the characteristic 
 
126 GEOLOGY OF CANADA. [CHAP. VIII. 
 
 fossils of the formation in the neighborhood, are Pleurotomaria calyx and 
 Serpulites splendens; the latter of which, often found more or less spirally 
 twisted, is usually of a deep brilliant black color, and on analysis has 
 been found, like the lingula, to be composed of phosphate of lime. 
 
 The beds of this part of the formation are massive, and afford large 
 blocks for building purposes. Those near Montreal have been employed in 
 the construction of the lower locks of the Lachine canal. The usual 
 color of the beds is grey, but they occasionally weather to a light brownish 
 tinge, and some of the layers to a decided yellowish-brown. These are 
 usually found to be of a magnesian character, and some bands and patches 
 are sufficiently so to constitute dolomites. The thickness of this part of 
 
 50, 51. BRACHIOPODA. 
 
 50. Rhynchonella pUna (Hall) ; a, ventral valve ; 6, side outline ; c, dorsal 
 
 valve. 
 61. Rhynchonella orient alls (Billings) ; four different views of two specimens. 
 
 the deposit is estimated to be about sixty or seventy feet, and the total 
 volume of the formation is supposed not to exceed 150 feet. 
 
 In its geographical distribution, the deposit appears to form a zone 
 around the geological depression between the Ottawa and the St. Lawrence. 
 In Hawkesbury, opposite to Grenville, where its presence has already been 
 alluded to, it has a breadth of about two miles ; and its upper part, among 
 other fossils, is marked by Orthis imperator. The sandstone of the lower 
 part occupies a small area in the front of the townships of Grenville and 
 Chatham, reaching nearly to Carillon, where the base crosses the Ottawa 
 to Point Fortune. From this, the formation appears to sweep round to the 
 westward into Lochiel, where it folds over the anticlinal axis which has 
 already been alluded to, and where it presents the usual abundance of 
 Rhynchonella plena, with some small black nodules of phosphate of lime. 
 Again returning eastward, the base reaches Grande Isle on the south side 
 of the St. Lawrence ; while large angular blocks of grey limestone filled 
 with Rhynchonella plena, indicate a proximity to the summit of the forma- 
 tion about a mile below Dalhousie mills on the river de 1'Isle. 
 
 From this, westward, the country is so much covered with drift that no 
 exposures of the rock have been observed until reaching Sheek's Island, 
 opposite Mille Roches, in the higher part of the township of Cornwall. 
 
CHAP. VIII.] CHAZ'Y FORMATION. 127 
 
 Here a grey limestone almost entirely composed of Rhynchonella plena, Cornwall. 
 with a few examples of Beyrichia Logani, rests on a mass of greenish shale 
 abounding in fucoids, and attests the presence of the middle part of the 
 formation. On the twenty-fourth lot of the fourth range of Cornwall, about 
 a mile and a half or two miles north of Mille Roches, a quarry is opened 
 in massive beds of black limestone, with fossils apparently belonging to 
 the succeeding formation. In the sixth lot of the same range of the town- 
 ship, in a quarry of which the stone has been extensively worked for the 
 construction of the canal locks, a similar description of black massive beds 
 occurs ; and here also some of the fossils appear to belong to the succeed- 
 ing formation, so that the summit of the Chazy would probably occur some 
 short distance north of the margin of the St. Lawrence in this vicinity. 
 
 52, 53. BKACHIOPODA. 
 
 62 
 
 62. a, 6, c, d, Camerella variant (Billings). 
 
 63. a, b, c, Camerella longirostra (Billings). 
 
 Beyond Cornwall, following the outcrop given to the Calciferous forma- 
 tion round to Osgoode, no exposures of the Chazy have been anywhere 
 observed, and its position must be taken as occupying a belt of country 
 lying between the exposures of the Calciferous on the one hand, and those 
 of the Birdseye and Black River, or of the Trenton formation, on the 
 other. In Osgoode, the deposit must come up against the same fault which Dislocation. 
 brings the Calciferous against the Hudson River formation, and there must 
 thus be a breach in the outcrop of the Chazy. In conformity with this, a 
 limestone is met with at the base of an escarpment on the twenty-second 
 lot of the fifth range of Nepean, which is supposed to represent the summit 
 of the deposit, being in the same escarpment overlaid by beds belonging 
 to the Birdseye and Black River, followed by others of the Trenton 
 formation. The escarpment is here about a mile south of the Potsdam 
 formation, towards which the beds dip at an angle of from one to three 
 degrees ; and it is probable that the Chazy comes up against the Potsdam 
 about a couple of miles to the north-eastward, on the south side of the fault. 
 
 From this, the formation is traceable into Huntley, and a considerable 
 display of it occurs on the road running across Huntley from March to 
 Ramsay, in the eighth and ninth lots, from the sixth to the twelfth ranges, 
 as well as on the same road across from the twelfth range of Ramsay to 
 Shipman's on the ninth range. In this part, the formation consists of the 
 yellowish-white sandstone in the lower part, with a grey limestone above, 
 
128 GEOLOGY OF CANADA. [CHAP. VIII. 
 
 Beds with in which there is an interstratified bed of blackish-brown limestone crowded 
 a * with bivalve entomostraca ; not far above which, are several feet of yellowish- 
 grey buff-weathering argillaceous magnesian limestone, applicable for the 
 purposes of hydraulic cement. The species in the blackish-brown lime- 
 stone are for the most part Leperditia Canadensis, many of them of the 
 variety LoucTdana. Associated with these is Bathyurus Angelini, and in 
 the grey beds occurs Strophomena alternata. Rhynchonella plena, which 
 marks the upper part of the limestone to the eastward, is in this part very 
 rare or altogether absent. On the ninth and tenth ranges of Huntley, the 
 road crosses a peat bog about a mile wide, which is probably underlaid by 
 the Calciferous formation, as the bog is on the axis of the anticlinal in 
 Huntiey anti- Huntley which has already been mentioned as bringing up a dome of 
 gneiss. The Chazy is found on each side of the bog, and, in folding over 
 this axis, reaches the south corner of Fitzroy. In rounding the southern 
 extremity of the southern synclinal, the formation reaches to some distance 
 on the line between Goulburn and Beckwith. On the south side of this 
 synclinal, the Chazy, being nearly flat or slightly undulating, presents a 
 breadth of between two and three miles for more than half-way across 
 Huntley ; but this breadth diminishes to not much more than half a mile on 
 the confines of Pakenham. On the sixth lot of the tenth range of this 
 township, it again turns upon the axis of the synclinal, and Leperditia 
 Canadensis in crowded abundance characterizes a brownish-black lime- 
 stone as before. 
 
 From this the formation probably has a considerable spread to the north- 
 eastward towards the spur of Laurentian gneiss which runs through Fitz- 
 roy. The details of its distribution in this part, however, are not quite 
 % certain. At Dickson's mills, -the formation is concealed by a dislocation 
 
 connected with the Huntley anticlinal. The dislocation, throwing the 
 measures down on the north side, brings the Calciferous against the 
 Birdseye and Black River formation ; but about half a mile to the north- 
 eastward, the Chazy emerges from beneath this latter. It is here, on the 
 north side of a shallow synclinal, subordinate to that on the north side of 
 the Huntley anticlinal ; parallel to the axis of which another anticlinal 
 occurs, about two miles and a half removed from it. The Chazy, in folding 
 over this axis, is carried forward to the second lot on the line between the 
 third and fourth ranges of Fitzroy ; but between this and the spur of Lau- 
 rentian gneiss in Fitzroy, no exposure of the rock has been observed, with 
 the exception of one about three miles to the north-east on the second lot of 
 the ninth range of the township, where it appears to abut against the gneiss 
 on the north side of the more northern synclinal. 
 
 The Chazy appears to form two patches on the Calciferous outlier of the 
 Lac des Chats, and westward to constitute the lowest rock of the outlier of 
 the Allumettes Island and pf the outliers south of it. The number of these 
 
CHAP. VIII.] 
 
 CHAZY FORMATION. 
 
 129 
 
 westward outliers is six, three of them being on the Bonnechre, and the 
 formation appears to constitute a rim to each of the six, but in the most outUers - 
 northern the rock is concealed beneath the waters of the north channel of 
 the Ottawa. 
 
 54r-56. BKACHIOPODA. 
 
 <t 3 e 
 
 54. Orthis platys (Billings); a, dorsal view ; 6, longitudinal section ; c, 
 
 ventral valve. 
 
 55. Orthis imperator (Billings) ; a, dorsal valve ; &, side view ; c, ven- 
 tral valve. 
 
 56. Orthis borealis (Billings) ; a, ventral valve ; b, side view; c, dorsal 
 valve. 
 
 On the north side of the dislocation connected with the Rigaud and 
 Fitzroy anticlinal, the Chazy follows the Calciferous formation, and occu- 
 pies, in its relative place, a large part of the northern trough west of the 
 Hull and Gloucester fault, leaving but two patches of superior rock, one 
 in Hull and the other in Nepean. In Nepean this fault brings the Chazy Nepean. 
 against the Utica formation, but in Hull it appears to abut against the HUII. 
 Trenton. The arenaceous part of the Chazy is displayed at Aylmer in 
 Hull, and in the eleventh range of Eardley, on the north side of the 
 Ottawa, as well as in March on the opposite side, overlaid in each place 
 by the limestone holding Leperditia Canadensis, and followed there, as 
 well as in Nepean, by the cement bed. In Nepean, Leperditia is accom- 
 panied by Rhynchonella plena, but this does not appear to be in great 
 abundance. 
 
130 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. VIII. 
 
 L'Orignal. 
 
 Between the Hull and Gloucester fault and Grenville, the Chazy forma- 
 tion keeps wholly on the south side of the Ottawa. In its progress it is 
 affected by four nearly parallel anticlinals, the axes of which approach to 
 north-west and south-east. Two of these have already been alluded to as 
 affecting the previously described Silurian deposits, one of them crossing 
 the Ottawa from Buckingham to Clarence, and the other from Lochaber 
 to Plantagenet. The higher of the other two crosses from Templeton to 
 East Gloucester, and the lower from Buckingham to Cumberland. In 
 folding over the former of these two, which are two miles and a half apart, 
 
 67-60. BRACHIOPODA. 
 
 60 
 
 58 
 
 57. Ortais perveta (Conrad) ; a, &, c, d, e,/, different views of two specimens. 
 58. 0. -^- Portia (Billings) ; a, ventral valve ; b, side view ; c, portion of 
 surface magnified. 
 
 59. 0. acuminata (Billings) ; a, ventral valve ; 6, side view. 
 
 60. 0. disparalis (Conrad) ; cr, ventral valve; &, side view. 
 
 the summit of the Chazy is carried two miles from the margin of the river, 
 and over the latter about a mile and a half. On the Buckingham and 
 Clarence axis, which appears to be connected with a dislocation, the dis- 
 tance is not quite certain, but it probably does not fall short of four miles, 
 while on the Lochaber and Plantagenet axis it may be about three miles. 
 In other parts the distance of the summit of the Chazy from the river 
 seldom exceeds a mile, with the exception of Alfred, where its course is 
 probably four miles south of the gneiss, which constitutes the most northern 
 part of the township. 
 
 The arenaceous portion of the formation is traceable at intervals in the 
 whole of the distance from Ottawa city, followed by the bd displaying 
 entomostraca ; and on reaching the South Petite Nation River, beds crowded 
 with Khynchonella plena again make their appearance, though they do 
 not seem to be so massive as they are in Hawkesbury. In the neighbor- 
 hood of L'Orignal some beds from two to four niches thick, which are 
 worked for tombstones and other purposes, are largely made up of this 
 fossil ; and in the entromostraca beds, in addition to some of the species 
 already named, there occurs Leper ditia amygdalina, which is the largest 
 species of this family in the formation. 
 
CHAP. VIII.] CHAZY FORMATION. 
 
 On the east side of the Beauharnois anticlinal the formation under 
 description follows the Calciferous along the margin of Lake Champlain plain 
 from the neighborhood of Keeseville to the province line, passing in its 
 course the town of Chazy, from which it takes its name. Beyond this, 
 folding over the axis of the Chambly anticlinal and under the corres- 
 ponding synclinal to the west, the formation attains Lake St. Louis, the 
 summit of it reaching some distance below Caughnawaga. At Caughna- 
 waga, beds crowded with RhyncJionella plena, accompanied with Orthis 
 boreatis, rest immediately upon the arenaceous part of the deposit. They 
 yield massive blocks of building stone, which are marked with small rose- 
 
 61 . LAMELLIBRAJf CHIATA. 
 
 61. a, 6, Vanuxemia Montrealensis (Billings). 
 
 red spots, and when cut and polished afford a pretty marble. From this 
 the formation, crossing Lake St. Louis, enters on the island of Montreal 
 above Pointe Claire, and is thence traceable to Ste. Gene vie ve, where it 
 affords very fine building stone. It then passes to Isle Bizard, which it 
 crosses about mid length, in a belt coming upon the Lake of Two Moun- 
 tains, at a point where a quarry is worked in it. In this quarry it shews a 
 grey limestone, exhibiting the same rose-red spots as at Caughnawaga, and 
 gives fine massive blocks. 
 
 The upper end of Isle Bizard displays the Calciferous formation, and Montreal 
 the lower the Trenton, which is seen above and below the seigniorial mill Island - 
 on the Riviere des Prairies. The Trenton is also displayed on the opposite 
 side of this stream for some distance, commencing a little below the extreme 
 point of Isle Je*sus. The Calciferous formation occurs a little below the 
 same point, on the opposite side of the island, on the river St. Jean au 
 Je*sus, so that the Chazy, unless it is let down and buried by a fault, must 
 enter on the island at the very extremity in a very narrow band. Widen- 
 ing as it proceeds, it sweeps round by St. Martin and the Riviere des 
 Prairies, above and at Lachapelle's bridge, the upper part of the formation 
 crossing the river to the island of Montreal in the vicinity of Isle au 
 Chats. At the south end of the bridge just mentioned there are quarries 
 in the formation, and from these it gains the neighborhood of St. Laurent 
 
132 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. VIII. 
 
 church. It is seen again on the north side of the cross-road between 
 C6te St. Laurent and C6te Ste. Catherine, running close alongside this 
 road to its junction with the Ste. Catherine road, and then turning toward 
 the Mile End road, which the summit crosses about a hundred yards on the 
 city side of the first milestone beyond the toll bar. 
 
 62. GASTEROPODA. 
 
 62. Pleurotomaria calyx (Billings) ; a, view of the flat spire ; 6, side view ; 
 c, a smaller specimen of the same. 
 
 This is the position in which, as already mentioned, the Chazy limestone 
 is quarried in the vicinity of Montreal. From it, the top of the formation, 
 after reaching northward to the cross-road from C6te St. Michel to C6te 
 de la Visitation, turns westward, and again crosses the Riviere des Prairies 
 a little below the Sault au Recollet. It sweeps round thence, probably 
 about a mile behind Les Ecors and the rocks of St. Vincent de Paul, 
 
 63. GASTEROPODA. 
 
 63. Pleurotomaria docens (Billings) ; a, view of spire ; &, side view ; 
 c, portion of band enlarged. 
 
 which are of the higher formations, and gains a position a little way west of 
 the village of Terrebonne. Making a sharp turn here, it is traceable to the 
 south-westward to within about a mile of Ste. Rose, keeping some distance 
 from the river St. Jean au Je*sus. The whole band probably crosses the 
 stream here to the RiviSre aux Chiens, a tributary joining on the north-west, 
 
CHAP. VIIL] 
 
 CHAZY FORMATION. 
 
 133 
 
 whence it runs to C6te St. Louis, where it has been quarried about three 
 miles north-eastward of Ste. ThdrSse. 
 
 In its farther progress it reaches the vicinity of St. Lin, north-west of st. Un ; trap, 
 the mills on the Little River, about half a mile above its junction with the 
 Achigan, where entire thick beds of the formation, giving fine building 
 stone, assume the rose-red color mentioned as occurring in spots at 
 Caughnawaga and Isle Bizard. Here Khynchonella plena characterizes the 
 
 64, 65. CRUSTACEA. 
 
 b *> c 
 
 64. a, bj c, Illcenus globosus (Billings) ; three different views. 
 65. a, b, c, /. Bayfieldi (Billings) ; " " 
 
 rock, and Stenopora fibrosa is associated with it in some abundance. 
 Where the Little River cuts the formation, it is paved with trap for about 
 fifty yards. About ten feet of this trap are seen in a cascade which 
 occurs at the spot. It appears to be an intercalated mass, and a calcareous 
 bed of fifteen inches, lying on the top, is converted into a highly crystalline 
 condition. Farther to the north-east the Chazy is traceable to the village of 
 
 66-69. CRUSTA CE A . 
 
 67 
 
 66. Sphcerexochus parvus (Billings). 
 67. Harpes antiquatus (Billings). 
 68. Bathyurus Jlngelini (Billings). 
 69. Amphion Canadensis (Billings). 
 
 Industry, where it occurs under the foundation of the mill, and is marked by industry. 
 Pleurotomaria staminea. From this the band appears to become thinner ; 
 and it is not at present recognised with certainty to the north-east beyond 
 the Chicot dislocation, until reaching the Mingan Islands, the interval 
 being upwards of 500 miles. 
 
134 GEOLOGY OF CANADA. [CHAP. VIII. 
 
 Mingan At the Mingan Islands the Chazy formation bears lithological charac- 
 
 ters somewhat different from those which have been given above. The 
 lowest part seen of the deposit occurs in the bay above Clear Water 
 Point, and the following is a section of the strata in ascending order : 
 
 Feet. 
 
 Reddish cream colored compact limestone with a conchoidal fracture, weathering 
 pale yellow, 1 
 
 Greenish and brownish-black shale, 1 
 
 Reddish cream colored limestone as before, in beds of from one and two inches 
 to a foot, interstratified with greenish shale in beds of about the same thick- 
 ness, 28 
 
 Greenish shale with Rhynckonella orientalis (which is a variety of -R. plena) in 
 great abundance, 3 
 
 Grey granular limestone with false bedding, holding comminuted fragments of 
 encrinites and other organic remains, including Bolboporites Jlmericanus, 
 Rhynchonella orientalis, a few of Camerella longirostrata, and other species,.. 13 
 
 Grey nodular limestone with Columnaria parva, Stenopora adherens, Fenestella 
 incepta, Orthis piger, Strophomena incrassata, Ctenodonta nasuta, Nautilus 
 Jason, JLmphion Canadensis, Harpes antiquatus, Illcenus globosus, 20 
 
 Grey magnesian limestone, with Murchisonia aspera,Maclurea Atlantica,0rthoceras 
 multicameratum, 0. bilinealun, 0. natator, O. Maro, 0. Antenor, 0. Mingan- 
 ense, 0. Shumardi, Illcenus Bayfieldi, and other fossils, 12 
 
 78 
 
 The following section, in ascending order, occurs on Large Island at its 
 most northern point ; it is supposed to belong to the Chazy formation, and, 
 from the fewness of the organic remains in it, probably overlies the previous 
 
 beds : 
 
 Ft. in. 
 
 Yellowish-grey limestone, weathering yellow, probably magnesian, 5 8 
 
 Green and black shale, 2 
 
 Yellowish-grey limestone, with Leperditia amygdalina at the top, 73 
 
 Yellowish-grey concretionary limestone, weathering yellowish-brown ; the con- 
 cretionary masses are from six to eighteen inches in diameter, and the con- 
 centric layers of the concretions thin, 4 
 
 Dull drab colored limestone, weathering slightly yellow, with nodules of chert ; 
 
 the surfaces of the beds show fucoids, 6 
 
 Dull drab colored compact limestone, weathering slightly yellow, in beds of from 
 
 six to twelve inches, , 18 
 
 Drab colored mottled arenaceous limestone, weathering yellowish-brown, in beds 
 
 of from three to nine inches, with corals, 10 
 
 Pale yellowish-grey arenaceous limestone, weathering yellowish-brown, in beds 
 of from three to nine inches, well marked with fucoids on the surfaces and 
 
 with impressions of Straparollus, 12 6 
 
 Measures concealed, "7 9 
 
 Yellowish-white arenaceous limestone, in beds of from one to two feet thick, 
 
 without observed fossils ; this would make an excellent building stone,. ... 80 
 
 Green calcareo-arenaceous shale, 1 6 
 
 Light greenish-white coarse grained calcareous sandstone, in ill defined beds, 
 with numerous obscure fragmentary fossils, and several small black nodules 
 and patches, 50 
 
CHAP. VIII.] CHAZY FORMATION. 
 
 Ft. in. 
 
 Measures concealed, 4 o 
 
 Green and grey shale, 11 o 
 
 Drab colored argillaceous limestone in even beds, some of which would probably 
 
 yield hydraulic lime ; ripple-mark occurs on some of the surfaces, 7 
 
 Greenish shale, 1 9 
 
 Greenish-drab compact limestone, mottled with yellowish-drab organic remains ; 
 
 this would make a handsome marble, 10 
 
 Greenish-drab very compact limestone, resembling lithographic stone in its tex- 
 ture, but unfitted by the presence of small transparent crystals of calcspar ; 
 the beds are from three inches to one foot thick ; this would make a very 
 
 fine building stone, 5 
 
 Light drab compact but brittle limestone, in beds of from six to eight inches, 
 
 with no observed fossils, 45 
 
 171 5 
 
 It is not certain that this includes the top of the Chazy, as between the 
 section and the lowest organic remains of the succeeding formation there 
 is a thickness of seventy-eight feet, of which the character has not 
 been ascertained. It would however appear probable that the total 
 volume of the formation in this part does not exceed about 300 feet. It 
 appears to include all the islands outside of Harbor Island, from the Perro- 
 quets to Clear Water Point, and with this point the islands to the east of 
 it as far as Wood Island. From this range, however, is excepted the 
 southern part of Large Island, which appears to belong to the succeeding 
 formation. 
 
136 GEOLOGY OF CANADA. [CHAP. IX. 
 
 CHAPTER IX. 
 
 THE BIRDSEYE AND BLACK RIVER FORMATION, AND THE 
 TRENTON FORMATION. 
 
 THE BIRDSEYE, BLACK RIVER, AND TRENTON LIMESTONES ; A GREAT GROUP. SECTION NEAK 
 MONTREAL; MOUNT ROYAL. DISTRIBUTION EASTWARD IN THE ST. LAWRENCE VALLEY. 
 MONTMORENCI FALLS. S AGUENAY ; LAKE ST. JOHN. DISTRIBUTION OP THE GROUP ON THE 
 OTTAWA ; OUTLIERS. ITS DISTRIBUTION IN WESTERN CANADA. LAKE SIMCOE. MANITOU- 
 LIN ISLANDS. LACLOCHE. ST. JOSEPH ISLAND. CAMPEMENT D'OURS. THE UNDERLYING 
 SANDSTONES. 
 
 The great mass of limestone strata which overlies the Chazy formation 
 was by the New York geologists divided into three portions, each of 
 which was supposed to be characterized by peculiar fossils. Lowest in 
 this series they placed the Birdseye limestone, so named from its peculiar 
 aspect, due to the abundance of Tetradium which it contains. To this 
 succeeds the so-called Black River limestone, followed in its turn by the 
 division which, from the Trenton Falls, has received the name of the Tren- 
 ton limestone. In their extension into Canada it has been found that the 
 distinctions between these divisions of this group are less definite than in 
 New York, and the whole series of strata is therefore described together. 
 In the tabular view given hi Chapter II. we have represented the Birdseye 
 and Black River limestones as one formation. Its characteristic fossils will 
 be introduced in the following pages before those of the Trenton formation. 
 Section at In the vicinity of Montreal we have shown that the summit of the 
 Montreal. Chazy formation consists of a mass of limestone marked by an abundance 
 of Rhynchonella plena. This is succeeded, after a short interval, by a set 
 of dark-colored limestones, of which the following is an ascending section : 
 
 Feet. 
 Measures concealed, 10 
 
 Greyish-brown compact bituminous and somewhat brittle limestone, weathering 
 to a lead-grey, in beds of from three to six inches, with a smooth conchoidal 
 fracture ; slender tube-like forms run in various directions in the rock, filled 
 with crystals of calcspar, probably replacing the remains of Tetradium 
 fibratum, 2 
 
 Dark greyish-brown compact bituminous limestone, weathering lead-grey, with a 
 conchoidal fracture, in beds of from three inches to a foot ; towards the 
 
CHAP. IX.] TRENTON GROUP. 137 
 
 Feet. 
 middle of the mass Tetradium fibratum occurs in abundance, most of the 
 
 tubes being filled with calcspar ; the beds contain univalve and bivalve 
 shells, difficult to be obtained from the brittleness of the stone, 5 
 
 Brownish-black bituminous nodular limestone intermixed with thin films of shale ; 
 some of the nodules contain fossils ; among these are Tetradium fibratum, 
 Helicotoma planulata, and Leperditia Canadensis, 1 
 
 Brownish-black compact bituminous limestone, in two beds, with Tetradium 
 fibratum, Stenopora fibrosa, Columnaria incerta? Stromatopora compacta, and 
 Helicotoma planulata 1 2 
 
 Brownish-black compact bituminous limestone in two massive beds, with Tetra- 
 dium fibratum, Cyrtodonta Huronensis, Helicotoma planulata, as well as 
 broken crinoidal stems, 5 
 
 Brownish-black compact bituminous limestone in a massive bed, with nodules 
 and patches of black chert and silicified fossils ; among the fossils are Tetra- 
 dium fibratum, Stenopora fibrosa, Rhynchonellarecurvirostra, Murchisonia gra- 
 
 cilis, M. ventricosa, Pleurotomaria lapicida, P. aperta, P. rotuloides, P. , 
 
 n. s., Helicotoma planulata, Ctenodonta nasuta, C. contracta. On the 
 top of the bed are Columnaria alveolata, Petraia profunda, Stenopora fibrosa, 
 Ctenodonta nasuta, Vanuxemia inconstans, Maclurea Logani, Trochonema 
 umbilicata, Helicotoma planulata, Orthoceras Sigsbyi, 3 
 
 28 
 
 Black bituminous limestone, not quite so compact nor so brittle as that of the 
 previous beds, nor quite so pure ; its fracture is less smooth, and there is 
 a slight tinge of yellow in the grey of its weathered surfaces. It is divided 
 into massive beds of from one to two feet thick, containing Columnaria 
 alveolata, Orthoceras Bigsbyi, and 0. multitubulatum, 10 
 
 38 
 
 The lower of these two masses represents the Birdseye, and the upper the Divisions of 
 Black River limestone of New York. In Canada, the line of demarcation the group * 
 between the two appears frequently to become very indistinct, and we have 
 in consequence been under the necessity of grouping them together. In 
 the vicinity of Montreal there is a distinct separation between the Birdseye 
 and Black Eiver formation, and the succeeding Trenton formation ; but 
 in some parts of the province, those fossils which are regarded as most 
 strongly distinguishing the Birdseye and Black River, become associated with 
 several that are characteristic of the succeeding division ; and we are not 
 prepared for the present, in representing the distribution of the whole series 
 on the map, to distinguish its parts by different colors. It will therefore be 
 convenient in this place to add to the preceding section the details of the 
 Trenton formation, premising that the strata with which it commences are 
 seen in contact with those already given. The section is as follows : 
 
 Black bituminous nodular limestones in beds varying from two to four inches, 
 separated by layers of black bituminous shale of from one to two inches 
 thick. The beds are highly fossiliferous from the very base, and contain 
 among other organic remains Stenopora fibrosa, S. petropolitana, Glyptocri- 
 nus ramulosus, Rhodocrinus pyrtformis, Pleurocystites elegans, Ptilodictya 
 
138 GEOLOGY OF CANADA. [CHAP. IX. 
 
 Feet. 
 
 acuta, Intricaria reticulata, Graptolithus amplexicaule, Leptcena sericea, 
 Strophomena alternata, Orthis testudinaria, 0. lynx, Ehynchone.Ua increbescens^ 
 Camerella hemiplicata, Lingula curta, Discina, Pelopea, Ceraurus pleurexan- 
 themus, Asaphus plalycephalus, Leperditia Canadensis, 10 
 
 Grey bituminous granular limestone in beds of from three to eighteen inches 
 at the bottom, passing into black nodular bituminous limestone at the top, 
 interstratified with black bituminous shale in irregular layers of from one to 
 three inches. The grey limestone is a mass of comminuted organic remains, 
 which consisting largely of the ruins of crinoids and cystideans, give, from 
 the peculiar crystallization of these fossils, a crystalline character to the 
 rock. Among the fossils are Stenopora fibrosa, which is very abundant par- 
 ticularly in the shale, Ptilodictya acuta, Leptcena sericea, Strophomena alter- 
 nata, Orthis testudinaria, O. lynx, Camerella hemiplicata in considerable 
 numbers, Rhynchonella increbescens, JLmbonychia bellistriata, Conularia Tren- 
 
 tonensis, Lingula Progne, Orthoceras ? Ceraurus pleurexanthemus, 
 
 Calymene Blumenbachii, and Jlsaphus platycephalus. The lowest bed is eigh- 
 teen inches thick, and in a grey granular matrix holds patches and lumps of 
 shale of about an inch in diameter ; it is succeeded by thinner beds, which 
 are grey and granular in the middle, but become black and more compact 
 towards the exterior, the black color increasing and the beds becoming more 
 nodular towards the top, 10 
 
 Grey granular bituminous limestone of the same character as before, in massive 
 beds of from ten inches to two feet thick, separated by thin partings of black 
 bituminous shale ; at two feet from the top there is interstratified a two-feet 
 band of black nodular limestone in layers of from one to four inches, separated 
 by thin layers of shale. There are extensive quarries in these grey lime- 
 stones near Montreal, from which is obtained the chief part of the stone at 
 present used in the construction of the best houses of the city. The fossils 
 of these beds are pretty much the same as those of the previous mass, 10 
 
 Black and dark grey bituminous nodular limestone, weathering light grey, in 
 beds varying from two to eight inches in thickness, separated by irregular 
 layers of black and brown bituminous shale of from one to three inches. The 
 nodular character of the limestone arises from the unequal distribution of 
 argillaceous material in the rock, causing it to weather into lumps, and ren- 
 dering it unfit for building purposes. About the middle of the mass, which 
 is the part most exposed, the following fossils, among others, are met with, 
 Stenopora fibrosa, S. petropolitana, Ptilodictya acuta, Leptcena sericea, Stro- 
 phomena alternata, Orthis testudinaria, O. lynx, Camerella hemiplicata, 
 Discinaccdata, Conularia Trentonensis, Ceraurus pleurexanthemus, Calymene 
 Blumenbachii, Jlsaphus platycephalus, Trinucleus concentricus, 150 
 
 Black bituminous compact limestone, containing about ten per cent, of argilla- 
 ceous matter ; it is divided into even beds of from three to ten inches, many 
 of which present a set of regular and parallel joints dividing them into 
 rectangular bars. The argillaceous mixture increases towards the surfaces of 
 the beds, which are separated by layers of dark brown or black bituminous 
 shale, varying in thickness from mere partings to two or three inches. The 
 limestones weather to a light grey, often with a tinge of yellow, and some- 
 times, when near trap dykes, to white. The surfaces of the beds usually show 
 in relief and often in abundance the remains of cystideans ; these are almost 
 wholly of the species Glyptocystites Logani, of which weathered masses of 
 the limestone occasionally appear to be almost completely made up. Of the 
 fossils enumerated in the nodular beds nearly every one is met with in these 
 more regular strata, though perhaps not in the same profusion, 350 
 
 530 
 
CHAP. IX.] 
 
 TRENTON GROUP. 
 
 139 
 
 It is probable that above the foregoing section there are additional beds, 
 in which the layers of shale gradually increase in thickness, so that the 
 total volume of the formation may be regarded as approaching about 600 
 feet. 
 
 70. ZOOPHYTA (B. B.) 
 
 70. Columnaria alveolata (Goldfuss). 
 
 The Birdseye, Black River, and Trenton formations * constitute one of Distribution, 
 the most persistent and conspicuously marked series of strata of the Lower 
 Silurian period on the continent of North America. In its distribution in 
 
 71. ZOOPHYTA (B.B.) 
 
 71. a, Tetradium fibratum (Safford) ; b, the same with the tubes separated 
 and scattered through the rock. 
 
 Eastern Canada, it enters the province from New York, where it occupies a 
 position on the west side of Lake Champlain, and it appears to follow the 
 Richelieu River, which discharges the lake, to within a short distance of 
 
 * The figures of the characteristic fos- those of the Trenton formation, and will 
 sils of the Birdseye and Black River forma- be distinguished by the initials B.B., those 
 tion will be given in this chapter before of the Trenton being marked TB. 
 
140 GEOLOGY OF CANADA. [CHAP. IX. 
 
 St. John. The nearest exposures occur about two miles west of the 
 town, where the rock is quarried and burnt for lime. The strata dip 
 N. N. E. < 4 and appear to belong to the smooth even-bedded limestones 
 of the upper part of the Trenton. They are very fossiliferous, and the 
 surfaces of some of the beds are crowded with various forms in high relief. 
 From these beds and from the interstratified shales, which crumble hi the 
 weather, are obtained, among other fossils, very perfect specimens of Lep- 
 tcena sericea, Strophomena alternata, and Orthis testudinaria, showing 
 the outside and inside of the shells. It is probable that the very summit of 
 the series approaches somewhat nearer St. John, but at the town itself 
 we have the Utica formation. 
 
 Chambiy Not far from this locality the strata fold over the axis of the Chambly 
 
 anticlinal, and then, sweeping round the synclinal form to the west, come upon 
 
 72. ZOOPHYTA (B. B.) 
 
 72. Stromatopora rugosa (Hall). A small and perfect specimen. 
 
 the St. Lawrence, the base being a little below the village of Caughnawaga 
 and the summit a little above the Sault St. Louis mill ; the breadth across 
 the measures on the bank of the river being about three miles. Crossing 
 to the island of Montreal, the measures spread out considerably, and, 
 while the 'summit strikes nearly straight across, the base, turning westward, 
 reaches Pointe Claire, about twelve miles higher up. In front of the 
 church at Pointe Claire there is an exposure of grey granular limestone 
 which belongs to the Chazy formation, and about a mile north of it there 
 is situated a quarry of black limestone. The dips near the church and in 
 the quarry both partake of a southerly direction ; but as the quarry displays 
 
CHAP. IX.] TRENTON GROUP. 
 
 the higher rock, being of the Birdseye and Black River formation, there must 
 be undulations or dislocations in the neighborhood to account for the rela- 
 tive attitude of the two exposures, though from the small inclination of the 
 strata these may not be important. From this quarry was obtained the stone 
 used in the construction of the piers of the north half of Victoria Bridge, while 
 that of the south half was from what is said to be the same formation, at 
 Isle la Motte, in Lake Champlain. On the north side of the Pointe Claire 
 quarry there is a vertical exposure of about thirty feet of massive strata, 
 varying in thickness from one to three feet, the blocks obtained from which 
 for the bridge ranged from four to seven tons. In the lower portion of 
 these strata Tetradium fibratum occurs in abundance, associated with 
 Murchisonia gracilis^ M. perangulata and Leper ditia Canadensis, while 
 at the top are Oolumnaria alveolata, Strophomena alternata, Oyrtodonta 
 Huronensis, Orthoceras Bigstyi, and Encrinurus vigilans. 
 
 73, 74. BKACHIOPODA (B. B.) 
 
 73 a 73 6 
 
 73. Lingula Eva (Billings) ; a, dorsal valve ; 6, ventral valve. 
 
 74. Lingula Kingstonensis (Billings) ; a, dorsal valve ; 6, ventral valve. 
 
 From Pointe Claire, the base of the series follows the zone of Chazy by Montreal 
 Ste. Genevive, Isle Bizard, Isle Je*sus, and Isle aux Chats, to the vicinity of Island - 
 Montreal, and thence by the C6te de la Visitation, C6te St. Michel, Sault 
 au Recollet, the lower part of Isle Je*sus, and the river aux Chiens to the 
 vicinity of St. Lin. The summit, pursuing a straighter course from 
 Sault St. Louis, is traceable by many exposures all the way down the 
 eastern front of the island of Montreal, in general removed about a mile 
 from the edge of the water, and always dipping easterly at a very small 
 angle. From this distribution, and from what has been said before, it will 
 be perceived that a flat anticlinal arch, of which the axis runs from the 
 north end of Mount Royal to a point a little westward of Ste. TheYese, 
 carries the Calciferous formation south-eastward into Isle Jsus, and the 
 Chazy eleven or twelve miles farther on, across this island, and across that 
 
142 
 
 GEOLOGY OF CANADA. 
 
 [CflAP. IX. 
 
 of Montreal to within three miles of the St. Lawrence. This anticlinal is 
 traversed nearly at right angles by two others, one in each of the islands. 
 This gives to the upper half of the island of Montreal the form of a shallow 
 trough, in which the series of limestones here described extends in a 
 spur from C6te St. Antoine to the upper end of Isle Je*sus, narrowed 
 
 76, 76. 
 
 -BKACHIOPODA (B. B.) 
 6 
 
 75. Obolus Canadensis (Billings) ; a, dorsal view, showing area of ventral 
 valve ; 6, side view ; c, ventral view ; d, dorsal valve of a 
 broad oval variety, 
 
 iG.Eichwaldia subtrigonalis (Billings) ; a, dorsal view ; 6, ventral ; 
 c, side ; rf, front ; e, apex, showing the foramen. 
 
 transversely in two places about six miles apart. Towards the northern 
 end of the spur at the White Horse Rapid, on the Riviere des Prairies, 
 about two miles below Isle Bizard, there is a part in the trough deeper 
 than the others, which holds a small isolated patch of the black shales 
 of the succeeding formation. 
 
 The main body of Mount Royal is an intruded mass of trap. The stratified 
 rocks that are entangled with it on the east side appear to belong to the 
 upper part of the Trenton, and those on the west to the Birdseye and 
 Black River formation. The grey limestones towards the base of the Trenton 
 are probably overlaid by the igneous rock. A superficial area of about 
 TOO acres, resembling in shape the frustrum of a wedge, is occupied by 
 
CHAP. IX.] TRENTON GROUP. 143 
 
 the trap, the highest part of which is about 750 feet above the St. Law- 
 rence in the harbor of Montreal. From this mass the strata dip on 
 both sides, more rapidly on the east than on the west, the inclination on 
 
 77, 78. BKACHIOPODA (B. B.) 
 a 77 6 c a 
 
 W.Camerella Volborthi (Billings) ; a, 6, c, ventral, side, and dorsal views. 
 78. Camerella Panderi (Billings) ; a, 6, ventral and dorsal views. 
 
 the former being about ten degrees. On this side, the flank of the hill, to 
 the height of about 360 feet above the river, is occupied by limestone 
 strata, the rise of which near the reservoir terminates in two or three abrupt 
 
 79-83. LAMELLIBRANCHIATA (B. B.) 
 79 
 
 
 a 80 b a 81 b 82 
 
 79. Ctenodonta abrupta (Billings) ; a, 6, c, three different views of the 
 
 same specimen. 
 80. Modiolopsis Maia (Billings) ; a, view of right valve ; &, dorsal view. 
 
 81. M. Nais (Billings) ; a, view of right valve ; 6, dorsal view. 
 
 82. Cyrtodonta Leucothea (Billings). 
 
 83.*Conocardium immaturum (Billings), enlarged ; a, natural size. 
 
 steps, presenting successive narrow terraces. On these the dip, approaching 
 the trap, moderates almost to horizontality, and the attitude of the two rocks 
 is such as to leave it doubtful, without farther evidence, whether the lime- 
 stone runs under the trap or abuts against it. 
 
 Around Mount Royal a great many dykes and interstratified masses of Trap Dykes, 
 trap are met with, all probably related to the igneous mass of the moun- 
 tain. The quarries in the limestones of the formations from the Chazy to 
 the Trenton inclusive, in the rear of the city, display a number of the 
 dykes of various thicknesses, up to three and four feet. They appear to 
 run in various directions^ one set approaching north, with the strike, and 
 another at right angles, so as to intersect one another as well as the lime- 
 
144 GEOLOGY OF CANADA. [CHAP. IX. 
 
 stone. In some of the quarries, the limestone having been removed from 
 among them, the dykes are left standing up several feet above the bottom 
 of the quarry, and present in a marked manner the various details of the 
 cracks they once filled. Very few of these cracks appear to be accom- 
 panied by important vertical displacements : most of the slips which have 
 been observed do not exceed from a few inches to one or two feet, and 
 this is not sufficient to disjoint in any remarkable degree the outcrops of 
 the strata, notwithstanding the moderation of the dip, which seldom exceeds 
 five degrees in inclination. 
 
 84-87. GASTEROPODA (B.B.) 
 
 a 85 b 
 
 84. Straparollus asperostriatus (Billings). 
 
 85. Straparollus Circe (Billings) ; a, view of spire ; 6, umbilicus ; c, aperture. 
 86. Straparollus Eurydice (Billings) ; a, view of aperture ; 6, back view. 
 87. Pleurotomaria Eugenia (Billings) ; a, 6, c, three different views of the 
 same specimen. 
 
 An intercalated mass of trap, of some importance, crosses the Papineau 
 road about a mile and a half from the St. Lawrence. It has been fol- 
 lowed on the strike of the limestone for about five miles to the northward, 
 but southwardly it is lost beneath the drift sand and clays in less than half 
 a mile. If the band were carried farther forward in this direction, it 
 would come into place about ten acres to the east of the trappean precipice 
 of that side of Mount Royal. The direct breadth of the band in the 
 vicinity of the Papineau road is between 200 and 300 yards. It is 
 divided into two thick layers, and exhibits two distinct escarpments running 
 parallel to one another. It dips with the stratification of the smooth even- 
 bedded black limestones overlying it, at an angle of about five degrees, which 
 would give a thickness of between fifty and eighty feet. That it is 
 an intruded mass, and not an overflow, is made evident by the fact that a 
 foot or two of the overlying limestone is occasionally met with in the con- 
 dition of a breccia, of which the fragments are held together by the trap 
 as a matrix. 
 
CHAP. IX.] 
 
 TRENTON GROUP. 
 
 145 
 
 Between Ste. The're'se and St. Lin, the junction of the Chazy and Birds- st. 
 eye limestones is displayed about a mile north of the church of Ste. Anne 
 des Plaines, and an escarpment, on the summit of which the road to St. 
 Lin runs for about a mile, is composed of the upper of these rocks. The 
 junction of the deposits crosses the road dividing the seigniories of Terrebonne 
 and Lachenaye, probably a short distance south-east of the point where this 
 road is intersected by the one to St. Lin, and it thence sweeps round to 
 the village of St. Lin on the Achigan. The occurrence of the Chazy to 
 the north-west of the mills on the Little River, above its junction with the 
 Achigan, has already been mentioned. Farther down on the Achigan, the 
 Black River division, marked by Columnaria alveolata, is seen at the 
 bridge just below Mr. Pangman's mill, leaving room for the Birdseye 
 
 88 
 
 89 
 
 88-95.-T-GASTEROPODA (B. B.) 
 
 b 90 91 
 
 88. Eunema strigillata (Salter). 
 89. a, 6, Eunema cerithioides (Salter). 
 90. Cyclonema semicarinata (Salter). 
 91. Holopea Pyrene (Billings). 
 
 92. Trochonema umbilicata (Hall). 
 93. Murchisonia serrulata (Salter). 
 94. Murchisonia Jlrachne (Billings). 
 95. Metoptoma Erato (Billings) ; 
 a, 6, side and dorsal views. 
 
 between the two localities ; while about three quarters of a mile still farther 
 down, though probably not more than 200 yards directly across the meas- 
 ures, black and grey limestones are met with, representing those near the 
 base of the Trenton at Montreal. 
 
 Proceeding from this position across the measures towards the St. Law- 
 rence, there is a breadth of between four and five miles, in which the strata 
 are concealed for a considerable distance to the right and left, on the strike. 
 Beyond it, black limestones, higher in the series, occur on the river St. 
 Esprit, at the bridge on the road from St. Rocque to St. Jacques, and at 
 intervals on the stream, to the vicinity of Mr. Viger's mills, not far from 
 
 K 
 
146 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 where the stream crosses the boundary line between the seigniories of St. 
 Sulpice and L'Assomption. South-westward from this, black limestones, 
 interstratified with a considerable amount of black shales, are exposed on 
 the Achigan at the village of St. Rocque, and for a mile up to the junction 
 of the Ruisseau des Anges. The limestones, which are in beds of three or 
 
 96-99. GASTEROPODA (B. B.) 
 
 98 
 
 96. Bellerophon sulcatinus (Emmons) ; a, side view ; b, dorsal view. 
 97. Bellerophon Charon (Billings) j a, side view ; 6, front view. 
 98. Bellerophon disculus (Billings). 
 99. Bellerophon Jlrgo (Billings) ; a, front view ; 6, side vie.w. 
 
 four inches, are characterized by Leptcena sericea, Orthis testudinaria, 
 Ceraurus pleurexanthemus, and Calymene Blumenbachii, and the shales, 
 some of the layers of which are three feet thick, by a lAngula resem- 
 bling L. curta, and by G-raptoliihus pristis. The latter species is referred 
 by Hall to the Utica slate, and it is probable that the beds may not be 
 far below the base of this formation. 
 
CHAP. IX.] 
 
 TRENTON GROUP. 
 
 147 
 
 Farther down the Achigan, where it intersects the line between the two 
 seigniories mentioned in the last paragraph, there is an exposure of black 
 limestone of the Trenton formation, and about half a mile from this, to the 
 south-east, black shales of the Utica formation make their appearance. 
 
 100. LAMELLIBRANCHIATA (B. B.) 
 100 
 
 100. Matheria tener (Billings) ; a, dorsal view ; 6, interior of right valve ; 
 c, exterior of left valve ; rf, interior of left valve. 
 
 \ 
 
 But above these positions, on the stream, and about half a mile to the south- intruded 
 west of the boundary line, there is a considerable exposure of trap, the 
 course of which would carry the intruded mass between the limestones and 
 
 101 
 
 101-103. LAMELLIBKANCHJATA (B.B.) 
 
 102 a 
 
 103 a 
 
 101. Cyrtodonta obtusa (Hall) ; a, left valve ; 6, interior of left valve. 
 102. Cyrtodonta Huronensis (Billings) ; a, left valve ; 6, interior of left 
 
 valve. 
 103. Cyrtodonta cordiformis (Billings) ; a, right valve ; 6, dorsal view. 
 
 the shales, and there may possibly be some dislocation connected with it. 
 Trap occurs also about two miles below St. Rocque : it is in nearly hori- 
 zontal beds, but the sedimentary strata with which the igneous rock is 
 associated are not visible. 
 
 Between the Achigan and the outcrop of the Birdseye and Black 
 River formation, in its range from the neighborhood of Terrebonne to St. 
 
148 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 Terrebonne. Lin, there is an area of about 200 square miles, which the anticlinal 
 of Isle Je'sus throws into a synclinal form, with a breadth of about 
 fifteen miles. The dips along the outcrop show that the trough must 
 be very shallow, and it is probable that there may be several minor 
 undulations subordinate to it. The area however is very much covered up 
 with drift, and there have been no facts ascertained to determine whether 
 
 104 
 
 104-106. LAMELLIBKANCHIATA (B. B.). 
 b 
 
 104. Cyrtodonta rugosa (Billings) ; a, right valve ; 6, interior of right valve. 
 105. Cyrtodonta subcarinata (Billings), right valve. 
 106. Cyrtodonta Canadensis (Billings), left valve. 
 
 Naquareau 
 River. 
 
 Industry. 
 
 any of the Utica formation occurs in it. The only exposures of rock that 
 have been met with are at Mr. Pangman's mills on the Mascouche, and 
 upwards of a mile to the south-east, on the road from these mills to the 
 village of St. Henry. In both of these localities black limestones of the 
 Trenton formation occur ; and as the dip in each, though at a small angle, 
 is towards the south-east, there must be a shallow synclinal crossing the 
 road between St. Henry and Isle Je'sus. 
 
 On the Naquareau River there is an exposure across the Birdseye, Black 
 River, and Trenton formations, extending from the Dalles, about a mile 
 and a half above the junction of the Red River, to a point about two and 
 a half miles below it ; and there is another of the same measures from three 
 to five miles to the north-east, on the Assumption River, extending from the 
 village of Industry to a large island in the stream, just ten miles, in a 
 straight line, from the St. Lawrence. The distance across the strata 
 in a direct line is a little over two miles and a half ; the dip, which varies 
 from S. S. E. to S. E., does not exceed two or three degrees, and the 
 whole thickness reaches a little over 480 feet. This section, which rests 
 upon thirty feet of Chazy, under the foundation of the mill and upper 
 bridge at the village, consists of nearly fifty feet of Birdseye and Black 
 
CHAP. IX.] 
 
 TRENTON GROUP. 
 
 149 
 
 Biver, marked by Tetradium fibratum and Columnaria alveolata. Above 
 this, some of the lower beds of the Trenton, varying from six inches to a 
 foot in thickness, give good building stones, which have been used on the 
 spot for the construction of the railway bridge over the river. The grey 
 beds are included in a total thickness of ninety feet, above which are 140 
 feet of dark grey nodular limestone, succeeded by 200 feet of black lime- 
 stones of smoother and somewhat more brittle character. It is not cer- 
 tain that these beds reach the summit of the Trenton formation. 
 
 Between the Naquareau and the Achigan there is a partial exhibition of st. Paul, 
 the same beds, from the Birdseye upward, on the Red River and at the 
 village of St. Paul ; but following the strike lower down the valley of the 
 St. Lawrence, the whole mass constitutes a low ridge, distinctly traceable 
 for eight miles in a direction approaching E. N. E., the breadth of which 
 gradually diminishes the whole way, until at this distance it comes to a 
 point, and disappears about a mile and a half south-west from Mr. Olivier's 
 mills on the Bayonne. The Birdseye and Black River strata running on 
 the north-west side of this ridge, are exposed on the river Chaloupe, and 
 so is the upper part of the Trenton beds, but the Chazy are concealed. 
 
 107. CEPHALOPODA (B. B.) 
 
 107. Orthoceras Bigsbyi (Stokes) ; a, fragment of the siphuncle separated 
 from the rock ; 6, a longitudinal section shewing the siphuncle and 
 the septa. 
 
 Immediately below Olivier' s mills- there is a section which exposes 420 Dislocation, 
 feet of the Trenton formation, and occupies about a mile on the Bayonne. 
 Just at the mills, some of the dark colored limestones of the lower part 
 of the deposit are seen abutting against the light grey geodiferous beds 
 of the Calciferous formation, affording clear evidence of the same fault 
 
150 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 which has already been alluded to as dislocating the Potsdam near Mr. 
 Cuthbert's mills on the Chicot. At these latter mills, which are nearly six 
 miles to the north-east of the Bayonne, and at a spot a mile lower down on 
 the Chicot, dark colored bituminous limestones are again met with. The 
 more south-eastern exposures are of the Trenton formation ; those at the 
 mills are lower beds of the same formation, and they reach to within three 
 quarters of a mile of the Laurentian gneiss. The Trenton may abut against 
 the gneiss ; but the interval being covered with drift, this has not been 
 positively ascertained. 
 
 Following the road leading from Cuthbert's mills through C6te St. Jac- 
 ques and C6te St. Joachim, we meet with three exposures of black bituminous 
 limestone in the latter, the whole of them belonging to the Trenton formation. 
 The first one, with a dip of five degrees to the south-eastward, reaches to 
 within a little over a mile of the general range of the gneiss ; and the other 
 
 108, 109. CEPHALOPODA (B.B.) 
 
 108 
 
 109 
 
 108. Orthoceras anceps (Hall) ; a, view of a specimen showing the 
 
 siphuncle and the septa ; 6, transverse section. 
 109. Cyrtoceras exiguum (Billings). 
 
 two, upon the river Cache'e and one of its tributaries, to about half that 
 distance, where they show a scarcely perceptible inclination. That on the 
 Cache'e is at Mr. Hamelin's mills, where the thickness displayed is ten 
 feet. In a range with these three Trenton exposures, there is another 
 with a dip of not over three degrees in the fief Carufel, about a mile and 
 a half from the south-western boundary, again about a mile from the gneiss. 
 On the Maskinonge* River, the black beds of the Trenton are covered up ; 
 but at the foot of the cascade which the stream sends down the flank of 
 the Laurentian rocks, calcareous beds containing a great amount of silicious 
 grains, and resembling some of those of the Chazy at the Dalles on the 
 Naquareau, may belong to this formation, and their dip, which is still to 
 
CHAP. IX.] 
 
 TRENTON GROUP. 
 
 151 
 
 the south-eastward, being raised to an angle of fourteen or fifteen degrees, 
 seems to indicate a proximity to the fault. 
 
 In the sixteen miles between the Bayonne and the Maskinonge*, it is not 
 easy to decide with certainty where to draw a line representing the sum- 
 mit of the Trenton formation. No traces of the Utica formation have been 
 discovered in the whole distance, nor indeed have exposures of any rock 
 been heard of between those already mentioned and the St. Lawrence. 
 The nearest approach yet known to the upper limit of the Trenton in this 
 area is therefore indicated by the upper beds on the Bayonne, and by 
 an exposure which occurs on the Little River du Loup, two miles beyond 
 the Maskinonge', in the parish of St. Ursule, a mile S. E. of the church. 
 This locality is about four miles, across the measures, from the gneiss. 
 
 110-113. CBUSTACEA (B. B.) 
 
 a b c 
 
 110. Illcenus Conradi (Billings), three views of a rolled-up specimen ; 
 
 a, the head ; 6, the thorax ; c, the tail. 
 
 111. lllanus conifrons (Billings) ; a, upper surface of head ; 6, side view. 
 l\'2.lllct>nus Milleri (Billings). 
 
 113. Illcenus angustieollis (Billings); a, back part of head; &, front ; 
 c, oblique view of one of the cheeks ; rf, side view. 
 
 Between the Little River du Loup and the St. Maurice the distance is Grand 
 nineteen or twenty miles, and the breadth from the outcrop of the gneiss 
 to the margin of Lake St. Peter and the St. Lawrence is twelve or thirteen. 
 The area may thus be considered to contain 240 square miles. In the 
 whole of this, only two exposures of the fossiliferous rocks have been met 
 
152 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 with. One of them is on the St. Charles brook, on the property of Mr. 
 Honore* Plauder, in the seigniory of Grand Pre*, not far from the division 
 between it and Dumontier, and about a mile and a half removed from the 
 gneiss ; the other is at the falls of the Little Yamachiche River, where this 
 is crossed by the road leading from St. Joseph to the GrSs. In the latter 
 place, the beds, which have a total thickness of about fifteen feet and con- 
 tain nodules and patches of chert, are nearly flat, but the geographical 
 position would appear to indicate a gradual turn in the strike, conforming 
 with the trend in the gneiss. 
 
 The rock which overlies the Potsdam on the St. Maurice is a limestone 
 in which the fossils are too obscure to determine its age. In lithological 
 characters it resembles the Birdseye formation, and whatever portion of the 
 Trenton is on the river must be concealed between the position of this rock 
 and Pointe a la Hache on the left bank of the river, nearly opposite the St. 
 Maurice forges, where there occurs an exposure of the Utica formation. 
 
 Between the St. Maurice and the Batiscan there is a distance of about 
 eighteen miles, which for a breadth of from ten to twelve miles presents a 
 nearly level surface covered with drift. The same character belongs to 
 an additional space between the Batiscan and the Charest, with that part 
 of the Ste. Anne de la Parade which is below the junction of its tributary. 
 The distance between these last limits is about seven miles ; and from the 
 St. Maurice, the whole space between, the gneiss and the St. Lawrence 
 may comprise an area of about 200 square miles. In the whole of this 
 there have as yet been discovered only two exposures of the fossiliferous 
 formations. These both occur in the Ste. Marguerite range : the first, belong- 
 ing to the Trenton, in Cap de la Madeleine seigniory, about four mile& from 
 the St. Maurice ; and the other, on the Riviere au Lard, a tributary of the 
 Champlain, about five miles and a half farther on, in the seigniory of Cham- 
 plain. In the latter exposure, the brook on which it occurs cuts across 
 the measures in a south-east direction for about a mile, and the strata, pre- 
 senting a dip with the stream of from two to two and a half degrees, may 
 have a total thickness of about 200 feet. The chief part of this belongs 
 to the Trenton formation ; but Columnaria alveolata^ occurring in abun- 
 dance at the base, shews it to include portions of the Black River. 
 
 Between the Charest and the line between the seigniories of Deschambault 
 and Portneuf, the exposures of limestone are numerous, and the measures 
 to which they belong are thrown into a synclinal form by the Deschambault 
 anticlinal. The axis of this runs from a spur of gneiss, which is upwards of 
 two miles north of the church of Deschambault, to the church of Grondines. 
 The most easterly exposures seen in the trough are at the Three Rapids 
 on the Ste. Anne, where a black bituminous limestone is met with, within 
 ten acres of the boundary between Deschambault and Portneuf, and within 
 half a mile of the gneiss. The dip is down the river (S. 86 W. < 7) ; the 
 
CHAP. IX.] TRENTON GROUP. 
 
 beds visible have a transverse measure of 650 yards, giving a thickness of 
 250 feet. The beds are thin, and at the base much loaded with nodules 
 of chert, and occasionally interstratified with very thin layers of the same Portneuf. 
 mineral, while at the summit occasional crystals of blende occur. The most 
 common fossils are some of those characteristic of the Trenton formation, such 
 as Stenopora fbrosa, 8. petropolitana, Leptcena sericea, Stropnomena 
 alternata, Orthis testudinaria, 0. lynx, Rhynchonella increbescens, I/ingula 
 riciniformis, with an undetermined Orthoceras, some of which are replaced 
 by chalcedony and beautifully weathered out. Three miles farther down 
 the river, and over a mile and a half from the gneiss, the same characteristic 
 fossils, in a similar state of silicification, occur at a spot called the Cascades, 
 close upon the division line between Deschambault and Chevrotiere. From 
 this for twenty acres to St. Olivier bridge, and for some distance below, the 
 river is confined to a narrow channel, with vertical sides of limestone rock, 
 
 114, 115. CBUSTACEA (B. B.) 
 115 
 
 ll.Bathyurus extans (Hall). 
 
 115. Bathyurus Smithi (Billings), an imperfect head of this species, 
 enlarged ; a, natural size. 
 
 between which the current is sufficiently strong, in some parts, to make them 
 difficult of examination. Among the fossils at and immediately below the 
 bridge are Stenopora petropolitana, Ptilodictya acuta, Strophomena 
 alternata, an undetermined Orthis, lAngula Briseis, with an undetermined 
 Cyrtodonta in great abundance, and Asaphus platycephalus. The distance 
 north-westward from the bridge to the gneiss is between two and three miles, 
 and the beds are probably higher in the series than those preceding. 
 Rocks of the Trenton are laid bare in many places farther down the river, 
 the last of which is at a rapid some distance above the mouth of the Charest. 
 The dip of the beds is S. 11 W. < 1 3. The strike would run to a 
 point a little way up the Charest ; and not far from the spot, beds are seen 
 holding characteristic fossils of the Trenton formation. 
 
154 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 Deschambault. 
 
 From these last positions the summit of the Trenton sweeps round by an 
 exposure near the south-western boundary of the fief Dorval, about a 
 mile and a half from the St. Lawrence. It crosses the river-side road to 
 the Grondines, about a mile within the seigniory, and comes upon the water 
 of the St. Lawrence at Pointe a Magon, a little above the ruins of the 
 old church and windmill at the Grondines village. 
 
 From Pointe a Mac,on to the Chevrotiere, a distance of about four miles, 
 the coast consists of a naked and often vertical cliff of the same limestone 
 in slightly inclined strata, piled up in some places to the height of a 
 hundred feet over the water, and the road on the summit runs on a bare 
 ledge almost the whole way. It is towards the upper end of this cliff that 
 the upper part of the Trenton folds over the Deschambault anticlinal. 
 From the mouth of the Chevrotiere a road runs back in a nearly straight 
 line across the concessions to St. Olivier bridge on the Ste. Anne ; a parallel 
 road runs some distance from the mouth of Belle Isle brook ; and on both 
 these roads, and in various parts of the seigniory of Che vrotidre, the Trenton 
 formation is largely exposed. Extensive quarries are worked in it on the 
 first mentioned road in the fourth concession, where massive granular beds 
 of a light yellowish-grey give a very excellent building stone, which some- 
 what resembles that from the grey beds of the Trenton at Montreal ; but 
 the Chevrotire, or as it is commonly called the Deschambault stone, is 
 more evenly colored, yellower, more granular, and softer than that of Mont- 
 real. If in the same stratigraphical place as the Montreal grey beds, these 
 of ChevrotiSre, being towards the middle of the general trough, must be 
 brought to the surface by an. undulation. Associated with the fossils most 
 commonly marking the Trenton, these beds contain Capulus Trenton- 
 ensis, not remarked elsewhere in this formation. 
 
 Following the upper part of the formation from the mouth of the Chevro- 
 tire, the rock crosses the Belle Isle brook and the adjacent road more than 
 a mile from the coast, and is seen in a quarry, where it shews massive beds 
 of a dark grey color with thin patches of black shale. Small cracks and 
 crevices in the beds are filled with a black mineral, supposed to be altered 
 bitumen, which, resembling coal in its color and its inflammable properties, 
 has occasionally been mistaken for this species of fuel. The quarry is 
 about a mile from the St. Lawrence, and, rising in a step in the land, close 
 in front of the limestone, the shales of the Utica formation appear dipping 
 S. 13 W. < 35. 
 
 Where this step comes upon the road between the first and second con- 
 cessions of Deschambault, the limestone is seen again, with the shales in 
 front of it, on the road which turns from the water side to the interior, about 
 half a mile below Deschambault church. The exposure is about a mile from 
 the river-side road. As in the quarry, the beds are massive ; but there 
 appears an irregularity at the spot, perhaps occasioned by a transverse 
 
CHAP. IX.] TRENTON GROUP. 155 
 
 fault, the dip being N. 56 E. < 46, while the general extended course 
 of the strata is north-eastward. 
 
 The gneiss of the Deschambault anticlinal comes out about a quarter of 
 a mile behind the limestone, and continues in the same relation to it and 
 to the Utica formation, up to the division line between Deschambault and 
 Portneuf. Beyond this, the Trenton limestone is exposed in the seigniory 
 of D'Auteuil, above and below the bridge over the river Portneuf on the D'Auteua. 
 St. Basil road, where it stretches along the road for between twenty and 
 thirty acres. South of the river, there are indications of a transverse 
 breadth of from sixty to seventy chains of the limestone ; the dip at 
 the bridge being S. 44 E. < 2. The gneiss rises about two miles to 
 the north-west, but the interval is concealed. 
 
 On the axis of the Cap Sant anticlinal, the gneiss is succeeded by a cap ssmte 
 few calcareous beds, in which the fossils are obscure ; but strata with Tren- antlcUnal - 
 ton fossils make their appearance at the upper bridge on the Jacques 
 Carder River, and afford a deep channel for the river down to the middle 
 one. Here, making a detour round a narrow neck of land, the water, con- 
 fined by the solid masses of rock on each side to a breadth of fifteen feet, 
 rushes with great violence under the bridge, descending many feet in a 
 short distance, and causing a considerable difference of level on the oppo- 
 site sides of the neck. Across this neck, a body of water sufficient to drive Jacques 
 a mill finds a subterranean passage, and pours out from an opening in the 2^ r er 
 vertical cliff on the lower side. A short distance below the mill which has 
 been erected here, the summit of the Trenton, leaving the right bank of 
 the river, appears to run along a line very nearly coincident with the road on 
 this side, for rather less than three miles. It then folds over the axis of 
 the anticlinal about half-way between this road and the next parallel with 
 it on the north-west, and about half way in a straight line between the 
 upper bridge and Cap 8ante* church. On the axis of the anticlinal, the 
 distance between the highest Trenton beds and the gneiss is about four 
 miles and a half. 
 
 A great development of limestone occurs at Pointe aux Trembles. It pointe aux 
 occupies somewhat less than three miles along the margin of the St. Law- 
 rence, presenting a low cliff, and the promontory near the church stands 
 almost in the middle of it. The fossils, which are abundant, shew the 
 rock to belong to the Trenton formation, and it here constitutes that part 
 of the Trenton zone which folds over the Pointe aux Trembles anticlinal. 
 On the north-westerly side of the anticlinal, the summit of the formation, 
 striking into the country, appears to run in a north-easterly direction, and 
 to cross the St. Nicholas road about two miles from the St. Lawrence, 
 which would give about a mile and a half as its distance from the gneiss on 
 that side of the axis. Farther on, it would again cross the road in sweep- 
 ing round with the trend of the gneiss to gain the same part of the forma- 
 
156 GEOLOGY OF CANADA. [CHAP. IX. 
 
 tion on the Jacques Cartier. On the north-west side of the anticlinal, and 
 not far removed from the gneiss, massive beds of limestone of a grey color 
 and granular texture occur on the land of Mr. J. Gagne* and others, afford- 
 ing excellent building material. The stone resembles that of the grey 
 beds of the Trenton at Montreal. 
 
 On the south-east side of the anticlinal, the dip is more precipitous than 
 on the north-west, and the strata on that side are broken and let down by 
 a fault. The position and course of this dislocation are plainly seen on 
 the beach at and near a spring a short distance above Mr. Dubord's ship- 
 yard, where strata of the Utica formation are brought against those of the 
 Trenton without any of that interstratification of calcareous and argilla- 
 ceous layers which indicates the passage from the one to the other. The 
 course of this dislocation, in its continuation, strikes the south-east side of 
 the Bonhomme Mountain ; and near the line of division between Pointe aux 
 
 116-118. ZOOPHYTA (TR.) 
 
 117 118 
 
 116. Stenopora fibrosa (Goldfuss). 
 117. S. petropolitana (Pander). 
 118. Petraia corniculum (Hall). 
 
 st. Augustin. Trembks and St. Augustin, the Trenton formation is wanting, and the 
 Utica shales come in contact with the gneiss. In this relation, these rocks 
 cross the seigniory of St. Augustin ; the Utica shales, which on the west 
 side of the seigniory are not more than one sixth of a mile wide, gradually 
 increasing to more than a mile on the east. A considerable distance far- 
 ther on, a narrow strip of Trenton limestone becomes interposed between 
 the shales and the gneiss, both rocks being tilted up to a high angle as 
 they approach the gneiss. 
 
 st. Ambrose. Arriving at St. Ambroise the limestone gets wider, and a few beds of 
 white sandstone (already alluded to) of the Potsdam formation, in all 
 about twenty feet thick, present themselves. These are overlaid by a bed 
 or two of grey granular limestone with Leper ditia Canadensis, associated 
 with Orthis testudinaria, and Oamerella hemiplicata. These grey beds 
 are followed by black limestones with Orthoceras Bigsbyi and L/ituites 
 undatus, belonging to the Black Kiver; but in the same fragment 
 of rock with the former there is Orthis testudinaria, and with Lituites are 
 
CHAP. IX.] 
 
 TRENTON GROUP. 
 
 157 
 
 Trinudeus concentricus and Conularia Trentonensis, which are character- 
 istic Trenton forms. On the river St. Charles, close by, these black lime- 
 stones rest upon the gneiss without the intervention of the Potsdam, and they 
 are followed by beds belonging to the Trenton, showing a united breadth 
 of about 700 yards, and dipping at an angle varying from fifteen to twenty 
 degrees, which gives about 600 feet of thickness. 
 
 On the Rividre des Metres, the width of the limestones increases, the 
 summit being below the mill on the Jeunne Lorette and Charlebourg road. 
 At Charlebourg, the summit passes near the church ; on the Bourg Royal 
 
 119. ZOOPHYTA (TK.) 
 
 119. Arthrochma pulchella (Billings); o, a portion of the principal stem 
 and of one of the branches enlarged. 
 
 road, it is about half a mile from the gneiss ; and beyond this, the formation 
 
 sweeps round in accordance -with the anticlinal of Montmorenci, attaining 
 
 a breadth of perhaps about four miles on the synclinal axis, which would 
 
 cross the road from Beauport to Laval, about two miles and a half from 
 
 the St. Lawrence. This breadth it maintains until reaching the anticlinal 
 
 axis. The summit of the formation comes upon the Quebec and Beauport Beauport. 
 
 road, a little west of the river Beauport ; and in a quarry on the north 
 
 side of the road, at the turn to Beauport bridge, there appears to be an 
 
 irregularity in the dip, connected probably with some dislocation. From 
 
 S. 13 W. < 28 on the west side of the quarry, it becomes .N. 84 W. 
 
 < 6 on the east. 
 
 The Montmorenci anticlinal, like that at Pointe aux Trembles, shows a 
 more precipitous dip on the south-east than on the north-west side ; and it 
 seems also, as in that instance, to be accompanied by a dislocation throwing 
 
158 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 Montmorenci the measures down to the south-eastward. This fault is traceable north- 
 easter ty fr m Beauport church, from which the road to Montmorenci runs 
 nearly the whole way on a bare ledge of Trenton limestone with a very 
 small dip ; while close on the south-eastern side of the road, the Utica shales 
 are in many places seen in a narrow strip, -tilted up at a high angle. The 
 details of the fault are well displayed at Montmorenci Falls. Here the chan- 
 nel of the river is cut down through the black limestone beds of the Trenton 
 formation to the gneiss of the anticlinal ridge, and the water at and below 
 the bridge flows down and across the gneiss, and leaps at one bound to the 
 foot of a precipice, which, immediately behind the water, is composed wholly 
 of this rock. 
 
 At the summit of the cascade, the Trenton beds on the west side have a 
 thickness of nearly fifty feet, marked by Leptcena sericea, Stropliomena 
 alternate Orthis testudinaria, Oonularia Trentonensis, and Calymene 
 
 120-123. BKYOZOA (TK.) 
 
 UQ.Ptilodictya recta (Hall) ; a, transverse section. 
 
 121. P. acuta (Hall). 
 
 122. Coscinium proavium (Eichwald), a fragment. 
 123. Intricaria? reticulata (Hall). 
 
 BlumeribacUi. The dip of these beds is down the stream, at a very small 
 angle ; but at tfre foot of the precipice, and in immediate contact with the 
 gneiss, about the same thickness of limestone is tilted up to an angle of fifty- 
 seven degrees. It is followed by a similar amount of black bituminous shale 
 with the same slope. In this attitude, the rocks climb up the face of the 
 precipice, presenting their edge to the chasm on each side. They are 
 followed by about eight feet of strong hard grey sandstone, weathering 
 brown, in beds of from ten to eighteen inches, interstratified with black 
 shales, to which succeed grey arenaceo-argillaceous shales, composing the 
 sides of the chasm out to the water of the St. Lawrence. The limestones 
 hold characteristic fossils of the Trenton, the black shales belong to the 
 Utica, and the grey shales to the Hudson River formation. 
 
CHAP. IX.] 
 
 TRENTON GROUP. 
 
 159 
 
 About half a mile beyond the bridge, the tilted limestones and black chateau 
 shales cross the road ; immediately on the north side of which, the gneiss 
 rises from beneath them, here showing the point around which the basset 
 edge of the limestone sweeps as it folds over the anticlinal axis. These 
 two formations keep close on the north side of the road for nearly a mile 
 and a half, when they suddenly become removed between one and two fur- 
 longs to the north-westward by a twist or dislocation. Proceeding beyond 
 this, they gradually increase in width, while the gneiss as gradually recedes 
 from the coast', until, becoming affected by the anticlinal of Chateau Richer, 
 they sweep round to the road. The upper part of the black shales comes 
 upon the road about half way between the churches of Ange Gardien and 
 Chateau Richer, and that of the limestone about three eighths of a mile 
 above the latter place. On the south-eastern side of the gneiss, which rises 
 
 124-129. BRACHIOPOD A (TR.) 
 
 124 
 
 126 
 
 124. Discina Pelopea (Billings). 127. Trematis terminalis (Emmons). 
 
 125. D. Circe. (Billings). 128. T. Montr ealensis. 
 
 126. Trematis filosa (Hall). 129. T. Ottawaensis (Billings). 
 
 130. T. Huronensis (Billings) ; a, lower valve ; 6, longitudinal section, 
 
 showing the curvature of both valves ; c, a portion of surface enlarged. 
 
 into a moderate hill, the Trenton limestone leans at a considerable angle, and 
 continues so until reaching the synclinal curve, where it comes upon the 
 Sault a la Puce River, and where the beds are found to be more arena- 
 ceous than usual. 
 
 On the south-eastern side of the anticlinal of Chateau Richer, the meas- Dislocation, 
 ures are broken by the effect of a fault, which again throws them down 
 on that side, bringing the Hudson River shales to abut against the gneiss. 
 At the cascade of the Sault a la Puce, the water is precipitated over the 
 gneiss rock with a fall of sixty feet ; and above the cascade for some short 
 distance this rock occupies the left bank of the river, while the arenaceo- 
 calcareous beds are seen on the right. At the foot of the cascade, the 
 
160 GEOLOGY OF CANADA. [CHAP. IX. 
 
 stream makes a sudden turn to the eastward ; and the rock on the right 
 bank, in face of the fall, appears to belong to the Hudson River shales, which 
 constitute both banks of the stream for the remainder of the distance to 
 the St. Lawrence. In the course of the fault to the north-eastward, these 
 shales continue in contact with the gneiss for two miles farther. A thin 
 strip of Trenton limestone is then interposed, and continues, with but little 
 augmentation in its breadth, all the way to the Riviere a la Rose. Both for- 
 mations maintain a high angle of inclination ; but they diminish in slope 
 and increase in width as they fold over the anticlinal of this vicinity ; again 
 however narrowing and becoming more precipitous as they proceed east- 
 ward on the south side of the axis. 
 
 ste. Anne. On the Ste. Anne, the limestone is seen leaning against the gneiss at the 
 foot of the lowest cascade. At the contact it has a southern dip of from 
 thirty to seventy degrees, and the breadth of the band does not exceed 
 twenty or thirty yards. Farther down the stream, the total thickness of 
 the Utica formation (to be hereafter described) is well displayed, with 
 measures belonging to the Hudson River formation beyond. Between the 
 river Ste. Anne and Cape Tourmente, both the Trenton and the Utica for- 
 mations are once more seen on the road from St. Joachim to Bay St. Paul, 
 where the road rises from the plain between the rivers Blondelle and 
 Marsolette. The limestone is seen for the last time in this neighbor- 
 hood where the Friponne descends from the gneiss. In both localities, the 
 limestone, dipping nearly south, rests on the gneiss at an angle of about 
 thirty degrees ; and at the Friponne the strata are abundantly stored with 
 fossils, such as Orthis testudinaria, Lingula curta, Discina filosa, Qonu- 
 laria Trentonensis, Qalymene Blumenbachii^ Trinucleus concentricus ; and 
 with them occurs Aoidaspis Horani. 
 
 Bay st. Paul. Descending the St. Lawrence to Bay St. Paul, which is about thirty 
 miles below Cape Tourmente, a great development of limestone is met with 
 on the east side at Cap aux Rets, between which and the gneiss running 
 out into Cap Rouge the cliff exposes a section nearly at right angles to the 
 strike of the strata. The general dip is westward, increasing irregularly 
 from sixteen to sixty degrees as it approaches the gneiss. Between the 
 limestone and the gneiss there is an interval of concealment of about fifty 
 yards, across the measures ; but independent of what may be in this, and 
 making allowance for one or two twists visible in the cliff, there is breadth 
 enough completely denuded to give a thickness approaching 600 feet, 
 the whole of which consists of dark grey and black bituminous limestone, 
 with the exception of a band of white sandstone within about thirty feet of 
 the bottom. The rock is fossiliferous, and among the remains are Grap- 
 tolithus amplexicaule, Leptoena sericea, Orthis testudinaria, Avicula Tren- 
 tonensis, Calymene Blumenbachii, Acidaspis Horani, and Trinucleus 
 concentricus. 
 
CHAP. IX.] 
 
 TRENTON GROUP. 
 
 161 
 
 On the west side of the bay. a portion of the same bituminous limestone Dislocation, 
 is met with at the mill on the Rividre au Moulin. The deposit is here seen 
 to dip eastward, and there is evidence to prove that it is brought into 
 place by a dislocation. The beds abut against the gneiss ; and at the 
 point of contact, the slope, which near the mill does not exhibit more than 
 from twenty to thirty degrees, is suddenly turned up at the cascade, on 
 one side of the stream to sixty, and on the other to ninety degrees, while in 
 one spot, the strata, conforming to the face of the cliff, even overhang the 
 
 131-138. BRACHIOPOD A (TK.) 
 
 133 
 
 f 
 
 1:34 
 
 131. Lingula quadrata (Eicbwald). 
 132. a, 6, L. Coburgensis (Billings). 
 133. L. Philomela (Billings). 
 134. L, Progne (Billings). 
 
 135. Lingula elongata (Hall). 
 136. a, b, L. Briseis (Billings), 
 137. L. obtusa (Hall). 
 138. L. curia (Conrad). 
 
 perpendicular. The direction of the junction of the two rocks is "N. 80 
 W. ; but following up the ravine above the edge of the cascade, in a direc- 
 tion nearly transverse to this, after passing over a few yards of gneiss, the 
 limestone again occurs, and continues present on one side of the ravine 
 while gneiss occupies the other for the space of nearly fifty yards, to the 
 second vertical leap in the fall. Here a face of gneiss presents itself, Mineral veins, 
 running N. 54 W. ; and on the north and south sides of the limestone thus 
 limited, mineral veins occur, holding small quantities of galena. The 
 gangue in which the ore is distributed is composed of calcspar, mingled 
 with apple-green fluor spar. The veins on the south side of the limestone are 
 
162 GEOLOGY OF CANADA. [CHAP. IX. 
 
 smaller than those on the north, but they are all probably connected with 
 one great line of disturbance. On the north side, there are two parallel veins 
 in the space of six feet, one of them being three feet wide, including a 
 fragment of gneiss which occupies half the breadth. In the valley of the 
 Gouffre, the bituminous limestone, which at the mouth of the river has a 
 breadth of two miles, has been traced up to St. Urbain, a distance of about 
 ten miles, reaching it without any apparent disruption of its continuity. It 
 is contracted however to a width of half a mile a little over half-way up, at 
 St. Croix and the river Remy, but it widens again to a mile before it 
 terminates above the church of St. Urbain. 
 
 Ebouiemens. Limestones present themselves again between three and four miles below 
 the Gouffre, entering upon the land a little above Les Eboulis. They extend 
 along the coast about fifteen miles, in a strip, of which the greatest breadth, 
 somewhat exceeding a mile, occurs between two small streams upwards of 
 a mile apart, one of them called the Ruisseau du Moulin and the other the 
 Ruisseau de 1'Eglise, in the seigniory of Les Ebouiemens. After an 
 interval of about five miles, the same rocks again come upon the coast, 
 along which they occupy a distance of about six miles, and run up the 
 valley of Murray Bay River. The strata at the base are seen in the 
 neighborhood of White Point, on the west side of the bay. They are 
 as a whole composed of calcareous sandstone, but the arenaceous layers are 
 interstratified with occasional bands of limestone. In one or two of the 
 arenaceous beds there are quartz pebbles as large as hen's eggs ; but in 
 general the grains range from the size of snipe shot to that of pigeon shot, 
 and are usually rounded, so as to give an oolitic aspect to the rock. They 
 consist sometimes of limestone and sometimes of quartz, the latter usually 
 prevailing to a considerable extent. The color of the rock is a dirty white. 
 On the east side of the bay, a coarse conglomerate fills up inequalities 
 in the surface of the Laurentian quartzite, and appears to be composed 
 of various moderately sized fragments, and even considerable boulders or 
 large angular blocks of the quartzite, held in various attitudes in a par- 
 tially calcareous cement. The best section on the east side of Murray 
 Bay is at .Les Ecorche's, where the lower part of the deposit consists of 
 calcareous sandstone, with a band or two of conglomerate holding pebbles as 
 large as pigeon's eggs, followed by grey and whitish layers which weather 
 to a yellowish-white, assuming a light drab when the stone is wet. These 
 are followed by a set of calcareo-arenaceous beds, which, though of a nearly 
 uniform light grey in fresh fracture, weather to a yellowish- white and a 
 reddish-white ; the two colors alternating with one another in the upper 
 part of the deposit. The total thickness of this part is about sixty feet. 
 The calcareous sandstones are followed by dark grey bituminous lime- 
 stones, which are highly fossiliferous, and these in some parts display a 
 considerable thickness, attaining perhaps nearly 200 feet. 
 
CHAP. IX.] TRENTON GROUP. 163 
 
 From these beds Dr. Dawson of McG-ill College has collected an in- 
 structive series of fossils. Among those from the calcareous sandstones 
 are Stenopora fibrosa, Receptaculites occidentalis, Tetradium fibratum, 
 Lingula Eva, (a new species), Ctenodonta nasuta, Pleurotomaria 
 staminea, P. allied to aperta, Bellerophon bilobatus, Illcenus Milleri, and 
 Leperditia Oanadenns. Among those from the dark grey limestones are 
 Stenopora fibrosa, Petraia corniculum, Crlyptocrinus ramulosus, Leptcena 
 sericea, Strophomena alternata, Orthis testudinaria, 0. pectinella, 0. 
 tricenaria, Oamerella Panderi, Ambonychia radiata (never before found so 
 low), Modiolopsis nasuta, BelleropJwn'Ulobatus^ Calymene Blumenbachii, 
 Bronteus lunatm, Illcenus Milleri, Trinucleus concentricus, Encrinurus 
 vigilans, and Asaphus platycephalus. From this it would appear that the 
 lower beds belong to the Birdseye and Black River, and the upper to 
 the Trenton formation. These deposits run for six miles up the valley of 
 Murray Bay River, and in this distance the breadth of six miles, which 
 they present on the coast, gradually diminishes to a mile and a half. At the 
 
 139-141. BKACHIOPODA (TR.) 
 
 140 
 
 141 
 
 139. Lept&na sericea (Sowerby) ; a, ventral valve ; 6, dorsal ; c, section. 
 140. Strophomena allernata (Conrad) ; a, ventral valve ; b. section. 
 141. S. deltoidea (Conrad). 
 
 bridge however, near the mouth of the river, an undulation brings to the 
 surface a narrow belt of gneiss, which, running in an easterly course, 
 approaches the coast beyond Le Heu. There appears to be another 
 parallel undulation below Les Ecorche's. 
 
 Proceeding along the road from the Murray Bay River, by the Ruisseau 
 des Frenes, there occurs beyond the extremity of the preceding spur, a 
 small patch of the limestone before reaching the Little Lake, and a large 
 one appears to extend from this lake to Nairne's Lake. The latter patch 
 is not over ten miles from the limestone of St. Urbain, and it is not impos- 
 sible that there may be others between the valleys of the Gouffre and 
 Murray Bay River, in the depression that runs from the one to the other. 
 The interval has however not yet been examined. 
 
 Between Murray Bay and the Mingan Islands, the series of rocks under 
 description is not yet recognised, and the only position that has been heard 
 of, as possibly presenting them, is at the entrance of the Bay of Seven 
 
164 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 Islands, where limestones are said to exist resembling those of Mingan, but 
 there has not yet been any opportunity of inspecting them. In the 
 southern part of Large Island of the Mingan group, the beds which have 
 been given as belonging to the Chazy formation are followed by about 
 thirty feet of yellowish-white pure limestone, some portions of which are 
 filled with -Maclurea Logani. The beds making up this mass are therefore 
 supposed to belong to the Birdseye and Black River formation. Before 
 however this is rendered certain, it would be necessary to obtain a larger 
 number of characteristic fossils from the locality, which is the only one in 
 which these strata have been observed among the Mingan islands. 
 
 142, 143. BKACHIOPODA (TK.) 
 
 142 
 
 142. Strophomena filitexta (Hall); a, ventral aspect; 6, dorsal aspect; 
 
 c, section of a slightly convex specimen ; d, interior of ventral valve. 
 143. Strophomena Thalia (Billings) ; a, ventral aspect; b, section. 
 
 On the Saguenay, at Lake St. John, which is nearly a degree west of 
 the longitude of Quebec, and somewhat less than two degrees of latitude 
 to the north of it, there is An outlying patch of Lower Silurian strata, to 
 which attention was first drawn by Captain, now Major General Baddeley, 
 R. E., in the year 1828. It probably underlies the whole lake, but 
 the strata belonging to it have as yet been observed only on the east and 
 west sides of it. The lower rocks of the series are limestones, and their 
 fossils indicate that they belong to the Birdseye and Black River and 
 Trenton formations. On the east side, the Trenton occupies a position on 
 a flat island about half a mile to the west of the Little Discharge. On the 
 west, the whole series of limestones extends in a belt from the Hudson's Bay 
 Company's post at the mouth of the Metabechouan to a position a little south 
 of Blue Point, a distance of about eighteen miles, whence it has been traced 
 only five miles farther, striking westward. The details of its distribution 
 
CHAP. IX.] 
 
 TRENTON GROUP. 
 
 165 
 
 beyond this have yet to be ascertained. The summit of the formation is 
 well defined by the presence of the Utica shales, and its thickness does not 
 appear to exceed a hundred feet. In the lower parts, there appears to be 
 an intermingling of the fossils of the Birdseye and Black River with 
 those of the Trenton. For example, about two miles west of the Metabe- 
 chouan River, in eight feet of brown compact bituminous limestone at 
 the base of the series, occur Stromatopora rugosa, Petraia profunda, 
 Receptaculitus occidentalis, and Orthoceras Bigsbyi, associated with 
 Leptcena sericea, Strophomena alternata, and Oalymene Blumenbachii. The 
 chief part of the limestones are of a yellowish-grey, and at the Ouiatchouan 
 in a three feet bed of this description at the base of the series, associated 
 with Stenoporafibrosa, Petraia prof undo,, Orthis lynx, Murchisonia gradlis, 
 M. bettieincta, and Trochonema umbilicata, there was met with Halysites 
 catenulatus, in no other place found so low on the American continent. 
 
 144-147. BBACHIOPODA (TB.) 
 
 146 
 
 144. a, b, c, Orthis testudinaria (Dalman). 
 
 145. a, b, a, b. 0. plicalella (Conrad), different views of two specimens. 
 
 146. a, 6, 0. subquadrata (Hall). 
 
 147. a, b, c, O. pectinella (Conrad). 
 
 In the trough between the Ottawa and the St. Lawrence Rivers, the Birds- Ottawa, 
 eye and Black River formation follows the contour which has been given to 
 the Chazy, and the Trenton probably fills up the centre of the southern of 
 the two subordinate synclinals into which the general trough is divided by 
 the Rigaud anticlinal, while in the northern it is overlaid by three isolated 
 patches of the succeeding Utica shales. The principal one of these is in the 
 vicinity of Ottawa city, and comes to within from a quarter to half a mile 
 of the Ottawa River, near the mouth of its tributary the Rideau ; leaving 
 but a narrow space for the Trenton limestone. The upper part of this, east 
 of the Rideau, appears to be buried by an east and west fault, which comes 
 upon the main stream about half a mile below the tributary, and shows a 
 downthrow to the south. The limestones are affected by two parallel dis- 
 
166 GEOLOGY OF CANADA. [CHAP. IX. 
 
 Dislocations, locations between 500 and 600 yards apart, west of the Bideau. One of 
 them, coming to the Ottawa a little below the exit of the canal, is a small 
 upthrow to the south, and the other, about 600 yards above it, beyond Bar- 
 rack Hill, is a downthrow of seventy feet in the same direction. Far- 
 ther west, the series of limestones which we are tracing comes up against 
 the Gloucester and Hull fault, with a breadth of probably seven or eight 
 miles, extending from the vicinity of the west side of the junction gore of 
 Gloucester, across the Ottawa, to the front of the sixth lot of the fifth range 
 of Hull. This fault being with an upthrow to the west, the limestones 
 show a less width on that side of the fault ; and as already indicated in 
 speaking of the Chazy, they present two areas, one on each side of the 
 Ottawa, between which there is probably an undulation bringing up the 
 lower measures seen on the river. 
 
 In consequence of these disturbances, it is difficult to measure correctly 
 the thickness of the series in this neighborhood. In the Barrack Hill 
 there is visible an uninterrupted succession of beds, hi all making 1ST feet 
 of thickness ; and on the south side of the downthrow fault occurring above 
 the hill, the beds continue to accumulate at a pretty regular rate for 
 nearly a mile across the measures, and probably to the Little Chaudiere 
 upthrow, which would be half a mile more. If an inclination of no more 
 than three degrees be given to these strata, the thickness resulting, com- 
 bined with that of the beds in Barrack Hill, after deducting the seventy 
 feet repeated by the Barrack Hill fault, would be upwards of 500 feet. 
 Approaching the Little Chaudiere fault, however, the inclination appears 
 to increase, while a part of the Trenton is buried in the fault, and it is 
 therefore probable that the total volume of these limestones at Ottawa 
 will not fall short of the 600 feet given. to them at Montreal. 
 
 Between the base of the Utica formation and the beds of the Barrack 
 Hill there appear to be a few bands of smooth even-bedded compact black 
 limestone ; while the strata of the hill, for about 150 feet down, are of a 
 nodular character, having the beds usually parted by black bituminous 
 shale. The lower part of the section, for about twenty feet, consists of 
 strong bands highly charged with chert, underlaid by beds crowded with 
 broken stems of encrinites, many of which are of large size and sometimes 
 in a good state of preservation. The layers between the nodular and 
 chert beds are thin, and are enriched with a great variety of crinoids, 
 star-fishes, and cystideans, of which the bodies and stems are sometimes 
 Fossils of nearly whole. These beds have greatly extended our knowledge of these 
 Ottawa. f am ^ es i n the Lower Silurian series, and among other remarkable forms 
 there have been obtained from them Pleurocystites squamosus, P. robustus, 
 P. filitextus, P. elegans, G-typtocystites multiporus, Comarocystites punc- 
 tatus, Amygdalocystites radiatus, Grlyptocrinus marginatus, Cr. ornatus, 
 Hybocrinus conicus, H. tumidus, Carabocrinus radiatus, Porocrinus coni- 
 
CHAP. IX.] 
 
 TRENTON GROUP. 
 
 167 
 
 cus, Dendroerinus gregarius, D. rusticus, Palceocrinus angulatus, Oleio- 
 crinus regius, Lecanocrinus elegans, Rhodocrinus pyriformis, Retiocrinus 
 fimbriatus, Agelacrinites Dicksoni, Edrioaster Bigsbyi, Stenasterpulchellus, 
 Petraster rigidus, and Palasterina stellata. These fossils are figured in 
 Decades III. and IV. of the Survey. In the same beds is obtained 
 Bronteus lunatus, the only species of this genus yet known in the Lower 
 Silurian series of America. 
 
 On the downthrow side of the Barrack Hill fault, and somewhat higher 
 on the river, grey yellow-weathering bituminous limestones occur, which 
 are lower in the series than those of the Barrack Hill cliff. They contain 
 numerous fossils, among which are Strophomena alternata, Rhynchonella 
 increbescens, Murchisonia gracilis^M. bellicincta, M. bicincta, Pleurotomaria 
 Americana, Ophileta Ottawaense, Uunema strigillata, Bellerophon disculus, 
 Helicotoma planulata^ Trochonema umbilicata, Ctenodonta nasuta, Ma- 
 
 148-151. BRA CHIOPOD A (TR.) 
 
 148. a, 6, c, Orthis borealis <Billings). 
 
 149. O. lynx (Eichwald) ; a, specimen with cardinal angles rounded ; 
 
 6, the more common form. 
 
 150. a, 6, 0. insculpta (Hall). 
 
 151. a, 6, O. tricenaria (Conrad). 
 
 theria brevis, M. obtusa, Orthoceras Ottawaense, and Phacops calliceplialus. 
 The fossils being replaced by sparry dolomite, which is less soluble in water 
 than the carbonate of lime in which they are imbedded, weather into relief 
 and, becoming brown from the presence of carbonate of iron, which is con- 
 verted into the peroxyd, are strongly contrasted with the rock. 
 
 Descending the valley of the Ottawa, the sandstone of the Chazy gener- Escarpments, 
 ally presents a distinct escarpment. The overlying limestone of the same 
 formation sometimes occurs in the same escarpment as the Birdseye and 
 Black River, but occasionally by itself, while the Trenton, with its lower 
 part sometimes in the same escarpment with this formation, often pre- 
 sents, at some distance back, another escarpment composed of higher por- 
 
168 GEOLOGY OF CANADA. [CHAP. IX. 
 
 tions of the formation. On the south-east side of Green's Creek three 
 Gloucester, escarpments appear. The first, which has a height of forty feet, presents 
 the Chazy sandstone ; the second, which is thirty feet, shows the Chazy 
 limestone ; and the third, of forty-eight feet, the Birdseye and Black 
 River. The last of these is removed from the Ottawa about a mile, being 
 on the line between the first and second ranges of East Gloucester, where 
 it is traceable along the strike for about a mile and a half. The formation 
 again appears in an escarpment on the second lot of the first range, but 
 is here not more than the third of a mile from the margin of the river, and 
 forms a point, from which it runs eastward on the one hand and south- 
 ward on the other. These two escarpments are on the opposite sides of 
 Anticlinal, the Templeton and East Gloucester anticlinal. It is not certain how far 
 they would run before meeting on the axis of the anticlinal, but it would 
 probably be somewhere in the east end of the third range of the township. 
 
 152-154. BRACHIOPOD A (TR.) 
 
 152. Rhynchonella recurvirostra (Hall). 
 
 153. a, 5, c, R. increbescens (Hall). 
 
 154. a, 6, c, Camerella hemiplicata (Hall). 
 
 The lower part of the Trenton does not appear to display any corre- 
 sponding escarpments succeeding these. But about five miles and a half 
 from the Ottawa, on the south side of the anticlinal, an escarpment of the 
 upper part of the formation, varying from thirty to ninety feet, crosses the 
 road between the eighth and ninth ranges of Cumberland, on the seventh 
 lot. This is traceable in a pretty straight line for between seven and eight 
 miles, to the line between Cumberland and Clarence, on the thirteenth lot, 
 upwards of six miles from the Ottawa. Here it makes a sudden turn to the 
 southward, and has been traced in this direction for about a mile. From 
 200 to 400 yards southward from the edge of this escarpment, the black 
 shale of the Utica formation can be traced the whole way, presenting a 
 very small dip to the southward until coming to the turn. A mile east- 
 ward of the turn a lower escarpment occurs, with another still lower, a mile 
 beyond; both run north-westward for upwards of a mile, and present a 
 small dip to the southward of west, indicating the crown of the anticlinal 
 
CHAP. IX.] TRENTON GROUP. 169 
 
 arch. The thickness in the three escarpments would probably be about a 
 hundred and fifty feet. 
 
 A great swamp extends nearly across Cumberland on the crown of the Cumberland, 
 anticlinal ; but on the north side of the anticlinal, limestones, which corre- 
 spond with those of the uppermost of the escarpments, form a point on the 
 third lot of the sixth range of Cumberland, about three and a half miles 
 from the Ottawa. They present a considerable area of bare rock, and up- 
 wards of a mile to the eastward are divided by a point of black shale. The 
 limestones on the south side of the shale soon become covered up, in their 
 progress eastward ; but those on the north present an escarpment of about 
 forty feet, facing the north, which is traceable for a couple of miles to the 
 road from the Ottawa to Dunning's mills, where the road runs through the 
 fourth range of Cumberland. On this road the escarpment is on the 
 second lot ; the outcrop of the black shales is about 650 yards southward 
 from it on the third, where they form part of the smallest of the three 
 patches of the Utica formation already mentioned, this smallest one being 
 separated from the largest by the limestones on the Clarence and Cumber- 
 land anticlinal. 
 
 Between the black shales and the Ottawa, the road which has been Thickness. 
 mentioned runs very nearly at right angles across the measures, and the 
 breadth on it of the Trenton formation, with the Birdseye and Black 
 River, is just about 5000 yards. The dip, which is from the Ottawa, does 
 not, on the average, exceed one and a half or two degrees, while there is a 
 difference in level of about a hundred feet between the summit and the 
 base. The total volume of the series would thus be between 650 and 
 700 feet, which accords very well with the supposed thickness both at 
 Montreal and Ottawa. 
 
 About two miles southward from McCauPs wharf in Clarence, the Chazy ciarence. 
 presents an escarpment of fifty feet, the base of which is occupied by the 
 sandstone of the formation, and a short distance from this step there rises 
 up another, the height of which is about a hundred feet. The lower part 
 of it is occupied by the Birdseye and Black River formation, and the upper 
 by a portion of the Trenton. This escarpment is on the south-west side of 
 the Buckingham and Clarence anticlinal, and is well marked for at least 
 two miles to the south-east. It is not yet ascertained how far the Birdseye 
 and Black River formation is carried in this direction before meeting the 
 dislocation which is connected with this anticlinal ; but however far it may 
 be, this formation is thrown northward again, beyond McCaul's mills, by the 
 fault, the rock at the mills being Trenton. 
 
 Freed from the effects of this fault, the same series presents itself in 
 another escarpment, which, from a position about a mile west of McCaul's 
 mills, runs in a nearly straight line .to the tenth lot of the fifth range of 
 Plantagenet, the distance being about eleven miles, and the bearing about 
 
170 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 piantagenet. five or six degrees south of west. The escarpment for some distance is 
 about a mile from the Ottawa ; but opposite the mouth of the South Petite 
 Nation it is nearly two miles. It runs up the valley of the river, and 
 gradually approaches to within less than a mile of the stream. On a road 
 which runs between the thirteenth and fourteenth lots of the third range 
 of Piantagenet, the outcrop of the Utica shales is met with about 300 
 yards south of the edge of the escarpment. They here constitute a part of 
 the rim of the third isolated patch of those shales, already mentioned. 
 This area of shales is no doubt separated from the second by the effect of 
 the Buckingham and Clarence anticlinal, but its breadth is somewhat 
 uncertain. Fragments of shale, however, on the sixteenth lot of the sixth 
 range of Piantagenet, show that it will probably attain at least three miles. 
 
 155, 156. LAMELLIBRANCHIATA (TK.) 
 
 Cambridge. 
 
 155 
 
 155. Amcula, elliptica (Hall). 
 156. A. Hermione (Billings). 
 
 / 
 
 Where the escarpment on the left side of the South Petite Nation reaches 
 the fifth range of Piantagenet, it takes a turn to the south-eastward, and 
 can be followed for nearly two miles in that direction. As the upper part 
 of the Trenton would here be nearly half-way across the space between 
 the anticlinals to the north-east and the south-west, it is probable that in its 
 farther progress it will turn farther round and thus limit the Utica shales 
 on the east. 
 
 At the High Falls on the South Petite Nation, in the twelfth lot of 
 the sixth range of Cambridge, the river runs northward on the face of a 
 single bed of Trenton limestone for about 300 yards, descending about 
 twenty feet. The position and dip of this rock make it probable that it 
 is on the north side of the main Rigaud anticlinal. The want of exposures 
 in the stream for a considerable distance below the High Falls renders it 
 
CHAP. IX.] TRENTON GROUP. 171 
 
 uncertain where the axis of the Templeton and Gloucester, and that of the Anticiinais. 
 Buckingham and Cumberland anticlinal would strike the stream. It is 
 conjectured however that the former would cross it near the mouth of 
 Cobb's creek, in the twenty-third lot of the twelfth range of Plantagenet, 
 and the latter not far from the elbow in the stream, near the south-east 
 corner of Plantagenet. The Lochaber and Plantagenet axis would appa- 
 rently run up the valley not far from the stream, nearly to Hatville, which 
 is six miles from the mouth, beyond which it would probably keep rather 
 to the north-east side of it. There are exposures both at Hatville and a 
 mile and a half farther up, and the strata in both places belong to the Tren- . 
 ton. Their dip appears to indicate that they are on the south-west side of 
 the axis, and it is probable that the base of the formation would fold over 
 it farther down the valley. 
 
 About two miles from the mouth of the South Petite Nation, the Birdseye 
 and Black River formation crosses the stream, dipping southward at an 
 angle of four degrees. Trenton beds are seen resting on it, and they under- 
 lie the road up the valley for more than a mile, in which they appear to be 
 quite horizontal. These rocks are seen in the same relation on the east 
 side of the township, in an escarpment below the road, crossing the line 
 between Plantagenet and Alfred, about two miles from the Ottawa. 
 The escarpment and the road keep in the same relation for two miles and 
 a half farther to the south-eastward, up the valley of the brook flowing into 
 George Lake ; but three miles farther east, on the second range of Alfred, 
 the escarpment is south of the road, and on the summit there occurs a bare 
 triangular surface of Trenton limestone, of a mile and a half long. In the 
 township of L'Orignal, the escarpment approaches nearer the Ottawa, being 
 about a mile from it on the west side, and a mile and a half on the road 
 which runs back from the village. In the rear of Hamiltonville in West 
 Hawkesbury, it is two and a half miles from the margin. Its position in Hawkesbury. 
 East Hawkesbury is not so well ascertained ; but the base of the series 
 very probably reaches the boundary between the western and eastern divi- 
 sions of the province, in sweeping round the extremity of the trough north 
 of the Rigaud anticlinal. On the south side of the trough, limestone beds 
 are met with at McDonald's mills, on the Riviere a la Graisse, in the 
 fifteenth lot of the seventh range of East Hawkesbury. These are at the 
 base of the Trenton ; and very nearly in the strike of these beds, there is 
 an exposure of Trenton limestone in the thirty-second lot of the ninth 
 range of Lochiel. 
 
 In the southern division of the general trough between the Ottawa and 
 the St. Lawrence, it is computed that the Birdseye, Black River, and Tren- 
 ton formations spread over an area of about 600 square miles, the Trenton 
 occupying the chief part ; but the area is so much covered over with drift 
 that its perimeter has not yet been ascertained. Following the exposures 
 
172 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 Lochiel. 
 
 Cornwall. 
 
 nearest the supposed base of the series, we have black Trenton limestone 
 on the thirteenth lot of the first range of Lochiel, on the Riviere de 1'Isle, 
 and good grey granular beds of the same formation, fit for building stone, 
 at and near Alexandria, on the river Garry, on the thirty-seventh and 
 thirty-eighth lots of the second range of Lochiel, as well as farther up on 
 the stream, on the fourth and sixth lots of the second range of Kenyon. 
 The Birdseye and Black Kiver limestones, with Columnaria alveolata, are 
 exposed on the river Beaudette, in the twenty-ninth lot of the seventh 
 range of Lancaster, and Trenton on the twenty-second lot of the second 
 range of Charlottenburgh, where a bed of fifteen inches yields a good 
 building stone. The thick black beds of the Birdseye and Black River 
 
 157. LAMELLIBKANCHIATA (TR.) 
 
 157. Modiolopsis Gesneri (Billings) ; a, side view ; b, dorsal view. 
 
 formation on the sixth and twenty-fourth lots of the fourth range of Corn- 
 wall, have already been alluded to. In the former of these two localities 
 Columnaria alveolata is a common fossil, and many of the specimens ob- 
 tained present the peculiarity of having the cells of the coral lined with 
 transparent crystals of quartz, and filled with a brilliant black carbona- 
 ceous matter, looking like coal. Leptcena sericea, Strophomena alternate) 
 and Orthis testudinaria occur in the other locality, and the beds may 
 therefore belong in part to the Trenton. The massiveness of some of the 
 beds makes them resemble those of the previous locality, and among the 
 fossils there is a large Orthoceras (0. magniventrum^) the chambers of 
 which hold mineral carbon. A siphuncle of one of these, on being slit open> 
 was found to contain 0. Bigstyi. Both of these are Black River species, 
 and it is therefore probable that we have here the junction of the Black 
 River and Trenton. Farther westward, on the twenty-sixth lot of the 
 fifth range of Osnabruck, black Trenton beds show Stenopora petropolir 
 
CHAP. IX.] TRENTON GROUP. 173 
 
 tana., Leptcena sericea, tStrophomena altemata, Orthis testudinaria, Lin- 
 gula like L. quadrata, L. elongata, and Avicula elliptica. 
 
 Sixteen miles farther in the same direction, black limestone occurs in the 
 northwest corner of Williamsburgh, about a mile from the right bank of the 
 South Petite Nation River. Being the most westerly exposure of black 
 limestone met with, connected with the southern division of the Ottawa and 
 St. Lawrence trough, it is probable that it may belong to the Birds- 
 eye and Black River formation. There is nothing to contradict this view 
 in the aspect of the rock, but no fossils have been obtained to confirm it. 
 Farther down the river, at the eleventh lot of the second range of Win- Winchester. 
 Chester, similar beds hold Leperditia; but here also the formation is 
 uncertain. Still farther down, at Armstrong's mills, on the twelfth lot of 
 the fourth range, and in several places in the neighborhood, quarries are 
 opened in black limestone beds, but there they are characterized by Tren- 
 ton fossils. From this vicinity, similar limestones occur at intervals all the 
 way to Crysler's mills in Finch, and nearly the whole of the township 
 
 158, 159. LAMELLIBRANCHIATA (TB.) 
 158" 
 
 158. Modiolopsis Meyeri (Billings). 
 159. Modiolopsis carinata (Conrad). 
 
 appears to be underlaid by such strata in a generally horizontal attitude. 
 At Crysler's mills, on the twelfth lot of the tenth range of the township, a 
 section shows alternations of grey or bluish and black limestones, dipping 
 N. 40 E. at an inclination of a little over forty feet in a mile. Lumps of 
 iron pyrites occur in the beds, and the strata are intersected by a set of 
 small parallel veins of calcspar, running about N. W. and S. E. 
 
 Westward of the High Falls, at Cook's mills on the Castor, in the eighth Russell, 
 lot of the ninth range of Russell, which would be in the strike of the 
 strata at the High Falls, already alluded to, there is a section of about five 
 feet, consisting of dark blue limestone alternating with black shale. Several 
 of the shale beds are very fossiliferous, and the shells in most abundance 
 are Leptcena sericea and Orthis testudinaria. On the south bank of the 
 Castor, in the next range to the west, thick beds of dark blue limestone 
 dip N. 40 W. < 32 ; and farther west, at Louck's mills, on the eleventh 
 lot of the fourth range, the dip, which, on the south side of the stream, is 
 S. 34 W., at an inclination varying, in the distance of a hundred yards, 
 
174 GEOLOGY OF CANADA. [CHAP. IX. 
 
 from sixty to five degrees, is on the north side N. 40 W. < 17. 
 While the north bank is occupied by thick bluish beds of granular lime- 
 stone, the section on the south is as follows, in descending order : 
 
 Ft. in. 
 
 Black shale supplied in abundance with a coral, of which the specimens have been 
 lost ; the upper part holds large concentric concretionary nodules of fine 
 grained black limestone, passing in parts into a bed of black limestone 
 
 eight inches thick, 3 6 
 
 Bluish-black limestone holding Leperditia Louckiana in abundance, some of the 
 
 specimens a quarter of an inch long, 1 10 
 
 Black bituminous limestone in a strong bed somewhat nodular in structure, .... 3 
 
 Black shale, 4 
 
 Bluish-black limestone, with imperfect divisions of black shale, 1 6 
 
 Dark bluish-grey limestone weathering black, with divisions of calcareous shale 
 
 holding imperfect fossils, 2 4 
 
 12 6 
 
 These exposures on the Castor, which are in a nearly straight line from 
 the High Falls, and in the direct continued bearing of the Rigaud and 
 Fitzroy anticlinal, are shown by the irregularity of the dips to be probably 
 affected by it. Two of them no doubt belong to the Trenton formation ; 
 but it is uncertain whether that at Louck's mill is to be placed immediately 
 beneath the Trenton or at its summit. The thickness of the black shale 
 associated with the limestone, and the fact that superior black shales occur 
 not far to the north of the anticlinal, would seem to countenance the latter 
 supposition, but at the same time the supposed position of the Chazy is not 
 far removed to the west. To perplex the question still farther, a dislocation 
 seems to be connected with the anticlinal near the spot, and it is not 
 certain on which side of the black limestone it may run. 
 
 Dislocation. This dislocation, as has already been stated, appears to be a downthrow to 
 the north-eastward, and to continue so to the vicinity of the south-east corner 
 of West Gloucester. It here splits into two branches, and while that which 
 runs into Hull continues a downthrow on the same side as before, the other, 
 running to Fitzroy, becomes a downthrow to the south-west side. Hence, 
 as was stated in speaking of the Chazy formation, an escarpment on the 
 twenty-second lot of the fifth range of Nepean shows this formation, with 
 the Birdseye and , Black River above it, and the Trenton following, on 
 the southward side of the fault. All these dip at a small angle towards the 
 Potsdam on the north, and each in its turn comes up against the Potsdam 
 a little to the eastward. From this position the Trenton continues along 
 the fault, first in contact with the Potsdam and then with the gneiss, until 
 reaching the neighborhood of the boundary between the townships of 
 Huntley and Fitzroy, where the line between the eighth and ninth ranges 
 of these townships intersects it. In this vicinity, the Birdseye and Black 
 River formation, and then the Chazy, again meet with the fault. 
 
CHAP. IX.] TRENTON GROUP. 175 
 
 Starting from the fault, the series of limestones more particularly under 
 description stretches across Huntley into Fitzroy , in a trough-like form, and 
 then crosses the southern part of Fitzroy into Pakenham, returning again 
 by the north-east corner of Ramsay into the west part of Huntley, modified 
 in the perimeter by the effect of several anticlinal and synclinal forms, 
 which have been explained in giving the distribution of the Chazy. The 
 Trenton formation appears to be confined to the two outside synclinals, 
 while the Birdseye and Black River forms a vinculum between them. 
 The latter appears to form an isolated patch on the Chazy, in the neigh- Pakenham. 
 borhood of Dickson's mills in Pakenham ; where, as has already been 
 stated, it is brought, by a dislocation, against the Calciferous, on the 
 south side. Near the mills, the Birdseye and Black River formation 
 yields very large masses of Columnaria alveolata, and some of its beds 
 abound with great orthoceratites, the chambers of which have occasion- 
 ally been found by Mr. Dickson to hold large quantities of petroleum. 
 
 160-164. LAMELLIBRANCHIATA (TR.). 
 
 b a 162 b 
 
 b 
 160. Ctenodonta contracta (Salter) ; a, interior, and b, exterior of right 
 
 valve. 
 161. Ctenodonta abrupta (Billings) ; a, dorsal view; 6, side view. 
 
 162. C. levata (Hall) ; a, side view ; b, dorsal view. 
 
 163. C. dubia (Hall) ; a, side view ; b, dorsal view. 
 
 164. C. astartceformis (Salter) ; a, dorsal view ; 6, side view. 
 
 This oil is probably derived from animal remains, and by its alteration 
 may account for the presence of the mineral carbon in the orthoceratites 
 and corals near Cornwall. Among the orthoceratites at Dickson's mills, 
 Orthoceras Bigstyi ranges from nine to eighteen inches in length, and 
 0. fusiforme is met with two feet long. 
 
 On the Silurian outlier of the Lac des Chats, the Birdseye and Black outliers, 
 River formation rests on the Chazy in two patches, and constitutes the high- Bomiechere - 
 est rock. On each of the three outliers of the Bonnechere, the Birdseye 
 and Black River follows the rim of the Chazy, and beds of the Trenton 
 formation rest upon it at Jessop's Rapids, on the farthest up outlier, 
 but none were met with on the other two. In the Birdseye and Black 
 River limestone of the second outlier, there is, at the Fourth Chute of the 
 
176 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 Allumettes. 
 
 New York. 
 
 Bonnechre, a remarkable subterranean channel, where a portion of the 
 water turns abruptly off at right angles to the general course, running 
 northerly, for about ten chains, through a great cavern. This cavern is 
 naturally nearly dry, excepting during freshets, but has been turned 
 to advantage by throwing a dam across the main body of the river near 
 the middle of the fall. This turns through a sufficient quantity of water 
 to convert the channel into a mill race, and the fall at the lower end of 
 the channel is applied to drive the wheel of the mill. 
 
 The Birdseye and Black River formation rests in two patches on each of 
 the two outliers between the Bonnechdre and Lake Allumettes, and no 
 Trenton beds succeed. In the Allumettes outlier, however, it forms only 
 one patch, which covers the chief part of Allumettes Island, and, crossing 
 the Ottawa at Paquette's Rapids, extends into Westmeath. Although it 
 is not supposed that any true Trenton beds cap the strata of this outlier, 
 
 165-167. LAMELLIBRANCHIATA (TR.) 
 
 165. Ctenodonta gibbosa (Hall). 
 
 166. C. nasuta (Hall) ; a, side view ; 6, dorsal view. 
 
 16 "7. Lyrodesma post striata (Emmons) ; a, exterior, and 6, interior. 
 
 there is here a commingling of Birdseye, Black River, and Trenton spe- 
 cies among the fossils, which has not been observed so conspicuously 
 elsewhere. At Paquette's Rapids, the fossils are most beautifully pre- 
 served, being replaced by silica, in a nearly pure calcareous matrix, and 
 weathered out into high relief. The species are numerous and in great 
 abundance, and the locality has afforded a rich collection. The best 
 specimens however are obtained in the bed of the river, so that it is only 
 when this is partially dry, in times of very low water, that they can be 
 easily procured. 
 
 From the province line, where it crosses Lake Champlain in Eastern 
 Canada, the Birdseye, and Black River, and Trenton formations, striking 
 through the valley of this lake and the valleys of the Mohawk and Black 
 Rivers, reach the waters of the St. Lawrence, and cross over into Western 
 Canada. On the United States side of the St. Lawrence, they 
 occupy a breadth extending from the Thousand Islands to Sandy Creek, 
 
CHAP. IX.] TRENTON GROUP. 177 
 
 and on the Canadian side, from the neighborhood of Kingston to the out- 
 side of the Prince Edward peninsula. 
 
 It has already been stated that between the Potsdam formation and the 
 strata characterized by the fossils of the Birdseye and Black River forma- 
 tion, to the westward of the Laurentian ridge of the Thousand Islands, there 
 are about eighty feet of strata, the age of which is not very clear. These Lower es- 
 appear in two succeeding escarpments, and are traceable for a consider- C8 
 able distance. At Vanluvin's mills, in Storrington, where they rest on stomngton. 
 intrusive flesh-red granite, the sequence in ascending order is as follows : 
 
 Ft. in. 
 
 Green shaly conglomerate ; the pebbles are chiefly of white quartz, and generally 
 rounded, the largest being about the size of a walnut ; they lie in a green 
 
 calcareo-arenaceous shale as a paste, 6 
 
 Green shaly conglomerate of the same materials ; the conglomerate, however, is 
 finer, and contains some angular fragments of quartz about two inches long j 
 a reddish tinge pervades some parts, and divisional planes of nearly a grass- 
 green color occur, 2 
 
 Greenish calcareous sandstone, with small rounded grains or pebbles of white 
 
 quartz, , 1 
 
 Measures concealed by drift, 20 
 
 Dark brownish-black fine grained compact bituminous limestone, with a some- 
 what nodular surface where exposed to the action of the atmosphere, and 
 slaty .towards the top. Organic remains are seen on the upper surface, 
 consisting of Tetradium fibratum, Strophomena like a small S.filitexta, Pleu- 
 rotomaria pauper, P. like P. Americana, Leperditia CanadensiSj and Bathyu- 
 
 rus Angelini, 5 
 
 Brownish-black compact bituminous limestone, with small crystals of calcspar 
 
 disseminated,.' 2 6 
 
 Measures concealed, 5 
 
 Grey slightly arenaceous limestone, 3 
 
 Grey compact limestone ; a good building stone, 10 
 
 Dark brownish-grey bituminous limestone with the same Strophomena as before, 
 and other fossils. The beds make good building stone, and yield good 
 
 lime of a darkish color, 11 
 
 Dark grey thin-bedded bituminous limestone, with large fucoids on the upper 
 
 surface, 3 
 
 Pale bluish-grey very compact bituminous limestone, 9 
 
 Dark brownish-grey bituminous limestone, with fragmentary fossils, chiefly of 
 the same Strophomena as before, and large fucoids on the upper surface. 
 
 Minute crystals of calcspar are disseminated through the bed, 1 
 
 Dark- grey compact limestone, with one division of calcareous shale ; the beds 
 
 hold many specks of iron pyrites, 2 9 
 
 Grey brown- weathering shaly limestone, 3 
 
 Pale grey limestone, 1 1 
 
 Bluish-grey calcareous shale, weathering to a rusty-brown color, 9 
 
 Brownish-black bituminous limestone, with small translucent crystals of calc- 
 spar, 1 6 
 
 Black shaly limestone, approaching to a shale, 2 
 
 Dark grey or blackish brittle thin bedded limestone, with a splintery fracture, . . 18 
 Dark grey or blackish brittle limestone of a fine texture, with a conchoidal frac- 
 ture, 1- 
 
 M 
 
178 GEOLOGY OF CANADA. [CHAP. IX. 
 
 Ft. in. 
 Measures concealed, 30 
 
 Dark brownish-grey bituminous limestone, having a conchoidal fracture ; the 
 exposed surfaces and edges are peculiarly marked with sharp deep angular 
 cavities, supposed to have held lenticular crystals of calcspar, 8 
 
 81 8 
 
 Kingston. These two escarpments, sometimes running into one, appear to come 
 round from the lake shore near Kingston, and at Kingston Mills an ex- 
 posure of twelve feet in thickness, of much the same character as the 
 lower portion of the strata, is seen resting on gneiss, in the excavation made 
 for the Grand Trunk Railway. In this, a fossil occurs, somewhat re- 
 sembling the siphuncle of Piloceras Canadense, but it may be a fragment 
 of the internal cast of the siphuncle of an Orthoceras. The former would 
 seem to ally the deposit with the Calciferous formation, but a single 
 fossil is too slight an evidence to fix its age. Leper ditia Oanadensis 
 ranges from the Chazy into the Birdseye and Black River, but the 
 presence of Pleurotomaria pauper and Bathyurus Angelini in the upper 
 
 168-170. GASTEROPODA (TB.) 
 
 168 *5*E-J-m-v*-<m ! r ^ i ..!.... 170 
 
 168. Cyclonema Halliana (Salter). 
 
 169. -C. Hageri (Billings). 
 
 170. C. Montrealensis (Billings). 
 
 portion might lead us to refer this to the Chazy, notwithstanding the 
 occurrence of Tetradium fibratum, which has not hitherto, in other places, 
 been found lower than the Birdseye and Black River formation ; unless 
 indeed some of the perforations taken for Scolithus in the Potsdam be not 
 rather impressions of that fossil. 
 
 Going westward from Vanluvin's mills, these rocks keep on the south 
 side of Loughborough Lake. The lower portion comes out to the shore, and 
 
CHAP. IX.] TRENTON GROUP. 179 
 
 is seen resting on the Potsdam sandstone at Knapp's Point. The upper 
 and more calcareous portion forms a sharp escarpment at no great distance lough ' 
 south from the other, and is traceable to a bay on the twenty-sixth lot of 
 the sixth range of Loughborough. Here the Laurentian gneiss appears, 
 and runs back to a small sheet of water called Round Lake, situated on 
 the town line between Storrington and Loughborough ; but on the west 
 side of this bay, the two escarpments again rise over the gneiss, and con- 
 tinue to run nearly parallel with the lake, at a distance south of it from 
 200 to 300 yards, to the eighteenth or nineteenth lot of the fourth range 
 of Loughborough. From the north side of the lake, the continuation of the 
 escarpments is traceable to the south-east end of Sloat's Lake ; and at the 
 base of the cliff, on this lake, a calcareous conglomerate occurs, resting on 
 flesh-red gneiss. The pebbles of the conglomerate are chiefly of gneiss, of 
 the same character as the rock it rests upon, with some of white quartz, 
 imbedded in a matrix of green and reddish calcareo-arenaceous shale. A 
 conglomerate of a somewhat brecciated character is observable in many 
 other parts, coming out from below the limestone ; its pebbles being 
 evidently derived from the Laurentian rocks, with which it is frequently 
 found in contact. 
 
 The escarpments are traceable to the head of Knowlton Lake, and there, 
 running nearer to one another, again rest on the Potsdam formation. As 
 already stated, the Potsdam appears to cease altogether near the foot of 
 this lake ; but the two succeeding deposits continue in separate escarp- 
 ments, by Pond Lily Lake and Mud Lake, to Centre ville in Amden, where 
 the upper one is marked by Leperditia Canadensis. From this, they turn Tamworth. 
 up northward, by Tamworth and Beaver Lake, to Clare River, shewing, in 
 a three-feet calcareo-arenaceous bed in the lower portion, in the neighbor- 
 hood of Tamworth, forms imperfectly resembling Scolithus, and in the 
 upper, not far from Beaver Lake, the same Leperditia as before, in some 
 abundance. Where the line between the third and fourth ranges of Shef- 
 field comes upon Clare River, there occurs the greatest thickness of the 
 beds observed in one mass in this part. It presents a cliff of about forty 
 feet, the upper part of which holds Leperditia in compact brownish-grey 
 limestone ; while on the same bank of the river, within seventy yards, the 
 rock is gneiss. 
 
 Turning westward, the two escarpments take a course somewhat parallel 
 with Clare River, to Sugar Island on the south side of Stucco Lake, but 
 the lower occasionally crosses to the north side, on the way. On the east 
 side of the Moira River, the escarpments are more widely separated than 
 hitherto, the lower occurring about a quarter of a mile, and the higher 
 five miles down the stream from the lake. On the west side, the second 
 escarpment rises abruptly from the river in the third range ; the beds 
 of the lower deposit are cut nearly in two, upwards of a mile from 
 
180 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 the river, by a projecting ridge of gneiss, which extends for three miles 
 Hungerford. to the south-west from Stucco Lake. At the termination of this Lauren- 
 tian spur, on the third lot of the fifth range of Hungerford, an escarp- 
 ment rises about fifty feet high in nearly horizontal strata. The lower 
 beds, exposed at a distance of about a hundred yards from the gneiss, 
 consist of pale bluish drab calcareous rock, without fossils, and may belong 
 to the lower deposit ; while the strata at the summit are dark brownish- 
 grey or blackish limestone, in pretty regular courses of from two to 
 three feet thick, holding Leperditia and some small univalves. 
 
 171-174. GA8TEREPODA (TK.) 
 
 173 a 
 
 174 
 
 I 1 ?!. Eunema Erigone (Billings). 
 
 172. Trochonema umbilicata (Hall). 
 
 173. Ophileta Ottawaensis (Billings); a, side view; 6, view of umbilicus. 
 
 174. Pleurotomaria subconica (Hall). 
 
 Below Hungerford Mills, on the twelfth lot of the tenth range of Hun- 
 gerford, which is on the north-west side of the Laurentian spur, strata are 
 exposed at the edge of the river, which must be near the base of the lower 
 deposit. They are in ascending order as follows : 
 
 Ft. in. 
 
 Dark blue limestone, 7 
 
 Drab colored limestone of very fine texture, in courses of three inches thick, 
 
 supposed to be fit for lithographic purposes, 9 
 
 Bed arenaceous limestone, passing into calcareo-arenaceous shale at the top, ... 8 
 Grey limestone, 4 
 
 6 
 
 Professor Chapman of Toronto states that in the red calcareo-arenaceous 
 rock of this place there is between forty and fifty per cent, of magnesian 
 carbonate of lime. The lowest and nearest Silurian dolomite to the east- 
 ward, of which the horizon is certain, belongs to the Calciferous, and this 
 
CHAP. IX.] TRENTON GROUP. 181 
 
 fact would rather strengthen the evidence afforded by the Piloceras at 
 Kingston Mills, as to the age of the Hungerford strata. Some of the Pots- 
 dam sandstone near Vanluvin's mills has a red color, but a red tinge 
 there prevails also in a part of the succeeding rock ; while the escarpment to 
 which these strata at Vanluvin's mills and at Hungerford are subordinate, 
 can be traced, with occasional difficulties, the whole way. 
 
 175, 176. GASTEROPODA (TB.) 
 175 
 
 175. Pleurotomaria supracingulato (Billings). 
 1 76. P. Progne (Billings). 
 
 At the lower end of Hog Lake on the south side, on the nineteenth lot 
 of the thirteenth range of Huntingdon, beds very nearly corresponding in 
 character with those of the Hungerford section, form a low cliff close to the 
 beach. The same rock appears to form the base of several outlying Silu- 
 rian patches in Madoc, and to be traceable to Marmora. 
 
 The section at the Marmora iron works, on the bank of the Crow River, Marmora, 
 is in ascending order as follows : 
 
 Ft. in. 
 
 Shaly limestone, filling depressions in the surface of contorted Laurentian gneiss, 
 
 which contains beds or veins of fine grained syenite, 1 
 
 Red sandstone, soft and calcareous ; the color is deep red in the divisions of the 
 beds, and lighter towards the middle of them ; one or two thin interstratified 
 layers are greenish, 8 3 
 
 Yellowish-white compact limestone of a character fit for lithography. This 
 increases to four inches about twenty yards to the N. N. "W. in the strike, 
 where however it appears to have too many crystals for lithographic pur- 
 poses. It has rough slightly dentated interfitting surfaces, with a greyish- 
 brown film between in some parts ; it has also small light green and some 
 dark olive-green patches, 1 
 
 Greenish calcareo-arenaceous shale, spotted with red, with a few quartz pebbles, 
 and a few cavities, as if calcareous pebbles had been worn out of them. At 
 the top there is a thin layer of snuff-brown earth, probably manganesian, 
 passing into green shale, 3 5 
 
 Mottled grey and greenish-white argillaceous limestone, slightly bituminous, ... 1 5 
 
 Dark grey bituminous limestone, somewhat shaly in part, 2 
 
 Light grey compact slaty limestone ; this would probably form good building 
 stone ; it is strong and very even but rather thin bedded ; some of it appears 
 fine enough for lithography, 2 
 
182 GEOLOGY OF CANADA. [CHAP. IX. 
 
 Ft. in. 
 
 Light brownish-grey compact limestone in a single bed ; this is apparently fine 
 enough in texture for lithographic purposes, but not of the right color ; it 
 has a small quantity of bitumen in it. Though seemingly one bed, it 
 splits apart in some places, and shews surfaces with short tooth-like inter- 
 fitting columnar projections, having a thin film of bituminous matter between, 1 7 
 
 Light brownish-grey calcareous shale, the last inch and a half becoming a hard 
 
 limestone in an even bed, 10 
 
 Columnar Light brownish-buff compact very fine limestone, the grain wholly impalpable ; 
 structure. the lower half is more homogeneous than the upper, which holds thin 
 lenticular crystals of calcspar ; the upper inch, which is just above the 
 part holding most crystals, fits upon it in tooth-like projections of a marked 
 character, the projections having columnar sides at right angles to the bed, 
 an inch long in some places ; a thin film of bituminous shale darkens the 
 Lithographic surface ; in the lower part there are obscure tooth-like divisions. This is 
 the Marmora lithographic bed, the best stone being in the lower portion. When 
 exposed to the weather, this part is generally affected by gash-like cracks, 
 which appear to terminate both ways, and run in two general directions, 
 dividing the mass into rhomboidal forms ; but there are other gashes which 
 run at a small angle to these ; the stone weathers nearly white, 2 
 
 Light grey limestone ; the fracture is conchoidal and slightly scaly ; the stone is 
 strong and tough, and it would make a good building stone. It weathers 
 slightly yellowish at the joints and bed divisions ; the beds are from three 
 to four inches thick, but aggregated beds of a foot and more occur ; some 
 of them separate in tooth-like projections, with a film of bituminous shale 
 between. Large slabs may be obtained, some of them six feet square ; some 
 of the surfaces are waved, 5 
 
 Light greyish-brown compact smooth limestone, weathering into gashes like the 
 
 lithographic stone, and more divided into joints than the bed below, 2 2 
 
 Brownish-grey compact limestone, rather lighter in color than the previous bed, 
 with lenticular crystals of calcspar ; this would make lithographic stone 
 were it not for the crystals, 7 
 
 Brownish-buff compact limestone with a conchoidal fracture ; there are lenticu- 
 lar crystals of calcspar in the bed, but much smaller than those of the pre- 
 vious layer. This might yield lithographic material ; it is doubtful, however, 
 whether the crystals are not too numerous, 7 
 
 Darkish grey very compact limestone with a conchoidal fracture, 5 8 
 
 Measures concealed, 5 
 
 41 7 
 
 These beds, in which no organic remains have been detected, are suc- 
 ceeded by about forty feet of limestone having much the same lithological 
 characters, in which fossils are sufficiently abundant, though many of them 
 are obscure. Those which have been recognised belong to the Birdseye 
 and Black River formation. In this section there appears to be such a 
 passage from the arenaceous beds at the bottom to the compact limestones, 
 which become fossiliferous at the top, as to induce the supposition that the 
 whole belong to the formation named, notwithstanding the two Chazy species 
 found at Vanluvin's mills. The rock of Kingston, which appears to be 
 nearly destitute of fossils, presents many instances of the columnar struc- 
 
CHAP. IX.] 
 
 TRENTON GROUP. 
 
 183 
 
 ture so prevalent at Marmora. It frequently contains small masses of Kingston; 
 yellow blende. Geodes holding sulphate of strontian occur in the lime- 
 stone at Kingston and near Sydenham, but these minerals have not been 
 met with in what is considered its equivalent to the westward. 
 
 That part of the Birdseye and Black River formation which is well marked 
 by its fossils, after crossing the upper part of Wolf Island, reaches Catara- 
 qui Point, a little above Kingston, and strikes for the west end of Lough- 
 borough Lake. From this, westward, it constitutes a third escarpment, 
 
 177-179. GASTEROPODA (TR.) 
 
 179 
 
 1*77. Murchisonia bellicincta (Hall). 
 
 ITS. M. gracilis (Hall). 
 
 179. Subulites elongatus (Emmons). 
 
 which rises at a varying, but usually not very great distance, back from the 
 two escarpments in which the less fossiliferous strata occur, presenting a 
 bolder and usually more rocky front than either of them. The attitude of the 
 whole series, including the Trenton, which does not usually show any marked 
 escarpment, is for the most part nearly horizontal, the inclination in many 
 instances being so small as to be almost inappreciable. In consequence, it 
 happens, that, except in the escarpments and in sections worn out in the 
 courses of streams, the rock is seldom seen, being concealed by a great 
 
184 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 deposit of drift. The general strike, through the country to Lake Huron, 
 
 is about north of west, and the dip, on an average, is about two degrees to 
 
 undulations, the southward. There is however a series of gentle parallel undulations, 
 
 which affect the strata, running nearly at right angles across the general 
 
 180, 181. GASTEROPODA (TK.) 
 
 180 
 
 181 
 
 Il9.Pleurotomaria Americana (Billings); section through the middle, 
 
 showing the form of the umbilicus. 
 180. Bellerophon bilobatus (Sowerby) ; a, view of aperture ; b, side view. 
 
 strike, the usual bearing being about 1ST. N. E. and S. S. W. Where these 
 undulations occur, the lower rocks come to the surface in long narrow 
 ridges, sometimes extending for several miles to the southward ; and on 
 
 182, 183. CRUSTACEA (TK.) 
 
 182. Jlsaphus megistos (Locke). 
 183. A. platycephalus (Stokes). 
 
 either side of them the fossiliferous escarpments rise, usually at no great 
 distance, sloping gently in directions obliquely opposite to one another. 
 
CHAP. IX.] TRENTON GROUP. 185 
 
 These features are more particularly observable in Loughborough, Camden, 
 and Sheffield, and in Hungerford, Madoc, and Marmora, extending thence 
 on the Crow River into Seymour. The most conspicuous of these undula- 
 tions are between the townships of Camden and Belmont, where the ter- 
 minal outcrop is in consequence, though tolerably straight in its general 
 bearing, very irregular in detail. 
 
 The more conspicuous and more fossiliferous escarpment presents itself Higher 
 about two and a half miles west of south from the upper one of the other fossiliferous 
 
 1 A escarpment. 
 
 two, on the third and fourth lots of the third range of Loughborough, where 
 beds of brownish-grey bituminous limestone, approaching to brownish-black, 
 crop out. Among other fossils, they hold Tetradium fibratum, Ptilodictya 
 reticulata, StropJiomena alternata, &. filitexta, Cyrtodonta Huronensis, 
 Helicotoma planulata, Orthoceras Bigstyi, Asaphus platycephalus, and 
 Leperditia Canadensis, leaving no doubt that the escarpment belongs to 
 the Birdseye and Black River formation. These beds strike over to the first 
 and second lots of the eighth range of Portland ; and beds resembling 
 them are met with on the road between Portland and Loughborough, in 
 the ninth range, about a quarter of a mile from the second escarpment. 
 In these also occur Ptilodictya reticulata, Stenopora fbrosa, Stro- 
 phomena alternata, and Orthoceras Bigstyi. On Mr. Purdy's farm, in the 
 eleventh lot of the eighteenth range of Portland, on Pond Lily Lake, 
 the third or uppermost escarpment is from a quarter to half a mile south 
 from the middle one. 
 
 From this, these two escarpments, passing diagonally through Camden, Camden. 
 gradually separate more and more. The main or superior one, passing 
 close by Centreville, strikes for the north-west corner of Camden, and the 
 inferior for Beaver Lake. They thus become from four to six miles apart ; 
 but south of Stucco Lake, they approach one another again to within a 
 mile. The Moira River, discharging Stucco Lake, runs on the axis of one 
 of the gentle undulations which have been mentioned. Both escarpments 
 run a considerable distance down the stream, and cross it five miles from 
 one another ; but the upper escarpment, turning northward on the west 
 side, joins the other, and both run in one, for a short distance, in the 
 fourth range of Hungerford. 
 
 On the Moira, the strata which constitute the escarpment marked by Moira Elver, 
 the well known fossils of the Birdseye and Black River formation, have a 
 thickness of about sixty-five feet. In ascending order, they are : 
 
 Feet. 
 
 Brownish-black very close textured limestone with a conchoidal fracture, weather- 
 ing ash-grey, in regular beds varying from six inches to a foot in thickness ; 
 some of the beds hold Leperditia Canadensis, and Orthoceras Menelaus, 30 
 
 Dark grey or blackish brittle limestone of a fine texture, with a conchoidal frac- 
 ture. No fossils are detected on breaking the stone in the lower two thirds 
 of the mass ; in the upper part there are obscure fossils, 11 
 
186 GEOLOGY OF CANADA. [CHAP. IX. 
 
 Feet. 
 
 Greenish-drab compact limestone, weathering white, in massive beds with numer- 
 
 ous fossils, many of them replaced by silica, ............................ 10 
 
 Brownish-grey and brownish-black limestone holding many nodules of black 
 chert ; a strong three-feet bed at the bottom abounds in Columnaria alveo- 
 lata and Stromatopora rugosa. The beds in the middle are thin and some- 
 what irregular ; those at the top vary from six to eight inches, and hold Stro- 
 matopora rugosa, Strophomena alternata, and Orthis tricenaria, ............ 14 
 
 The beds which succeed these are well marked by fossils of the Trenton 
 formation ; they are as follows : 
 
 Feet. 
 
 Grey limestone of a crystalline texture, derived from the peculiar crystallization 
 of the echinodermata, which, in a comminuted condition, constitute the mass 
 of the rock. The beds vary in thickness from six to eight inches, the thickest 
 being at the bottom, and they are separated by thin layers of grey calcareous 
 shale. The limestone weathers to a yellowish-grey tinge. The fossils which 
 can be identified are Stenopora fibrosa, Ptilodictya recta, Glyptocrinus ramu- 
 losus, Glyptocystites multiporus, Leptcena sericea, Strophomena alternata, 
 Orthis testudinaria, 0. lynx, Rhynchonella increbescens, and R. recurvirostra, . . 20 
 
 Bluish limestone in thin beds and often nodular, interstratified with layers of 
 shale, increasing towards the top near Belleville ; the dip of the strata is 
 down the stream with an inclination of from one to two degrees. In the 
 lower part the limestone weathers whitish, and in many instances the fossils 
 are replaced by silica ; being much weathered and ''blackened by vegetable 
 matter, they are brought into strong relief. The most common are Orthis 
 testudinaria and Strophomena alternata, ................................. 594 
 
 614 
 
 To this volume it is probable that there would be still something to add, 
 to give the full thickness of the formation, as the whole of the Prince Edward 
 peninsula belongs to it. The beds of the peninsula seem, in general, to 
 be of a nodular character, and the summit of the deposit would appear to 
 conform in its strike with the south-west front, the limit being concealed 
 under the waters of the lake, probably not very far out from the land. 
 
 In running north through Hungerford, the two upper escarpments sep- 
 arate to the extent of about half a mile, but approach across Huntingdon, 
 Marmora, and run into one in some parts of Marmora. Succeeding the unfossilif- 
 erous section already given there, near the iron works, the beds are : 
 
 Feet. 
 Brownish-grey limestone not well exposed, but fossiliferous, .................. 30 
 
 Brownish-grey bituminous limestone with fossils, .......... .................. 5 
 
 Brownish-grey bituminous limestone with nodules of chert and various fossils, 
 among others Tetradium fibratum, Petraia profunda. Columnaria alveolata, 
 Murchisonia -gracilis, Helicotoma planulata, and Orthoceras recticameratum, . . 4 
 
 39 
 
CHAP. IX.J TRENTON GROUP. 187 
 
 The summit of this mass of strata crosses Crow River at the fall, north 
 of the town line of Marmora and Rawdon, with a slope of forty-two feet 
 in a mile. The river here flows on the axis of an undulation, on which 
 twenty-two feet of the same beds again come to the surface, resting on a 
 protrusion of Laurentian syenite in Rawdon, on Laurentian iron ore at 
 Allan's mills in Seymour, two miles farther down, and on fine grained 
 augitic trap, still two miles beyond. Large fragments of the trap, Breccia, 
 cemented together by limestone, form a brecciated bed at the base of 
 the fossiliferous rock. Near its junction with the trap, the Silurian lime- 
 stone assumes a variety of colors, red, orange, blue, green, and yellow ; 
 and it sometimes happens that all these colors are displayed on one sur- 
 face, giving an appearance a good deal resembling rude mosaic. In the 
 strata south from the trap, the black chert, and the silicified fossils black- 
 ened with vegetable matter, lie on a ground of white-weathering limestone 
 in great abundance. Columnaria alveolata, Stromatopora rugosa, and 
 
 184-186. CRUSTACEA (T.B.) 
 
 185 
 
 184. Phacops callicephalus (Hall). 
 185. Dalmanites Bebryx (Billings). 
 186. Dalmanites Achates (Billings). 
 
 Petraia occur, with Orthoceras, Strophomena, and Orihis. A fragment of 
 an orthoceras here met with was three feet long, the diameter of the upper 
 part being about ten inches. 
 
 The banks of the Trent below Healy's falls, which are a little above River Trent. 
 Crow Bay at the junction of Crow River, rise in vertical limestone cliffs 
 sometimes upwards of forty feet, the strata of which are filled with the 
 fossils of the Trenton formation. The lowest beds of the clifis are from 
 four to eight inches thick, the surfaces being thickly studded with black 
 weathered fossils, chiefly an Orthis. Above these beds is a strong one 
 about three feet thick, holding Leptcena sericea^ Strophomena alternata, 
 
188 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 Orthis testudinaria, and RTiynchonella recurvirostra. The rest of the 
 exposure consists of dark grey or blackish and blue limestones, alternating 
 with dark green calcareo-argillaceous shale. These beds are very fossilif- 
 erous, the most numerous species being the four just named. From Crow 
 Bay to Ramsay's falls, on the ninth lot of the sixth range of Seymour, a 
 distance of about four miles and a half, the measures accumulate at the 
 rate of about forty feet in a mile ; and at the latter place they rise in 
 vertical cliffs on each side of the river to the height of forty or fifty feet. 
 All the beefs are filled with Trenton fossils, and some are almost a mass of 
 Leptcena sericea. 
 
 At Chisholm's Rapids on the Trent, on the eighth lot of the eighth 
 range of Sidney, a section of about six feet of thin bedded bituminous 
 grey limestone is exposed, the prevailing fossils being the same four species 
 as before. Below Chisholm's Rapids, the rock is occasionally seen on the 
 bank of the river, holding in all parts abundance of characteristic fossils of 
 the Trenton formation, and dipping gently a little west of south, at an aver- 
 age not exceeding forty feet in a mile. If this dip were continuous, and no 
 
 187-189. CRUSTACEA (TE.) 
 188 
 
 187 
 
 18*7. Bronteus lunatus (Billings). 
 
 188. Cheirurns pleurexanthemus (Green). 
 
 189. Calymene BLumenbachii (Brongniart). 
 
 undulations existed, causing repetitions of the strata, the thickness from 
 Healy's falls to the mouth of the river would be 960 feet. There appears 
 however to be at least one slight undulation on the east and west reach 
 of the river, north of the town line of Murray and Seymour, which would 
 reduce the thickness to about 750 feet. 
 
 In their western run from Healy's falls, the escarpments we have been 
 following approach Stoney Lake ; the main one presenting an abrupt rocky 
 
\ 
 CHAP. IX.] TRENTON GROUP. 189 
 
 cliff from two to three miles from the south margin of the lake, and the 
 other, of small elevation, approaching the margin to within about a mile. 
 After sweeping round a small sheet of water called White Lake, in the 
 township of Dummer, the two escarpments partially unite, striking Salmon 
 Trout or Clear Lake at about the fourth range of that township, keeping 
 the south shore of the lake to its western extremity. The corresponding 
 escarpment rises on the north-west side of Salmon Trout Lake, and then 
 follows the sinuosities of the chain of lakes and the river up to Buckthorn 
 Lake, keeping the south side, at a distance seldom exceeding a quarter of 
 a mile- It crosses Buckthorn Lake at the strait, about two miles and 
 a half above Buckthorn Falls ; and then, again separating into two parts, 
 the main one strikes nearly straight by Sandy and Pigeon Lakes to the 
 head of Balsam Lake, the inferior escarpment keeping about a couple of 
 miles to the north-east. In the general course westward from Belmont Lake, 
 the rocks composing the lowest escarpment thin out and disappear before 
 reaching the western end of Salmon Trout Lake. Here the base of the 
 series is composed of very regular beds of buff colored limestone, bearing 
 the lithological characteristics of the succeeding portion ; while the upper 
 tier of beds contains black chert and silicified corals of those species 
 which peculiarly distinguish the Birdseye and Black River formation. 
 The whole height of the escarpment, from this, seldom exceeds fifty feet. 
 
 On the Ottonabee, the thick bedded coral-bearing stratum with chert, DOUTO. 
 containing chiefly Columnaria alveolata and Stromatopora rugosa, crops 
 out on the twenty-second lot of the sixth range of Douro, where the 
 river opens into a small lake called Kawchewahnook. Below this, assisted 
 by the effect of a gentle undulation on the axis of which the river runs, 
 there is a continued section of limestones and shales all the way to Peter- 
 borough, holding many characteristic fossils of the Trenton formation. 
 Between Peterborough and Rice Lake, the Ottonabee nowhere exhibits a 
 rock section, nor was there one observed at any place between Rice Lake 
 and the shore of Lake Ontario at Cobourg ; but at the latter place, and 
 between it and Port Hope, there are some small exposures of blackish-grey 
 thin bedded nodular limestone and shale, which, among other Trenton 
 fossils, hold Lingula Oanadensis and Asaphus megistos. 
 
 The farthest-up exposures of Trenton limestone, near the lake shore, Bowmanviiie. 
 occur about a mile south of the village of Oshawa in Whitby, where the 
 dip is N. < 5 ; and at Bowmanviiie, where a quarry has been opened for 
 the purposes of the Grand Trunk Railway, at the summit of the formation. 
 The strata here dip to the north-westward at a small angle, and, as they 
 must finally crop out with a southward dip, it is plain that the beds of the 
 quarry are on the southward side of a synclinal form, and that, after run- 
 ning to the north-east on the strike for some uncertain distance under the 
 
190 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 drift, they must ultimately turn northward to conform to the deeper strata 
 seen farther northward. 
 
 The limestone escarpment south of Burleigh Falls, in the township of 
 Smith, is about eighty feet high. On the summit, thin beds of limestone 
 and shale occur, holding one or two varieties of Leptcena or Strophomena, 
 with fragments of trilobites, encrinites, and corals, but not sufficiently 
 characteristic to determine the formation. Except at the top, the rock is 
 more or less covered by moss and small trees ; but about twenty or thirty 
 feet below, strong beds of limestone occasionally come out in points, and pro- 
 bably represent the cherty beds of the Birdseye and Black River formation. 
 In the continuation of this course westward, the cherty beds with their 
 characteristic corals are displayed at the top of the cliffs which rise over 
 the exit of Buckthorn Lake. They are seen too on Pigeon Lake and at 
 Balsam Lake. Bobcaygewan Rapids, near the foot of Sturgeon Lake. On the north part 
 of Balsam Lake, in a great bay on the west side, they occur on the land 
 of Mr. Stephenson, in block E of Bexley, where they incline at a very 
 small angle southward, and display Oolumnaria alveolata and Stromato- 
 pora rugosa. 
 
 The base of the inferior escarpment is seen at the foot of Mud Turtle 
 Lake, near where 'the continuation of the line between the eighth and 
 ninth ranges of Somerville would cross it, about three miles north from the 
 
 190, 191. CRUSTACEA (TB.) 
 190 
 
 191 a 
 
 1916 
 
 190. Acidaspis Horani (Billings). 
 
 191. Trinucleus concentricus (Eaton) ; a, head showing the spine ; 
 6, a specimen without the spine. 
 
 north-east bay of Balsam Lake. The base consists of pale drab limestone 
 of fine texture, in very regular layers of from three to six inches, without 
 fossils, and over it an escarpment rises a little way south to the height of 
 forty or fifty feet. The upper beds are massive and fossiliferous, but the 
 fossils are very obscure. Among the fossils a small Leptcena was observed 
 to be very abundant, and another bivalve was occasionally found with 
 
CHAP. IX.] TRENTON GROUP. 
 
 encrinites and fucoids, but the specimens are too ill defined to be easily 
 identified. 
 
 At the rapids at the outlet of Balsam Lake there are flat surfaces of 
 limestone exposed just over the edge of the water, with fossils weathering 
 in relief, among which Stenopora fibrosa, Glyptocrinus ramulosus, Leptcena 
 sericea, Orthis testudinaria, and Asaphus platycepJialus are observed. 
 At Fenelon Falls, near. the exit of Cameron's Lake, where there is a 
 section of about twenty feet in the gorge of the river below the cascade, 
 the following Trenton species occur : Ptilodictya acuta, Stenopora fibrosa, 
 S. petropolitana, Heterocrinus Canadensis, columns of Q-typtocrinus, Lep~ 
 tfena sericea, Strophomena alternata, S. filitexta, Orthis testudinaria, 0. 
 lynx, 0. pectinella, 0. subquadrata, Rhynchonella increbescens, R. recur- 
 virostra, Pleurotomaria subconica, MurcTiisonia gracilis, and M. bellicincta. 
 
 On Sturgeon Lake, opposite the mouth of the Scugog River, where the 
 
 strata are of greenish calcareous shale, with very thin beds of limestone, the 
 
 fossils in greatest abundance are Stenopora fibrosa, Petraia corniculum, 
 
 Grlyptocrinus ramulosus, Leptcena sericea, Orthis testudinaria, Rhyncho- 
 
 nella increbescens, Calymene Blumenbachii, and Encrinurus vigilans. 
 
 At the village of Lindsay, on the Scugog River, in Ops, there is a small Lindsay, 
 exposure of blue limestone in beds of six or seven inches, interstratified 
 with blue calcareo-argillaceous shale, holding abundance of fossils : among 
 them are Stenopora fibrosa, S. petropolitana, Crlyptocrinus ramulosus, 
 Leptcena sericea, Strophomena filitexta, Orthis testudinaria, 0. plicatula, 
 Rhynchonella increbescens, R. recurvirostra, Camerella hemiplicata, 
 Pleurotomaria Americana, P. subconica, Bellerophon Ulobatus, Orthoceras 
 Ottawaense, Encrinurus vigilans, and Bathyurus spiniger. 
 
 Between Balsam Lake and Lake Simcoe, a distance of nearly thirty miles, 
 the detailed distribution of the outcrop of the formations which we have 
 been tracing, has not been ascertained. The base of the series is supposed 
 to be limited northward by the south branch of the Black River, a trib- 
 utary of the Severn. It comes upon the east side of Lake St. John, in the Lake Coucw- 
 fifth range of Rama, and continues from the west side to a cove in Lake cLing ' 
 Couchiching, on the thirtieth lot of the lake front. Crossing this lake, 
 it would strike the fifth lot of the tenth range of Orillia, where it is con- 
 cealed, and pass to the mouth of the Coldwater in Matchedash Bay. 
 
 On Lake St. John, the lowest Silurian beds, not far removed from the 
 Laurentian gneiss, consist at the base of a yellowish fine grained and 
 somewhat arenaceous limestone, passing in a few feet to a drab colored 
 compact limestone with a conchoidal fracture, some of the strata resem- 
 bling the Marmora lithographic stone. The thickness seen is about twenty 
 feet. Fossils are rather scarce in the rock, and somewhat obscure, the 
 only one which has been identified being Stroplwmena filitexta. In one of 
 the beds, the fossils are coated with a leek-green mineral, and the same 
 
192 GEOLOGY OF CANADA. [CHAP. IX. 
 
 substance invests what appear to be very small fissures in the rock. On 
 Lake Couchiching there is exposed above the water nearly the same thick- 
 ness of a similar limestone, which is quarried for building and lime burning, 
 for both of which purposes it is well suited. 
 
 Sandstones At the mouth of the Coldwater, a green fine grained sandstone rests 
 es< upon the Laurentian gneiss, in beds of from four to twelve inches thick, 
 interstratified with green arenaceous shales. This sandstone is in great 
 request among the Indians for the purpose of manufacturing tobacco pipes. 
 It is soft and porous when first taken from the bed, but becomes hard after 
 exposure for some time to the air. The Indians carve out their pipes with 
 a common knife, to which the stone yields easily ; and it is not improbable 
 that vessels of larger capacity and greater utility, such as would be suitable 
 for various purposes on a farm, might be made with great facility. The 
 sandstones and shales do not exceed eight or ten feet in total thickness, 
 and they appear to be destitute of fossils. 
 
 These beds are probably immediately beneath those of lakes St. John and 
 Couchiching, as they are beneath those met with to the westward on the 
 two horns of Hog Bay (or Coil's Bay, as called in Bayfield's map), one of 
 the deep recesses on the south side of Gloucester Bay. These two points 
 consist of limestone similar in character to that of Rama. The fossils in 
 some of the beds are coated with the same green mineral, and among the 
 species there occur Strophomena alternata, S. filitexta, Rhynclionella 
 recurvirostra, Cyrtodonta subcarinata, Ctenodonta contract^ Leperditia 
 Canadensis, Beyrichia Logani, Asaphus platycepTialus, and Bathyurus 
 spiniger, leaving no doubt that these limestones belong to the Birdseye 
 and Black River formation. The dip of the beds in Matchedash Bay 
 appears to be south, while that of the more western strata seems to 
 point to the south-westward. The inclination in both cases does not prob- 
 ably exceed from thirty to thirty-two feet in a mile. 
 
 Mara. On the east side of Lake Couchiching, these beds reach to the line be- 
 tween the townships of Rama and Mara, where they become covered over 
 with drift, so that their precise summit has not been determined. Proceeding 
 southward, the strata, after an interval of concealment, are again exposed in 
 Mara, striking to the northward of east, and coming upon the banks of the 
 Talbot River, about three miles and a half from the lake shore. The 
 sections are seldom over five feet in thickness, and a better display exists 
 at the northern extremity of Canise Island, opposite the mouth of the 
 Talbot, where the beds present an aggregate of ten feet over the water's 
 edge. The upper layers are thin, coarse, and irregularly deposited ; but 
 the lower ones are thicker, and afford good limestone for burning. This 
 locality, with those on the Talbot, is very fossiliferous, the species being 
 such as characterize the Trenton formation. 
 
CHAP. IX.] TRENTON GROUP. 193 
 
 A ridge of the Trenton formation is met with near the Beaver River in 
 Thorah ; and on Graves Island, which is considerably to the south of Canise, 
 are to be seen some calcareous rocks, which are probably pretty high up 
 in the series. South-eastwardly, similar beds strike the main shore on the 
 twenty-second lot of the first range of Thorah, not far from the lake corner 
 of Brock ; and it is said that similar limestone is met with on the twenty- 
 third lot of the eighth range of the last mentioned township. On the 
 former lot, the beds are from three to eight inches thick, and constitute 
 an aggregate of ten or twelve feet over the surface of Lake Simcoe. They 
 yield excellent lime when burnt, and are occasionally fit for building. At 
 this place a favorable opportunity is afforded to determine the dip. It 
 would appear to be south-westerly ; and as the strata seen on the lake shore 
 crop out about half a mile from it, where they stand at a height of thirty 
 feet over the lake, the difference between this and their height at the 
 margin would be about eighteen feet, so that the slope may be taken as 
 something between thirty and thirty-five feet in a mile. This would give 
 a volume of about 150 feet for the Birdseye and Black River formation on 
 Lake Couchiching, and from 500 to 600 feet for the Trenton formation 
 on Lake Simcoe. The country to the southward of the exposures men- 
 tioned being covered over with drift, it is difficult to say whether this 
 would comprehend the total thickness. 
 
 Westward from Hog Bay, the whole of the peninsula of Penetangui- 
 shene appears to be enveloped in drift ; but on an island in Georgian Bay 
 beyond it, called the Giant's Tomb, the base of this series of limestones is 
 met with, resting on the Laurentian gneiss, which occupies the north- 
 eastern half of the island. The upper members of the series are on the 
 south-east side of Georgian Bay. They there compose the little islands 
 called the Hen and Chickens, and may be observed about eight miles west 
 of the Nottawasaga River, at McGlashan's mills, as well as at Hurontario, 
 in the township of Nottawasaga ; and at the contiguous corners of Nottawa- 
 saga and Collingwood, where they are seen to pass under the black shales coiiingwood. 
 of the Utica formation. The transverse breadth of the series is thus about 
 thirty miles, and the thickness, supposing the dip to be south-westward at 
 the rate of thirty feet in a mile, would be 900 feet ; but it is not unlikely 
 that the strata may be affected by very gentle undulations, and it would 
 therefore be scarcely safe to state the amount at more than about 750 feet. 
 
 A group of islands situated about eight miles from the east coast of 
 Georgian Bay, between Parry Sound and Franklin Inlet, and designated 
 on Bayfield's chart as the Limestone Islands, very probably belongs to the 
 series of rocks under description. ' South from Collins' Inlet there are two 
 groups, called the Fox Islands and the Papoose Islands ; the former about 
 three, and the latter about seven miles from the general run of the coast. 
 On Bavfield's chart they are described as being composed of limestone. 
 
 N 
 
194 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 Manitoulin 
 Islands. 
 
 Lacloche 
 Island. 
 
 Dolomites 
 and sand- 
 stone 
 
 These also very probably belong to the series, and the distance between 
 them may indicate its breadth in this part. None of these groups how- 
 ever have yet been visited by the officers of the Survey, but strata 
 belonging to the series have been observed by them on Squaw Island, 
 which is westward of the Papoose group. 
 
 Farther to the west, the rocks of the series come upon the Great Mani- 
 toulin Island, and compose the chief part of the promontory separating 
 Wequamekong and Manitouwaning Bays, with one of the points of the 
 mainland opposite ; where, as well as on several islands near, they are seen 
 resting on the Huronian quartzites. With the exception of a narrow strip 
 at the south end, which is occupied by black shales, they compose also the 
 island of Shequenandod, and pass thence to that promontory of the Great 
 Manitoulin which is immediately south of Lacloche Island. They consti- 
 tute likewise the south side of this island. The whole breadth of the 
 series is observable on Lacloche and the Great Manitoulin, where the rate 
 of inclination, although inappreciable to the eye, is uniformly nearly south, 
 descending at the rate of thirty-five or forty feet in a mile. Taking the 
 maximum as the rate of dip, the total thickness would be about 320 feet. 
 The upper part of this consists of bluish, buff, and brownish limestones, 
 which generally weather yellowish. The beds at the top of the series are 
 strongly bituminous ; they are generally of a dark grey in fresh fractures, 
 but weather to an orange red. A large portion of the whole series of 
 limestones in this part is more or less magnesian, and towards the bottom 
 the rock becomes a nearly pure dolomite. 
 
 The whole series of strata is here very fossiliferous ; it is chiefly however 
 from the lower part that specimens have been collected. On Lacloche 
 Island and the extremity of Lacloche peninsula, the dolomitic base of the 
 series, as has been already stated, is seen resting upon twenty or thirty 
 feet of the red, greenish, and whitish sandstones which are considered 
 equivalent to those of Sault Ste. Marie. Some few of the fossils char- 
 acterizing the dolomite descend into the uppermost arenaceous bed, 
 which is red, and are tinged with this color. The dolomite displays a 
 thickness of about thirty feet ; and the fossils which occur in it, immediately 
 above the red strata on Lacloche Island, are Stenopora fibrosa, Tetradium 
 fibratum, Stromatopora rugosa, Columnaria alveolata^ Strophomena alter- 
 nata, S.jilitexta, Orthis subcequata, 0. tricenaria, Khynchonella plidfera? 
 Vanuxemia inconstans, Orihoceras multicameratum, 0. Bigsbyi, 0. recti- 
 cameratum, 0. Murrayi, Illoenus Milleri, Cheirurus pleurexanthemus, and 
 Leper ditia Canadensis, leaving no doubt that the beds belong to the 
 Birdseye and Black River formation. 
 
 In this region, the formation appears to have a somewhat greater thick- 
 ness than has been noticed elsewhere, and its characteristic fossils are 
 associated with a greater number that ascend into the Trenton forma- 
 
CHAP. IX.] TRENTON GROUP. 195 
 
 tion. Five or six islands which lie in the strait separating Lacloche from 
 the Great Manitoulin, may be considered to be somewhat less than half way 
 between the base and the summit of the series. The fossils which occur 
 in the strata composing them, and at the same horizon on the islands 
 immediately west of Lacloche, are Stenopora fbrosa, Receptaculites occi- 
 dentalisj Strophomenafilitexta, Rhynchonella increbescens, R. recurvirostra, 
 Orthis borealis ? Vanuxemia inconstans, Cyrtodonta subangulata, Cteno- 
 donta nasuta, Murchisonia gracilis, Bellerophon bilolatus, Orthoceras pro- 
 teiforme, 0. arcuoliratum, 0. multicameratum^ 0. Huronense, 0. Bigsbyi, 
 0. anceps, Asaphus platycephalus and Leperditia Canadensis. These 
 strata also would thus appear to belong to the Birdseye and Black River 
 formation ; but about half a mile inland from the south side of the strait 
 there rises an escarpment of 155 feet of limestone, which probably attains 
 the summit of the series, and may represent that portion which is to be 
 considered as Trenton. The strata of this escarpment, where they come 
 upon the coast, are however covered up with drift, and no specimens have 
 been obtained from them in the interior to determine the fossils. 
 
 Seven or eight islands which range in a line a little north of west from 
 Lacloche, are composed of the same series of limestones. On the largest 
 of them however, being the one immediately north of Maple Point, the 
 shales of the Utica formation occupy the south' front. Mississague Island, 
 about three and a half miles south from the river which gives it a name, 
 with Grant's Islands, a group about thirteen miles farther on, and the 
 Snake Islands a mile beyond, show the trend of the limestones westward, snake 
 On the Snake Islands about twenty feet of limestone rest almost horizon- Is 
 tally upon the tilted rocks of the Huronian series, about eight feet at the 
 base being made up of fragments of the Huronian quartzites cemented to- 
 gether by fossiliferous limestone. The fossils here are Petraia profunda, 
 Columnaria alveolata, Strophomena filitexta, &. alternata, Orthis testudi- 
 naria, 0. tricenaria, Rhynchonella increbescens, R. recurvirostra, Subulites 
 elongatus, Orthoceras Huronense, Asaphus platycephalus, Illomus angus- 
 ticollis, I. Americanus, and Bathyurus spiniger, shewing the strata, as 
 before, to belong to the Birdseye and Black River formation. 
 
 In the next nineteen or twenty miles, Bigsby, Thessalon, and Serpent raiiadeau 
 Islands, with the south-western island of the Palladeau group, mark the pro- I8lands - 
 longation of the same limestones. The fossils met with on Thessalon Island 
 are Tetradium fibratum, Strophomena filitexta^ Orthis tricenaria, Vanuxe- 
 mia inconstans, Cyrtodonta Huronensis, Orthoceras Bigsbyi, and 
 Asaphus platycephalus ; and on the south-western Palladeau, Tetradium 
 fibratum, Stenopora fibrosa, Lingula Huronensis, Cyrtodonta Huronensis, 
 Vanuxemia inconstans, Pleurotomaria staminea, Orthoceras Bigsbyi, 
 0. recticameratum^ Asaphus platycephalus , and Leperditia Canadensis. 
 
196 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. IX. 
 
 St. Joseph 
 Island. 
 
 Campement 
 d'Ours. 
 
 The northern half of St. Joseph Island is occupied by this series of 
 limestones. That part however which may belong to the Trenton formation 
 is much covered with drift, and it is chiefly from the lower portion of the 
 series that fossils have been obtained to establish its age. As already 
 stated, the fossiliferous limestone here rests upon about eighty feet of 
 sandstone, the outcrop of which, there is little doubt, runs to a junction 
 with the sandstone of Sault Ste. Marie, while an outlying patch of the 
 same two rocks occurs to the north, on the island of Campement d'Ours. 
 As will be seen in the accompanying figure, the exposures on the two 
 islands lie in the same plane of stratification, dipping at a very small angle 
 to the south, the separation between them being the result of denudation. 
 
 192. SECTION OF SILURIAN AND HTJRONIAN ROOKS. 
 
 Campement d'Ouri. Channel. St. Joseph. 
 
 c a b e e b a 
 
 ivg^^Siisr^^ ^^Z i~! 
 
 Horizontal and vertical scale, 1 inch to a mile. 
 
 a, Birdseye and Black River limestone. 
 
 b, Ste. Marie sandstone. 
 
 c, Huronian conglomerates. 
 H, Level of Lake Huron. 
 
 S, Level of the sea. 
 
 The following ascending section gives the characters of the limestone in the 
 exposures observed at Campement d'Ours, the fossils leaving little doubt 
 that it belongs to the Birdseye and Black River formation : 
 
 Feet. 
 
 Bluish-grey shales interstratified with thin beds of yellowish compact limestones, 
 presenting an escarpment over the sandstone. The fossils observed are 
 Stenoporafibrosa, Ptilodictya fenestrata, P. acuta, Strophomena alternata, 
 Rhynchonella plicifera, Murchisonia gracilis, and a small undetermined species 
 of Lingula, 20 
 
 Measures concealed, 60 
 
 Ash-grey compact limestone, in beds of from three to five inches, interstratified 
 with a five-inch bed of drab-colored compact limestone ; among the fossils 
 are Stenoporafibrosa, Glyptocrinus ramulosus, Strophomena alternata, Pleu- 
 rotomaria subconica, Subulites elongatus, Jlmbonychia amygdalina, Cyrtodonta 
 Huronensis, Vanuxemia inconstans, Orthoceras Bigsbyi, 0. Murrayi, Leper- 
 ditia Canadensis, and JLsaphus platycephalus, 4 
 
 Ash-grey compact limestones, in beds of from four to six inches, underlaid by a 
 dark brownish-grey arenaceous limestone bed of about ten inches, and 
 divided by thin layers of grey calcareo-argillaceous shale. All the strata 
 of this division are very fossiliferous, and contain Glyptocrinus ramulo- 
 sus, Ptilodictya mullipora, Coscinium flabellatum, Strophomena alternata, 
 S.filitexta, Rhynchonella recurvirostra, Orthis subcequata, Vanuxemia incon- 
 stans, Cyrtodonta Huronensis, C. subcarinata, Pleurotomaria subconica, Tro- 
 chonema umbilicata, Murchisonia perangulata, Orthoceras recticameratum, 
 Cheirurus 'pleurexanthemus, and Leperditia Canadensis 30 
 
CHAP. IX.] TRENTON GROUP. , 197 
 
 Feet. 
 
 Ash-grey compact limestones of the same character as the preceding, but still 
 more fossiliferous. The beds contain Tetradiumfibratum, Stenopora fibrosa, 
 Columnaria alveolata, Petraia profunda, Ptilodictya labyrinthica, Stropho- 
 mena alternata, S. filitexta, RhynchoneUa recurvirostra, Ambonychia amygda- 
 lina, Cyrtodonta Canadensis, C. Huronensis, Vanuxemia inconstans, Ctenodonta 
 nasuta, Modiolopsis mytiloidea, Pleurotomaria subconica, Eunema strigillata, 
 Subulites elongatus, Orthoceras Bigsbyi, O. Murrayi, an undescribed Cyrto- 
 cerasj Jlsaphus platycephalus, and Leperditia Canadensis, 16 
 
 130 
 
 The strike of these limestones on St. Joseph would carry them across 
 the southern half of Neebish Island into Michigan, but no exposures of 
 them have been observed either on the island or on the mainland. 
 
198 GEOLOGY OP CANADA. [CHAP. X. 
 
 CHAPTER X. 
 
 THE UTICA AND HUDSON RIVER FORMATIONS. 
 
 BLACK GRAPTOLITIC SHALES; ARENACEOUS SHALES AND SANDSTONES. DISTRIBUTION OF THE 
 TWO FORMATIONS. MONTMORENCi; ORLEANS ISLAND; ST. MAURICE. OVERLYING RED 
 SHALES. DESCHAMBAULT ANTICLINAL. MONTREAL ISLAND; CHAMBLY. LAKE ONTARIO; 
 WHITBY; TORONTO. LAKE HURON; OWEN SOUND; MANITOULIN ISLANDS. OTTAWA OUT- 
 LIERS. SAGUENAY; LAKE ST. JOHN. ANTICOSTI. 
 
 The limestones of the Trenton formation are in general separated by 
 thin layers of black and blackish-brown bituminous shale. These layers in 
 some places become thicker towards the top, and present a passage to the 
 succeeding deposit, which consists of black brittle bituminous shales, con- 
 stituting what has been called in New York the Utica slate formation. 
 These shales pass into others of a less bituminous character, which become 
 interstratified with dark grey arenaceous shales, and with light grey sand- 
 stones weathering to a drab, and usually not very thick : with them are 
 occasionally associated some few beds of arenaceous conglomerate with 
 calcareous pebbles. These strata constitute the Loraine shales, or the 
 Hudson River formation of the New York geologists. The most complete 
 River ste. section of the Utica formation occurs on the River Ste. Anne (Montmo- 
 renci), between the lowest fall on the stream and the mouth of its tribu- 
 tary the Riviere a la Rose. At the foot of the fall the upper portion of the 
 Trenton formation is seen leaning, at a high angle against the Laurentian 
 gneiss, which is the rock of the cascade, and it is succeeded by the follow- 
 ing strata in ascending order : 
 
 Feet. 
 1. Black brittle bituminous shale with an undetermined Lingula and Grap- 
 
 tolithus pristis, 19 
 
 Black brittle bituminous shale with two bands of yellow-weathering limestone, 
 
 black within, probably magnesian, and fit for hydraulic purposes, 8 
 
 Black brittle bituminous shale, 23 
 
 Black brittle bituminous shale, breaking into small fragments in consequence 
 
 of an imperfect cleavage independent of the bedding, 11 
 
 Black brittle bituminous shale with Graptolithus pristis, 245 
 
 Grey hard sandstone, interstratified with bands of black shale, 5 
 
 Black brittle bituminous shale, interstratified with beds of sandstone, 7 
 
 318 
 
CHAP. X.] UTICA AND HUDSON FORMATIONS. 199 
 
 Feet. 
 
 2. Light grey yellow-weathering sandstone, with black argillaceous nodules at 
 
 the top ; in some parts the sandstone beds hold fossils, which are obscure, 
 
 but appear to be Leptana sericea and Orthis testudinaria, 10 
 
 Measures concealed, 13 
 
 Black brittle bituminous shale, 6 
 
 Dark grey arenaceous shale, 51 
 
 Dark grey arenaceous shale, 192 
 
 Dark grey arenaceous shale, with thin beds of sandstone, t 8 
 
 Light grey sandstone in a massive bed, weathering greenish in the air and 
 reddish in the water ; two bands of conglomerate occur in the middle, 
 holding pebbles of limestone and of quartz. Some parts appear to weather 
 
 faster than others, in bands conformable with the bedding, 18 
 
 Dark grey slightly greenish arenaceous shale, 58 
 
 Light grey conglomerate beds, with about two feet of fine grained sandstone at 
 the bottom ; the conglomerate parts hold pebbles of limestone and quartz 
 of various sizes up to two inches in diameter, those of limestone being in 
 
 greater abundance than the quartz, 5 
 
 Grey sandstone in a massive bed, becoming a conglomerate in parts, 14 
 
 Grey calcareous conglomerate as before, 3 
 
 Light grey sandstone weathering brownish, 3 
 
 Grey calcareous conglomerate, with soft shaly sandstone as a matrix, 2 
 
 Greenish arenaceous shale, striped with dark grey bands, 84 
 
 Greenish arenaceous shale, striped with dark grey, and having a six-inch 
 band of hard light grey reddish-weathering sandstone at the top, and 
 
 another at the bottom, 18 
 
 Greenish arenaceous shale, striped with dark grey, with occasional bands 
 
 of hard light grey sandstone, weathering reddish-brown as before, 125 
 
 Greenish arenaceous shale, striped with dark grey, with thinner and finer 
 
 bands of light grey sandstone, 39 
 
 greenish arenaceous shale with dark stripes without any bands of sandstone, . . 70 
 
 719 
 
 3. Black brittle bituminous shale, weathering reddish and yellowish-brown, and 
 
 holding Graptolithus ramosus and G. bicornis, with a small Discina and 
 
 Triarthrus Beckii, 16 
 
 Black bituminous and slightly arenaceous shale, not quite so brittle as the 
 
 preceding, except in a few hard black bands, which hold graptolites, 17 
 
 Black bituminous and slightly arenaceous shale, with two bands of a harder, 
 
 more brittle, and more bituminous character, the latter with graptolites, . 4 
 Dark grey bituminous and slightly arenaceous shale, finely striped with black 
 
 lines, 33 
 
 Black brittle bituminous shale, weathering a light or yellowish-brown, without 
 
 grit, and holding Graptolithus and Orthoceras, 7 
 
 77 
 
 1114 
 
 The first division of the above section presents the lithological character- 
 istics of the Utica formation, and the second those of part of the Hud- 
 son River. The third so thoroughly resembles the first division that it is 
 very difficult to distinguish them, particularly as there is a resemblance 
 between the two in the few fossils which are met with. An additional amount 
 
200 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. X. 
 
 Island. 
 
 of dark grey bituminous and arenaceous shales, interstratified with occa- 
 sional light grey brown-weathering sandstones, overlies the third division, 
 on the Ste. Anne, occupying the distance between the mouth of the Riviere 
 a la Rose and the St. Lawrence. In the channel between the margin of 
 Orleans the St. Lawrence and the island of Orleans, deposits of a similar charac- 
 ter probably prevail, and they come upon the island at Ste. Famille, 
 about five miles above the point opposite the mouth of the Ste. Anne. 
 Along the north margin of the island black bituminous shales occur, 
 with some thin beds of black bituminous limestone, interstratified with 
 occasional grey yellow-weathering arenaceous limestones from three to 
 twelve inches thick. In the black shales there occur Grraptolithus bicornis 
 
 193-195. BRYOZOA ? (IT.)* 
 
 193 194 195 
 
 19B. Graptolithus bicornis (Hall). 
 
 194. G. ramosus (Hall). 
 
 195. G. pristis (Hall. Hisinger?) 
 
 and Gr. ramosus. The direct breadth across the deposit, from the Riviere 
 a la Rose, is probably about three miles and a half. In the part between 
 this tributary and the mouth of the Ste. Anne there appear to be at least 
 two undulations, and others probably occur under the St. Lawrence ; so 
 that it is difficult to state with precision the whole thickness to be assigned 
 to the Hudson River formation. It is probably however not over-estimated 
 at 2000 feet, while that of the Utica formation, as already shewn in the 
 section, is over 300 feet. 
 
 North-eastward from the river Ste. Anne (Montmorenci) these two 
 formations come out obliquely upon the St. Lawrence, the Utica shales 
 
 * The fossils of the Utica formation are 
 given in this chapter before those of the 
 Hudson River, and are distinguished by 
 
 the letter U, those of the latter formation 
 being marked by the initials H. R. 
 
CHAP. X.] UTICA AND HUDSON FORMATIONS. 201 
 
 reaching the margin a little above Cape Tourmente, and about eight miles 
 from the Ste. Anne. To the south-westward they occupy the space 
 between the Trenton formation and the margin of the St. Lawrence, as far 
 as Quebec. Their distribution as far as Beauport church has already been 
 given in describing that of the Trenton, and it is sufficient for the present 
 purpose to state, that opposite to the fall of the Montmorenci the Hudson 
 River formation occurs on the north side of the island of Orleans, at the 
 upper end, giving there to this formation a breadth of about two miles. 
 
 After leaving the Montmorenci dislocation at Beauport, from which 
 they turn north-westward in a narrow band with a sharp dip, the Utica 
 shales gradually spread out, by the diminution of their slope, to a breadth 
 of about a mile and a half on the axis of the synclinal beyond. Near 
 Charlebourg church the breadth diminishes again to about a quarter of chariebourg. 
 a mile ; but on the St. Charles River it once more reaches a mile and a 
 
 half, through the effect of an undulation. Between this and Pointe aux 
 
 i 
 
 196, 197. BRACHIOPODA (TT.) 
 
 196 197 
 
 196. Lingula Progne (Billings) ; a, dorsal valve ; 6, ventral valve. 
 197. L. curia, (Hall). 
 
 Trembles, the Utica shales are seen in many places, more particularly in 
 St. Augustin, where they abut against the Laurentian gneiss. 
 
 From Beauport to Pointe aux Trembles, the space between the Utica Quebec, 
 shales and the St. Lawrence is occupied by the Hudson River formation, 
 with the exception of Cape Diamond, on which Quebec is situated, and the 
 ridge which runs from it, by the plains of Abraham, to the Cape Rouge 
 River ; as well as a strip extending about a mile and a half along the St. 
 Lawrence, beyond that river. These belong to the Quebec group, hereafter 
 to be described, and behind them the Hudson River rocks present a lower 
 surface, with a breadth of between four and five miles. A south-westward 
 continuation of the Montmorenci dislocation would run between the two. 
 The rocks of Quebec are, however, not brought into their position by this, 
 but by another and very remarkable break in the same place, which will be 
 more particularly mentioned in a future chapter. Where the Hudson 
 River formation comes upon the St. Lawrence, above Cape Rouge, it pre- 
 sents a bold, nearly vertical cliff of about a hundred feet, the base of which, 
 for two miles up, is washed by the flood at high tides. Near to the dislo- 
 cation the rock consists of black bituminous shales, some of which holcj 
 Q-raptolithus ramosus and Cr. pristis. Associated with the shales are two 
 
202 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. X. 
 
 thick beds of a hard jaspery character, and olive-green color, with short 
 cracks in various directions, occasionally holding a black carbonaceous 
 matter resembling anthracite. The shales a little higher up, on the mar- 
 gin of the river, become interstratified with occasional calcareous sand- 
 stones, and one or two beds of limestone conglomerate, in which Leptcena 
 serieea, Strophomena alternata, and Orthis testudinaria occur in some 
 abundance. 
 
 Grondines. From Pointe aux Trembles to the Grondines, the two formations fill up 
 the space between the summit of the Trenton group and the St. Law- 
 rence, generally presenting, in the lower half of the distance, a bold nearly 
 vertical front to the river. In this neighborhood the passage from the 
 Utica to the Hudson River formation, by a diminution of bituminous 
 matter, is so gradual, that the division between them has to be somewhat 
 arbitrarily assumed. The position taken as indicating this would leave the 
 
 198-200. CRUSTACEA (U.) 
 
 198. Triarthrus glaber (Billings). 
 
 199. T. spinosus (Billings). 
 
 200. T. Beckii (Green). 
 
 latter formation spread out in two separate areas on the north-west bank ; 
 one in the synclinal between Pointe aux Trembles and Cap Sante*, and the 
 other, which is but little exposed, between Cap Santo* and Deschambault. 
 Where the Utica shales fold over the Pointe aux Trembles anticlinal, they 
 are concealed beneath the waters of the St. Lawrence ; but they strike into 
 the land again on the north-west side of the anticlinal, with a breadth occu- 
 pying about a mile and three quarters on the margin of the river. The 
 Hudson River area, between the Pointe aux Trembles and Cap Sant6 anti- 
 clinals, extends four and a half miles along the margin ; and behind the village 
 of Les Ecureuils, which is in the middle of the distance, it has a breadth of two 
 miles. Sweeping around this area, the Utica shales come upon the Jacques 
 Cartier River, which in the last six miles of its course runs through them, 
 in a deep ravine with nearly vertical sides. Folding over the Cap 
 
CHAP. X.] 
 
 UTICA AND HUDSON FORMATIONS. 
 
 203 
 
 anticlinal, they have a breadth of probably five miles, about a mile and a 
 half of which is concealed under the St. Lawrence ; and from the axis of 
 the anticlinal, their breadth gradually diminishes as the formation sweeps 
 round the synclinal to Portneuf Biver, where it may be upwards of a mile. 
 This breadth is probably maintained along the south-east side of the Des- 
 chambault anticlinal as far as the Grondines. 
 
 Between the Jacques Cartier River and Cap Sante* 5 the Utica shales are cap sants. 
 interstratified with a bed or two of black limestone, sometimes reaching a 
 foot in thickness ; and on the beach at Cap Sante* village there is a thick- 
 ness of about twenty feet of argillaceous limestone of a lighter color. In 
 the vicinity, layers of this lighter colored limestone of from four to six 
 inches thick, are met with at intervals, above the twenty-feet band ; and 
 they afford in several places close to the cliff, and out between high and 
 low water mark, beautifully even slabs, fit for door lintels, window sills, and 
 such purposes. The slope of the strata being very moderate, considerable 
 areas are exposed on single beds : these are often cut up by joints, the 
 planes of division running in three principal directions. 
 
 The great dislocation, which limits the Hudson River formation above 
 the Cap Rouge River, crossing the St. Lawrence obliquely, reaches the 
 opposite side a little above the church of St. Nicholas. From this point 
 the formation constitutes a bold cliff running along the south side of the St. 
 Lawrence by St. Antoine, St. Croix, and Lotbiniere, to the Grande Riviere 
 du Chene, the distance being upwards of thirty miles. Inland, the southern 
 limit of the formation is traceable to St. Antoine, where it is about two 
 miles and a half from the river. It is here marked by a black limestone, 
 holding, among other fossils, Stenoporafibrosa,Petraia corniculum, Stropho- 
 mena filitexta, Oamerella extans, Bellerophon bilobatus, and Trinucleus 
 concentricus. Farther up it becomes obscured by drift. It probably, 
 however, reaches the Grande Riviere du Chene in a pretty straight line, 
 and runs westward on the south side of it, conforming in its distribution 
 to the effect of the Pointe aux Trembles and Cap 8ante* anticlinals. On the 
 south-east side of the Deschambault anticlinal, the limit of the dark shales 
 is removed about seven miles from the St. Lawrence, on the line between 
 the seigniories of Deschaillons and St. Pierre les Becquets ; the axis of the 
 anticlinal being about half that distance from the river. 
 
 The strata at the summit of the Hudson River formation here dip S. Red shales. 
 < 8, and are followed by a set of red shales, which appear to overlie them 
 conformably. Where the road running near the top of the lower forma- 
 tion crosses the Little River du Chene, the beds are fossiliferous. Among 
 the fossils found here, and at various places along the margin of the river 
 between St. Nicholas and Riviere du Chene, are Leptcena sericea, Stro- 
 phomena alternata, and Orthis testudinaria. Beds of drab-weathering 
 sandstone are occasionally interstratified among the shales of the cliffs on 
 
204 GEOLOGY OF CANADA. [CHAP. X. 
 
 the south side of the St. Lawrence, between the Grande Riviere du Chne 
 and St. Nicholas, and frequently present the fossils just named, in some 
 abundance. 
 
 On the north side of the St. Lawrence, from the Grondines to the island 
 of Montreal, a distance of about a hundred miles, the space between the 
 margin of the river and the exposures which have been mentioned as 
 belonging to the Trenton formation, is so much covered with drift, that in 
 an area of about 1000 square miles, only two exhibitions of the strata have 
 st. Maurice, been discovered, both belonging to the Utica formation. One of these 
 is on the St. Maurice, and the other on the Achigan. That on the St. 
 Maurice occurs on the left bank, at Pointe a la Hache, about nine miles 
 from the St. Lawrence, and nearly opposite to the St. Maurice forges ; it 
 occupies about 200 yards of the margin. The dip varies from S. 30 E. 
 to S. 45 E., with a slope of two degrees, and the deposit consists of black 
 bituminous shales, inters tratified with occasional layers of black bituminous 
 limestone. The limestone has a smooth surface and a smooth conchoidal 
 
 201. CRUSTACEA (U.) 
 
 201. Jlsaphus Canadensis (Chapman). 
 
 fracture, and becomes reddish-yellow under the influence of the weather. 
 The fossils which characterize the beds are G-raptolithus pristis, a small 
 Discing and Triarihrus Beckii. It is probable that the deposit extends 
 farther up the stream ; for 300 yards above Pointe a la Hache, on the 
 right side, fragments of similar shales are strewed on the bank, and there 
 is a ripple across the river, perhaps occasioned by an outcrop of the 
 shales in the bottom. The exposure on the Achigan, as has already been 
 mentioned, occurs on the boundary line between the seigniories of L'As- 
 somption and St. Sulpice, not far from the highest Trenton beds seen in 
 that neighborhood. It presents a thickness of about twelve feet, and 
 consists entirely of black brittle bituminous shales. 
 
 These two exposures give but imperfect data to determine the distribu- 
 tion of a hundred miles of the formation to which they belong. Their posi- 
 tions appear sufficient however to establish the probability that there must 
 
CHAP. X.] UTICA AND HUDSON FORMATIONS. 205 
 
 be some breadth of the Hudson River formation on the north side of the 
 St. Lawrence in this part, and that it may occupy several miles at the 
 mouths of the St. Maurice, Batiscan, and Champlain Rivers. A set 
 of fossiliferous strata, such as sometimes indicate an approach to the 
 summit of the formation, is met with on the south side of the St. Lawrence, 
 just opposite to the St. Maurice. The beds appear to be in a nearly hori- 
 zontal attitude, and are marked by Stenopora fibrosa, Leptcena sericea, 
 tStrophomena alternata, Orthis testudinaria, 0. occidentalis, Athyris 
 Headi) Rhynchonella capax, Avicula demissa, Orthoceras crebriseptum, 
 and Asaphus platycephalus. They rise into a low ridge occupying the st. Gr<goire. 
 chief part of the space between the shore and Lake St. Paul ; on the south 
 side of which lake, the red shales, already mentioned as overlying the 
 Hudson River formation, form a marked escarpment. In this relation, 
 dipping southward at an angle of one or two degrees, the fossiliferous beds 
 and the overlying red strata, are traceable down the St. Lawrence nearly as 
 far as the Gentilly River. The escarpment of red shales can be followed 
 in an opposite direction to the Nicolet. Four and a half miles from the 
 mouth of this river, rocks of a red color are exposed on its banks. 
 
 The patch of red shale to which this escarpment belongs, lies in a shallow syndinai. 
 synclinal form, with a breadth of nearly eight miles. It is separated 
 from the red shales of St. Pierre les Becquets, in the prolongation of these 
 to the south-westward, by fossiliferous grey shales of the Hudson River 
 formation, brought to the surface by the Deschambault anticlinal on the 
 Becancour, in the sixth range of Maddington, and again on the Nicolet, 
 about fourteen miles from its mouth. Although no fossils have as yet Red shales, 
 been detected in these two patches of red shale, their color and position 
 make it probable that they should be classed with the succeeding forma- 
 tion, which is the Medina sandstone. In its continuation south-westward 
 from the Nicolet, the axis of the Deschambault anticlinal, which runs 
 between them, appears to cross the St. Francis toward the north-west 
 side of Wendover and Grantham, where it is marked by Hudson River 
 graptolites. Farther on, the axis reaches St. Dominique in the seigniory st. 
 of St. Hyacinthe, and thence its course would carry it to the neighbor- uique> 
 hood of Phillipsburgh, near the province line. In the seigniory of St. 
 Hyacinthe, not far to the south-east of this axis, and parallel with it, will 
 probably run the continuation of that great break in the strata wilich has 
 already been alluded to as occurring at Quebec. 
 
 About six miles north-eastward of St. Dominique, the Deschambault Anticlinal, 
 anticlinal brings to the surface the Trenton formation. The limestones 
 belonging to this, as well as those of the Birdseye and Black River, and 
 occasionally the Chazy, all determined by characteristic fossils, are trace- 
 able in a comparatively narrow strip from this position, with few intervals 
 of interruption, by St. Dominique and St. Pie, to the boundary between 
 
206 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. X. 
 
 St. Hyacinthe and Farnham. Among the Chazy fossils met with are 
 Ptilodictyafenestrata, Orthis borealis, 0. platys, Strophomena alternata^ 
 Vanuxemia Montr ealensis, and Pleurotomaria Crevieri: with these are 
 sandstone, associated Ampyx Halli. A sandstone, of which about thirty feet are 
 seen, underlies the fossiliferous limestones, and is supported by a very pure 
 dove-grey limestone, without observed fossils. Along the whole range of 
 the exposures, the dip appears to be to the eastward ; but in the neighbor- 
 hood of St. Pie, some of the dove-grey limestone, a little removed to the 
 westward of the range, has a westerly dip. This is considered sufficient 
 to show the existence of an anticlinal. There may however be a disloca- 
 tion connected with it, throwing up the measures on the east side. 
 
 Between the summit of the Trenton formation, as already traced in its 
 distribution from the west side of Lake Champlain to the Maskinonge* on 
 the one hand,, and the Deschambault anticlinal from the St. Francis to 
 
 202-204. ZOOPHYTA (H. R.) 
 
 a 202 6 
 
 202. Favistella stellata (Hall) ; a, longitudinal section through several 
 
 of the tubes ; 6, transverse section. 
 203, 204. Varieties of Stenopora fibrosa (Goldfuss) ; a, a, portions of the 
 
 surface magnified. 
 
 Farnham on the other ; the whole country, comprising an area of about 
 2500 square miles, appears to be underlaid by the Utica and Hudson 
 River formations, with the exception of the intrusive masses of Montar- 
 ville, Rouville, Rougemont, and Monnoir Mountains. In this area is 
 included another small shallow synclinal mass of the overlying red shale, 
 crossing the St. Francis about seven miles from its mouth. 
 
 Along the eastern front of the island of Montreal there is space above 
 the highest exposures of the Trenton limestone for a part of the Utica 
 formation ; but no exhibition of its strata occurs before reaching the city. 
 
CHAP. X.] UTICA AND HUDSON FORMATIONS. 207 x 
 
 The first exposure of them, proceeding along the margin of the island, is Montreal 
 at Point St. Charles, and several are met with between that point and the Island> 
 head of Sault St. Louis. The black shales extend from the water's edge 
 'at least as far back as the city aqueduct and the third lock of the Lachine 
 canal ; the upper part of the aqueduct and the lower part of the canal 
 having been, in some parts, excavated in these shales. In front of 
 Montreal, the deposit forms St. Paul's Island, and it was met with in the 
 bed of the St. Lawrence, at the foundation of every one of the piers of 
 the Victoria Bridge. On the right bank of the river it is seen at Lon- 
 gueuil, with some of its characteristic graptolites, and its summit may here 
 attain the distance of a mile from the water. This would give to the Utica 
 formation, in this part, a total breadth of about four miles. The dip of 
 the strata, which is about east, exhibits a slope in several places of between 
 three and five degrees ; but there may be several gentle undulations under 
 the river, and one of the depressions probably underlies St. Helen's Island, 
 which, with Round Island immediately below, constitutes an isolated patch 
 of a much newer formation. These undulations would materially diminish 
 the average inclination of the strata, and make it probable that the thick- 
 ness of the deposit at Montreal does not exceed that assigned to it 
 near Quebec. 
 
 In the neighborhood of Montreal, the Utica shales, like the limestones 
 beneath them, are much intersected by trap dykes, and intercalated with 
 trap floors. Instances of the former are seen on the right bank of the 
 river opposite and below St. Helen's Island ; and of the latter, about a Trap floors, 
 quarter of a mile forward, on the cutting for the St. Lawrence and Atlantic 
 Railroad, as well as at Moffatt's Island, where the trap is a trachyte, and at 
 Laprairie. On the left side, they are met with at Point St. Charles, on St. Point st- 
 Paul's Island, and higher up the river. Where the outcrops of these floors Charles, 
 come into the bed of the stream, and at any place cross its course, the 
 unequal wearing of the soft shale and hard trap leaves projections and steps 
 in the bottom, which frequently occasion leaps and rapids, impeding the 
 navigation of the river. The Sault Normand, out in front of Point St. 
 Charles, appears to be of this description, the ledge occasioning it being 
 probably connected with the trap at the point. More important instances 
 occur in several parts of the Sault St. Louis. On the aqueduct near 
 Lachine there is met with a set of white trachyte and phonolite dykes, 
 hereafter to be described, which cut not only the shales of this formation, 
 but the more ancient dolerites and melaphyres by which these shales are 
 penetrated. A dyke of a similar description, near the reservoir, intersects intrusive 
 the trap of Mount Royal, and an isolated patch of the Utica shales which dykes - 
 abuts against the mountain, shews, what the limestone beneath leaves 
 doubtful, that this great mass of trap breaks through the strata, The 
 shales are considerably indurated near the junction, and at the point of 
 
208 GEOLOGY OP CANADA. [CHAP. X. 
 
 contact of similar shales with an intercalated layer of trap at Point St. 
 Charles, well formed crystals of pyroxene penetrate the shale to a dis- 
 tance of half an inch. 
 
 Above Longueuil, the Utica shales sweep round by Laprairie, La Tortue, 
 and St. Philippe, to the Richelieu River, where they are seen in the exca- 
 vations of the Chambly canal, and are again intersected by dykes of 
 trachytic trap. Folding over the axis of the Chambly anticlinal, the 
 formation -runs up the east side of the Richelieu, with a width extending 
 beyond Henry sville, where Triarthrus Beckii occurs, and the formation 
 apparently constitutes all that point on Lake Champlain lying between 
 the exit of the lake and Missisquoi Bay. 
 
 Although it is stated as probable that the upper limit of the Utica forma- 
 tion does not extend beyond a mile from the St. Lawrence at Longueuil, 
 the strata characterized by the fossils of the Hudson River formation are 
 
 205. ZOOPHYTA (H. R.) 
 
 2Q5.Petraia Canadensis (Billings). 
 
 not met with nearer than four miles beyond this. These fossiliferous beds 
 are laid bare in the cutting for the St. Lawrence and Atlantic Railway ; 
 and kept at the surface by undulations, they occur at intervals, across the 
 measures, as far as the Yamaska. There is a development of them on both 
 sides of the Richelieu, at the rapids above the basin of Chambly. The strata 
 are there nearly flat, and consist of alternating layers of bluish and grey 
 argillaceous and calcareous shales. The calcareous beds are at the same 
 time arenaceous, and exhibit many organic remains, among which are the 
 
CHAP. X.] 
 
 UTICA AND HUDSON FORMATIONS. 
 
 209 
 
 characteristic species Avicula demissa, Modiolopsis modiolaris, Orthonota 
 nasuta, and Ambonychia radiata. On the Riviere des Hurons, about half 
 way between the Richelieu and the Yamaska, there is another exhibition of 
 the same fossiliferous beds, near the village of St. Jean Baptiste, where, 
 among other forms, Modiolopsis complanata, M. securiformis, and Murchi- 
 sonia Beatrice occur. A third locality is on the east side of Eougemont 
 Mountain, precisely in the strike of a fourth locality at St. Hyacinthe on the 
 Yamaska, where the strata consist of dark greyish-blue argillaceous shales, 
 interstratified with occasional thin layers of limestone. At Turcotte's mills, 
 
 . BKACHIOPODA (H. R.) 
 
 206 
 
 207 
 
 nfflillW 
 
 Wlllllf" 
 
 206. Strophomena Hecuba (Billings). 
 
 207. S. fluctuosa (Billings); a, longitudinal section. 
 
 208. S. nitens (Billings) ; a, longitudinal section. 
 
 l 
 
 lower down the stream, bluish-grey shales are associated with calcareous 
 sandstones. Among the organic remains in these last two localities are the 
 characteristic species, Ambonychia radiata and Trinucleus concentricus. In 
 both places the measures are disturbed by undulations, causing slopes at 
 high angles, sometimes on one side and sometimes on the other ; the strike, 
 which remains pretty uniform, running with the general course of the river. 
 The limited areas of these exposures make it difficult to say what may be 
 the average dip, either in direction or amount. It is not improbable that 
 the Yamaska, the Hurons, and the Richelieu may run upon three parallel 
 anticlinals, so that the spaces between the rivers around the mountains 
 of Rougemont and Rouville would be occupied by somewhat higher strata 
 than those holding the fossils. 
 
 These isolated mountains, with those of Montarville and Monnoir, are intrusive 
 composed of diorites and dolerites, resting on sedimentary rocks at the base, rc 
 and will be described farther on. At Chambly, about half a mile above 
 the fort, there is an interstratified floor of trachyte, similar to tfcat in the 
 
 
 
210 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. X. 
 
 Utica formation, already mentioned on the Chambly canal. At St. Hya- 
 cinthe, a dark colored compact two-feet dolerite dyke cuts the strata: 
 small disseminated crystals of feldspar give a porphyritic character to the 
 rock, and are associated with grains of olivine. 
 
 New York. The two formations which we are tracing, passing out of the province, 
 ascend Lake Champlain and come upon the Hudson River, from which the 
 
 209, 210. BKACHIOPODA (H. K.) 
 
 210 a 
 
 209 a 
 
 209. Lingula Canadensis (Billings) ; a, portion of thf; surface enlarged. 
 210. Orthis occidentalis (Hall) ; a, side, 6, ventral, and c, dorsal view. 
 
 upper portion takes its name. Turning thence to the valley of the Mohawk, 
 the lower formation passes under the town of Utica, from which its title 
 is derived. The two formations reach the shore of Lake Ontario, between 
 Sandy Creek and Oswego, and are next met with on the north shore of 
 the lake, extending between Bowmanville and the river Credit. 
 Lake Ontario. The most eastern exposures of the Utica formation, on the north shore, 
 are just above those of the Trenton already mentioned as occurring to the 
 south of Oshawa, and near to Bowmanville ; both on the south side of the syn- 
 clinal which has been indicated there. An outcrop of some of the strata of 
 the formation is met with on the creek, at Nash's brewery, in the village of 
 Windsor, which is on the twenty-seventh lot of the lake-front range of 
 Whitby ; and at Bowerman's mill, on the thirty-second lot of the third 
 range, a well has been sunk in the formation to the depth of fifty feet. 
 The rock^n this part of the country, as elsewhere, is a dark brownish-black 
 
CHAP. X.] 
 
 UTICA AND HUDSON. FORMATIONS. 
 
 211 
 
 hard brittle and very bituminous shale, which splits into thin laminae. 
 When dried and again wetted, the shale soon cracks and falls to pieces ; 
 so that when exposed to the weather it rapidly decomposes, and at length 
 forms a dark-colored clay, which constitutes a good soil. 
 
 The exposures which have been mentioned are all that are yet known 
 near the lake shore, and they are too few to make the distribution of the 
 formation in this part perfectly intelligible. The dip of the strata in the 
 well at Bowerman's mill has not been ascertained, and it is therefore 
 
 211-213. BRACHIOPOD A (H. K. ) 
 
 211 b a 212 
 
 211. Rhynchonella ? modesta (Conrad) ; a, dorsal, and b, ventral view. 
 
 212. R. JLnticostensis (Billings); a, dorsal, 6, side, and 
 
 c, ventral view. 
 213. R. capax (Conrad) ; a, dorsal, b, side, and c, ventral view. 
 
 difficult to say whether this locality is, like the others, on the south side of 
 the synclinal, or to determine where the base of the formation may sweep 
 round in its progress towards the next known outcrop of the rock, which 
 does not occur until reaching Nottawasaga Bay on Lake Huron. The expo- 
 sures in this bay are seen along the coast, in the third and fourth ranges of 
 Collingwood, and, from the limestone beneath, occupy a breadth of about a 
 mile. The slope perhaps somewhat exceeds the rate which has been given 
 as the average inclination of the subjacent limestone, and the thickness of 
 the deposit is supposed to be between fifty and a hundred feet. 
 
 The Utica formation, both here and at Windsor, is very fossiliferous. 
 Among the species which characterize it, there is a great abundance of 
 Asaphus Canadensis, of which chiefly the tails are preserved. This trilo- 
 bite is accompanied by Triarthrus Becldi, Leptcena sericea, Stropho- 
 mena alternata, Orthis testudinaria, Khynclwnella increbescens, and one or 
 two species of Discina, Orthoceras, and Cytheropsis, which have not yet 
 been named. In Collingwood, the deposit consists of dark brownish-black 
 shales, interstratified with occasional beds of compact brownish limestone, 
 
212 GEOLOGY OF CANADA. [CHAP. X. 
 
 coiungwood. and the shale yields by distillation such an amount of bitumen as to have 
 induced the establishment of a manufactory at Collingwood, for its extrac- 
 tion. Judging from specimens, the strata at Windsor would be equally 
 well adapted for the purpose. Iron pyrites occasionally occurs in some 
 abundance, coating the fossils of this formation. 
 
 Toronto. Between the river Rouge in the township of Pickering on the east, and 
 
 the river Credit in the township of Toronto on the west, sections of the 
 Hudson River formation maybe seen on almost all the intervening streams. 
 
 214-216. BRACHIOPOD A (H. R.) 
 
 a 214 & 
 
 214. Athyris Headi (Billings) ; a, dorsal, and b, side view. 
 
 215. A. dnticostensis (Billings) ; a, dorsal, and 6, side view. 
 
 216. A. borealis (Billings) ; a, dorsal, and 6, side view. 
 
 The formation here consists of a series of bluish-grey argillaceous shales, 
 enclosing bands of calcareous sandstone, sometimes approaching to a 
 limestone, at irregular intervals and of variable thickness. In some 
 instances the bands are of a slaty structure, splitting into thin laminae in 
 the direction of the beds ; in others they have a solid thickness of a foot ; 
 but in few cases do they maintain either character for any great distance. 
 The sandstones, while in the beds, are hard and solid, and upon fracture 
 exhibit a grey color, with much of the appearance of limestone ; but by long 
 exposure to the weather they turn to. a dark brown, and ultimately crum- 
 ble and decay. These sandstones generally abound in calcareous fossils, 
 which in some places predominate so as to give rise to beds of impure 
 limestone ; these beds are, however, rare. A workable limestone bed of 
 this kind, in the vicinity of Toronto, would be of great value, as the stone 
 yielding the lime for the consumption of the city is at present transported 
 from some distance. The slaty variety of the sandstones is well adapted 
 for nagging, and, by a careful selection, some of the arenaceous bands 
 may yield abundance of good building material, but the stone cannot be 
 said to be generally adapted for the purpose. 
 
CHAP. X.] UTICA AND HUDSON FORMATIONS. 213 
 
 The banks of the Credit, the Etobicoke, the Minaco, the Humber, and 
 the Don, for certain distances from the lake shore, expose sections exhibit- 
 ing sixty feet or more of these strata ; but advancing northward, the forma- 
 tion becomes concealed by the great accumulation of drift, of which the 
 interior of the country is composed. At Weston on the Humber, near to number, 
 the townships of Etobicoke and York, some good limestone occurs ; and at 
 Fisher's mill, below Dundas Street, on the same river, there is more of 
 
 217. LAMELLIBRAKCHIATA (H. K.) 
 
 217. Modiolopsis modiolaris (Conrad). 
 
 the same material. At the latter place, the banks of the stream rise to a 
 height of more than a hundred feet, of which from fifty to sixty are com- 
 posed of the Hudson River shales and sandstones, while the upper part 
 consists of sand and gravel. 
 
 Most of the localities named abound in the characteristic fossils of the 
 formation. On the Don, some thin calcareous beds are almost a mass of Don. 
 Leptcena sericea, which is accompanied by Khynchonella modesta, Ambony- 
 chia radiata, and Modiolopsis modiolaris. On the Humber, Orthoceras 
 crebriseptum occurs in great abundance, and among other species are 
 Stenopora fibrosa, 8. petropolitana, columns of G-lyptocrinus, Leptcena 
 sericea, StropTiomena alternata, Rhynchonella increbescens, Avicula demissa, 
 Ambonychia radiata, Modiolopsis modiolaris^ and Lyrodesma poststriata. 
 On the Credit, in addition to many of the preceding species, are found an 
 undetermined Tetradium and Favistella stellata. 
 
 Escaping from beneath the great mass of drift, which conceals the for- 
 mation between Lake Ontario and Lake Huron, the whole thickness of 
 the deposit can be determined on the east side of the township of Colling- 
 wood, where it rises, in nearly horizontal strata, to the height of 770 feet, 
 in the flank of a hill overlooking the Utica shales, which have been men- 
 tioned as exposed at the level of the lake . Farther on , the deposit shows itself 
 near Cape Boucher in Nottawasaga Bay, where cliffs, rising abruptly to the 
 height of about 150 feet, present sections of buff or drab-colored argil- 
 laceous shale, interstratified with thin beds of grey yellow-weathering 
 sandstone. The formation next makes its appearance at Point Rich, and 
 
214 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. X. 
 
 continues exposed in a high, and nearly vertical cliff to Point William, 
 where we find bluish and drab argillaceous shales, with thin beds of lime- 
 stone and calcareous sandstone, in a precipitous hill, which slopes back 
 from the vertical part. The strata are piled on one another to the height 
 of 335 feet over the lake, and they are capped by twenty feet of red and 
 bluish-green clays, with an occasional band of harder rock : these belong 
 to the succeeding formation. 
 
 Exposures of Hudson River strata occur on the road between conces- 
 sions B and C of Sydenham, from -the sixteenth to the twenty-third lot, 
 
 218. LAMKLLIBRANCHIATA (H. K.) 
 
 218. Cyrtodonta Hindi (Billings) ; a, dorsal, and 6, side view. 
 
 having between them and the lake a long outlier of the succeeding forma- 
 tion, which there constitutes a considerable hill. On the lake side of the 
 hill, no Hudson River strata have been observed ; but the. summit of this 
 formation is supposed to occur at the margin of the water, about three miles 
 Owen Sound, below the town of Owen Sound, and to cross thence to the opposite side of 
 the bay, where Hudson River strata are seen at intervals to Cape Commo- 
 dore. They are met with also on the islands opposite to Colpoy's Bay, 
 at Cape Crocker and Point Montresor, as well as Barrier Island, but higher 
 formations occupy the remainder of the coast to Cabot's Head. If a 
 straight line were drawn from Point Boucher to Point Rich, to represent 
 the outcrop of the base, the formation would have a breadth of about 
 
CHAP. X.] 
 
 UTICA AND HUDSON FORMATIONS. 
 
 215 
 
 seventeen miles at Owen's Sound ; which, at the supposed slope of thirty 
 feet in a mile, would give a thickness of about 500 feet. 
 
 In some of the beds at Point Boucher concretionary nodules of calcspar point Boucher 
 are observed, and similar nodules at Point Rich are associated with others 
 of orange-red gypsum and of heavy spar. These occur also at Cape Com- 
 modore, but no masses of the gypsum of a workable description have been 
 
 219, 220. LAMELLIBRANCHIATA (H. B. ) 
 
 220 
 
 219. Ambonychia radiata (Hall). 
 220. JLvicula demissa (Conrad). 
 
 met with. The 'materials of economic importance presented by the strata 
 along the coast, are confined to stone for building, for tiles, and for flag- 
 ging, with occasional beds of limestone fit for burning into lime. 
 
 Fossils in great abundance, but unequally distributed, are found in the 
 formation in this region. In the section near Point Boucher, some of the 
 sandstone surfaces are marked by G-raptolithus mucronatus ; but the 
 organic remains consist chiefly of columns of different species of crinoids. 
 Testacea are rare, those observed being confined to a few specimens 
 of Ambonycliia radiata, Modiolopsis modiolaris, Rhynchonella modesta, 
 StropJwmena alternata, S. filitexta, and one or two undetermined bivalve 
 shells, with Stenopora fibrosa, and a species of Asaplius. At Point Eich, Point men. 
 and thence gradually rising in the strata, to Point William, testacea 
 are more plentiful, but not in great abundance. The most numerous fossil 
 is Orthoceras crebriseptum, which is accompanied by /Stenopora fibrosa, 
 S. petropolitana, and a species of Petraia, Leptcena sericea, Strophomena 
 alternate S. filitexta, Orthis lynx, 0. ocddentalis, Rhynchonella modesta, 
 Ambonychia radiata, Modiolopsis modiolaris, Avicula demised, two species 
 
216 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. X. 
 
 Manitoulin 
 si and. 
 
 of Cyrtodonta, three species of Murchisonia^ Belter ophon ornatus, and 
 Orthoceras bilineatum. At Cape Commodore, which is higher in the 
 series, there occurs, with most of these, Avicula elliptica ; and at Cape 
 Crocker and Point Montresor, on the same horizon as Cape Commodore, 
 nearly all the species above named are met with in great abundance. 
 
 The next exposures of the two formations under description occur on the 
 east end of the Great Manitoulin Island, and on some of the small islands 
 adjacent. The Utica formation presents itself at Cape Smyth, on the 
 
 221-224. LAMELLIBKANCHIAT A (H. K.) 
 
 221 222 
 
 224 
 
 221. Ctenodonta Iphigenia (Billings). 
 222. Lyrodesma poststriata (Emmons). 
 223. Cleidophorus 1 several small species. 
 224. Orthonota parallela (Hall) ? 
 
 east side of Wequamekong Bay. It has here a breadth of about a mile, 
 at the point of the Cape, and, with a similar breadth, follows the Trenton 
 formation across the neck of the promontory between Wequamekong and 
 Manitouwaning Bays. It appears again at the southern extremity of 
 Shequenandod Island, and forms- a small island in Shequenandod Bay. 
 Entering upon the west side of the bay near the village of Shequenandod, 
 it crosses to Beaufort Bay, resting unconformably on the south side of a 
 quartzite ridge of the Huronian series, near the village, and on the Trenton 
 limestone, as it enters the latter bay. Where these shales rest on the 
 Huronian rocks, the beds are slightly turned up at the outcrop, dipping 
 S. < 15 ; but this dip does not extend above two chains from the ridge, 
 beyond which the strata again become nearly horizontal. Beyond Beaufort 
 Bay, the shales run along the south side of the small island north of Maple 
 Point on the Great Manitoulin, which has already been alluded to, where 
 they rest on the Trenton beds. From Cape Smyth to this position, the 
 thickness of the deposit does not anywhere exceed about fifty feet. 
 
CHAP. X.] UTICA AND HUDSON FORMATIONS. 217 
 
 Some of the beds of the formation in this part are more than usually cape Smyth, 
 bituminous, and on the island north of Maple Point a spring of petroleum 
 rises from them. At Cape Smyth, the usual very bituminous black 
 shales of the formation are interstratified with a few bands of a less 
 bituminous character, grey in color, and with an occasional thin layer of 
 brownish limestone. These contain, in great abundance, a few species of 
 fossils, consisting of Orthis testudinaria, Pleurotomaria Hebe, P. Artemis, 
 
 225, 226, GASTEROPODA (H. K.) 
 
 225 
 
 225. Cyclonema bilix (Conrad). 
 226. Cyrtolites ornatus (Conrad). 
 
 and P. tennis, with columns of Heterocrinm. At Shequenandod, the pre- 
 vailing species belong to G-raptoliihus and Orthoceras ; while on the 
 islands off Maple Cape the only species observed are orthoceratites, with 
 Triarthrus Beckii, which is met with at all the localities. 
 
 Between the Maple Cape Islands and the island of St. Joseph nothing St. Joseph, 
 more is seen of the Utica formation before reaching one or two small islands 
 off the east coast of St. Joseph. Though much covered with drift on 
 this latter island, there are indications on the two sides of it that the band 
 passes across in a due east and west course, nearly opposite to the southern 
 point of Neebish Island, whence it strikes into the northern peninsula of 
 Michigan in the bight of Mud Lake Bay. 
 
 More than half way across from Cabot's Head to the Great Manitoulin, 
 the Hudson River formation constitutes the strata of Lonely Island, which 
 rises to a considerable height. It forms also an island about four or 
 five miles farther west, as well as Rabbit Island about three miles beyond, 
 where bluish argillaceous shales are interstratified with thin bands 
 of grey drab-weathering limestone and calcareous sandstone. Among 
 their fossils we find for the first time, Beatricea undulata, which is accom- 
 panied by Favistetta stellata, Ambonychia radiata, Vanuxemia amyg- 
 dalina, Pleurotomaria Americana, and Orthooeras bilineatum. 
 
 These beds belong to the upper part of the deposit, but it is not certain 
 how far they may be from the summit. The base of the Hudson 
 River formation is seen resting on the Utica shales at Cape Smyth ; so that 
 the breadth of the formation in this part is at least nine miles, and the 
 thickness about 300 feet. At Cape Smyth, the deposit consists of bluish 
 
218 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. X. 
 
 and greenish argillaceous shales interstratified with grey drab-weathering 
 calcareous sandstone, and abounds in fossils, many of them well preserved. 
 Twenty-six species have here been met with : among them are Tetradium 
 fibratum, Stenopora fibrosa, Favistella stellata, undetermined species of 
 Petraia and Stromatopora, Leptcena serieea, Stropliomena alternata, 8. 
 filitexta, Orthis lynx, 0. occidentalis, 0. insculpta, Ehynchonella modesta, 
 R. recurvirostra, -Modiolopsis modiolaris, Avicula demissa, undetermined 
 species of Orthonota and Oyrtodonta, Pleurotomaria Americana, P. 
 Helena, Cyelonema Ulix, an undetermined Murchisonia, Orthoceras 
 bilineatum, 0. crebriseptum, and an undetermined Asaplius. 
 
 227, 228. CEPHALOPODA (H. K.) 
 
 227 
 
 22 1. Jlscoceras Canadensis (Billings). 
 228. Orthoceras crebriseptum (Hall). 
 
 Proceeding westward, a high and bold escarpment marks the lower part 
 of the formation between Wequamekong and Manitouwaning Bay, as well 
 as on the west side of the latter bay. It is continued south of Shequenan- 
 BeaufortBay. dod Bay, and farther to Beaufort Bay, while a depression, overlooked by 
 the escarpment of a more recent rock, follows the summit from Manitoulin 
 Gulf to Manitouwaning, thence to the north part of Tecumseth Lake, and 
 farther to the upper part of Beaufort Bay. In this part of its range, the 
 Hudson River formation, gradually narrowing, diminishes in volume, and 
 south of Lacloche Island its thickness probably does not exceed 200 feet. 
 
CHAP. X.] UTICA AND HUDSON FORMATIONS. 219 
 
 Between Beaufort Bay and Bayfield Sound, the same formation composes 
 all the north side of the Great Manitoulin, with a breadth of five or six 
 miles south from Maple Point. It also forms Barrie Island and the northern 
 salient points of the Great Manitoulin beyond, Cape Robert being the most 
 conspicuous. It constitutes also the northern capes of Cockburn Island, 
 and nearly one half of the north and south breadth of Drummond Island. Island 
 North of Drummond Island, the base reaches Sulphur Island, where it 
 
 229. '-Asaphus platycephalus (Stokes). 
 230. Proetus Alaricus (Billings). 
 231. Cheirurus Icarus (Billings). 
 
 abuts against the Huronian quartzites. Farther westward, it underlies 
 rather less than the southern half of the island of St. Joseph, striking 
 thence into the northern peninsula of Michigan. 
 
 In describing the distribution of the Trenton group of limestones, allusion Ottawa out- 
 has already been made to the occurrence of the Utica and Hudson River liers - 
 formations in those outlying patches of Lower Silurian strata which occur 
 in the northern division of the great basin which occupies the country be- 
 tween the Ottawa and the St. Lawrence. Enough has been said to indicate 
 the position of these outliers. The two smaller patches, one lying in Clarence 
 and Plantagenet, and the other in Cumberland, consist wholly of the Utica 
 formation. The third and largest, a part of which touches the city of 
 Ottawa, though chiefly composed of the same formation, presents a set of 
 grey brownish-weathering calcareous sandstones, obscurely exposed in the 
 north-eastern part of Russell, and extending from the twelfth to the twenty- 
 first lots of the second and third ranges. These sandstones are marked by 
 Strophomena altemata, Athyris Headi, AmbonycJiia radiata, Modiolopsis 
 modiolaris, and Calymene senaria, the chief part of which clearly show 
 these strata to belong to the Hudson River formation. To the northward 
 of them, red shale is met with between the twenty-first and twenty- 
 second lot of the third range. Red shale occurs also in the rear of the 
 fourth lot of the eighth range of Osgoode, probably connected with the 
 shale of Russell; but the rocks in this part are so covered with drift. 
 
220 GEOLOGY OF CANADA. [CHAP. X. 
 
 that the complete distribution of the Hudson River strata, and their rela- 
 tion to the red shales, have-not yet been made out. The fossils of the Utica 
 shales in this region are several species of G-raptolithus, Leptcena sericea, 
 Strophomena alternata, Orthis testudinaria, undetermined species of 
 Lingula, Otenodonta and Orthoceras, Asaphus Canadensis, Triarthrus 
 BecJcii, and T. spinosus. 
 
 Saguenay, The trend of the Utica formation on the south side of the Lower Silurian 
 
 trough of Lake St. John, has been given in tracing the distribution of the 
 Trenton limestone. The apparent flatness of the trough makes it probable 
 that the formation may occupy a zone of some two or three miles wide, 
 chiefly under the waters of the lake, surrounding a considerable nucleus of 
 the Hudson River deposits. The Utica formation on the lake, in every 
 observed exposure, consists of the usual black and strongly bituminous 
 shales, lying in beds from a sixteenth to an eighth of an inch thick, 
 and the whole mass is estimated to be about a hundred feet. The 
 change from the limestones below them is sudden, there being no inter- 
 stratification of calcareous layers at the base. From a quarter to half 
 an inch at the bottom is filled with fragments of crinoidal columns, which, 
 being white, give to the layer a dotted grey aspect, and supply it with 
 calcareous matter. Graptolites abound in the beds: among them is 
 G-raptolithus mucronatus, and there are probably some undescribed species. 
 Dictyonema occurs, and among the fossils are also Discina filosa, D. lamel- 
 losa, an undetermined Lingula, with several new species of Orthoceras 
 and Triarthrus Beckii. 
 
 The only spot on Lake St. John where the Hudson River formation is 
 met with is at Snake Island, where there occurs an argillaceous yellow- 
 weathering limestone, of which only a small exposure has been seen in 
 place. The island, which is about a mile long and a furlong wide, is 
 covered with fragments of the same kind, and from those around the island 
 a considerable collection of good fossils has been obtained, some of the 
 forms among which are characteristic of the Hudson River formation. 
 Among the fossils are Beatricea undulata, Petraia corniculum, Ptilodictya 
 acuta. Holy sites catenulatus, Orthis occidentalis, a large variety of 0. 
 lynx, 0. testudinaria, Athyris ITeadi, Rhynchonella increbescens, and Am- 
 lonychia radiata. 
 
 It has been stated in a previous chapter that the highest rocks of the 
 Mingan Islands belong to the Birdseye and Black River formation. The 
 measures there dip towards the island of Anticosti, which is to the south of the 
 Mingan group, with an average slope of about ninety feet in a mile. 
 
 Anticosti. Much higher deposits in Anticosti stand very much in the same attitude, 
 and it is therefore presumed that this slope of the strata is preserved 
 in the bottom of the intermediate channel, which is nineteen miles 
 across. The thickness of the intervening strata would -thus be about 
 
CHAP. X.] UTICA AND HUDSON FORMATIONS. 221 
 
 1700 feet. This volume probably consists of the upper part of the Birds- 
 eye and Black River, with the Trenton, the Utica, and the lower part of 
 the Hudson River formation ; what is considered the upper part of the 
 latter, being the first rock met with on the north side of Anticosti. 
 
 Loose fragments of black strongly bituminous graptolitic shales, in every 
 way resembling those of the Utica formation, and of some of the interstratified 
 beds of the Hudson River, are met with on the beach on the north side of 
 Anticosti. These are probably washed up in storms, or pushed up by the 
 ice, from the intermediate channel, and seem to offer some evidence that 
 the Utica formation, and the Hudson River, in its lower portion, have con- 
 tinued to preserve the aspect which they present near Quebec. The portion 
 of the Hudson River formation which is seen on the island, has however a 
 character differing in some degree from that which it possesses elsewhere 
 in Canada ; the strata being much more calcareous, and containing several 
 new organic forms. 
 
 The following ascending section, obtained at the western end of the Ascending 
 island of Anticosti may be taken as representing the measures : 
 
 Ft. in. 
 
 Grey limestone beds of two and three inches thick, interstratified with 
 greenish shale. The limestone beds are in peaces filled with fossils in 
 patches of from two to three feet in diameter, while no fossils are 
 observed in the same bed for? considerable intervals. The limestone is 
 hard and compact, and the fossils are in consequence with difficulty 
 got out ; among them are Stenopora fibrosa, Leptcena sericea, 
 Strophomena nitens, S. fiuctuosa, S. planumbona, Orthis subquadrata, 
 Rhynchonellarecurvirostra, R. Jlnticostensis, Athyris Headi, Murchisonia 
 multivolvis, M. rugosa, Orthoceras xiphias, and Asaphus platycephalus, 44 
 
 Grey limestones and shales of a similar character, with the addition of 
 interstratified layers of conglomerate limestone of two or three inches 
 thick, in which the pebbles consist of grey limestone and greenish 
 shale, and measure more in the plane of the beds than transversely to 
 them ; the diameter of the largest is about three inches. The pebbles 
 lie in a grey argillaceous matrix, 25 6 
 
 Grey limestones, shales, and conglomerates as before. This part is very 
 fossiliferous, and among the remains are Stenopora fibrosa, Leptcena 
 sericea, Strophomena nitens, S. fiuctuosa, S. planumbona, Orthis sub- 
 quadrata, Rhynchonella recurvirostra, R. Anticostensis, Athyris Headi, 
 Obolus Canadensis? Ambonychia radiata, Cyrtodonta sigmoidea, C. 
 obtusa, Murchisonia gracilis, M. varians, M. multivolvis, M. rugosa, M. 
 modesta,Pleurotomaria Americana, Orthoceras formosum, O. balteatum, 
 0. xiphias, O.Anticostense,AscocerasCanadense,Asaphus platycephalus, 10 
 
 Grey argillaceous limestone interstratified with greenish argillaceous shale; 
 in these beds fossils are not so numerous, but they contain, among 
 other species, Stenopora fibrosa, Favosites Gothlandica, Strophomena 
 planumbona, Obolus Canadensis, Murchisonia modesta, M. gracilis, M. 
 varians, Pleurotomaria Americana, Orthoceras xiphias, Asaphus platy- 
 cephalus, Cheirurus pleurexanthemus, with undescribed species of 
 Encrinurus and Dalmanites, 63 
 
222 GEOLOGY OF CANADA. [CHAP. X. 
 
 Ft. in. 
 
 Grey argillaceous limestone and greenish argillaceous shale, similar to the 
 last; interstratified with beds of pure limestone and of limestone con- 
 glomerate. In different parts of the measures up to this point, besides 
 the fossils already mentioned, there occur Halysites catenulatus, Jlm- 
 bonychia ungulata, Cyrtodonta obtusa, Jlsaphus obtusus, Cheirurus 
 1 Icarus, Illeenus grandis, I. orbicaudatus, and the following unde- 
 scribed species, 1 of Ptylodictya, 1 Heliopora, 4 Cyrtodonta, 1 Modio- 
 lopsis, 1 Orthonota, 1 Avicula, 1 Pleurotomaria, 1 Bellerophon, 1 Cyr- 
 tolites, 1 Metoptoma, 2 Orthoceras, 86 
 
 Bluish-grey hard brittle argillo-calcareous bed, smooth on the surface, 
 with remarkable impressions like the track of an animal, consisting 
 of two parallel rows of semicircular pits, each pit about half an inch 
 broad ; the one row separated from the other about half an inch, and so 
 arranged that the curves of the pits are on the outside, while the centre 
 of each pit is opposite the interrupted circumference of two pits on 
 the other side. The bottoms of the pits on opposite sides slope away 
 from one another, leaving a species of ridge between them. These 
 double rows of alternate pits are usually from about ten to about 
 eighteen inches long, and are more deeply impressed at one extremity 
 than at the other ; the impressions are so numerous on some parts of 
 
 the surface that scarcely a square yard is without them, 06 
 
 229 
 
 Bluish-grey somewhat argillaceous limestone, in hard and compact beds of 
 
 from three to six inches thick, interstratified with partings of green 
 shale. Towards the top there are oands of light reddish-grey lime- 
 stone, rather purer than those below. Some of the bands contain 
 fragments of trilobites, and other fossils, of which it is difficult to pro- 
 cure good specimens from the hardness of the rock ; the surfaces of 
 some of the beds show fucoids, 50 
 
 Grey limestone beds of from three to six inches, with shale partings be- 
 tween, much like the preceding in character ; the top bed contains 
 numerous beautiful specimens of corals of a pure yellowish-white 
 color, standing out in relief on the surface. The corals are F'avosites 
 Gothlandica, and an undetermined species of Stromatopora, 50 
 
 Reddish-grey limestone in thin beds, holding on the top the characteristic 
 
 species Cyrtodonta sigmoidea, 20 
 
 Reddish-grey limestone beds, with thin greenish shale partings; interstrat- 
 ified, at intervals of from three to ten feet, with beds of from three to 
 six inches, consisting of a conglomerate, the pebbles of which are com- 
 posed of grey limestone, and are of various sizes, up to three inches 
 in diameter, lying flat in a matrix of grey limestone. Many 
 fragments of trilobites are met with in the deposit, with other fossils, 
 among which are Cyrtodonta sigmoidea and the same undescribed 
 Metoptoma as before, 25 
 
 Reddish-grey limestones, conglomerates, and shale partings as before, ... 88 
 
 Reddish-grey limestones in beds of from six to ten inches, interstratified 
 with conglomerates as before. The fossils which these beds contain 
 are Stenopora fibrosa, S. mammillata, Favosites Gothlandica, Halysites 
 catenulata, Leptcena sericea, Strophomena Ceres, Orthis subquadrata, 
 Rhynchonella recurvirostra, R. capax, Lingula quadrata, Obolus Cana- 
 densis ? Pleurotomaria Helena, Murchisonia rugosa, Subulites Richard- 
 soni, Orthoceras balteatum, Jlsaphus platycephalus, and an undescribed 
 Harpes. Towards the top Beatricea undulata occurs in abundance,. . 102 
 
CHAP. X.] UTICA AND HUDSON FORMATIONS. 223 
 
 Ft. in. 
 
 Grey limestones, conglomerates, and shale partings, with similar fossils. 
 
 A bed at the top contains an undescribed species of Dendrocrinus, . . . 82 
 
 Grey limestones, conglomerates, and shale partings, with fossils as before,. 33 
 
 Grey limestones, conglomerates, and shale partings as before ; in addition 
 to Beatricea undulata and other fossils similar to those already men- 
 tioned, a considerable number of orthoceratites are present, 64 
 
 Grey limestones, conglomerates, and shale partings ; in addition to fossils 
 previously named, there is a greater abundance of spiral univalves, 
 chiefly Murchisonia gracilis ? than in any of the beds lower down, . . . 165 
 
 Measures concealed ; supposed from fragments observed on the beach to be a 
 greenish-grey argillo-arenaceous shale, or, from the character of beds 
 occupying an equivalent place in another part, a greenish-grey fine 
 grained slightly calcareous sandstone, 
 
 959 
 
 These beds occupy nearly the whole length of Anticosti on the north 
 side, extending from the west-end light-house to Fox Point, within about 
 fourteen miles of the eastern extremity of the island, the distance being 130 
 miles. They dip inland, with a slope of about ninety feet in a mile, and 
 present to the sea an escarpment divided into a set of transverse ridge-like 
 elevations of from 200 to 500 feet above high-water mark, separated by 
 depressions, which gradually rise to the general surface of the country 
 behind. From English Head, three miles east from the west end, to 
 West Cliff, a distance of fifty-three miles in, a straight line, each successive 
 ridge, from valley to valley, occupies a base of from four to six miles. The 
 ridges present somewhat rounded ends, facing the sea. Their rise is first 
 well marked at from a quarter of a mile to a mile from the shore ; and 
 about a mile farther inland they attain their greatest elevation. Among 
 these, Macasty Mountain, eleven miles east from the west end, rises up- 
 wards of 400 feet at about a mile inland. High Cliff, eighteen miles farther, 
 attains probably 500 feet, at a quarter of a mile from the shore. These 
 are the most conspicuous ridges. High Cliff is a bold headland, while 
 Macasty Mountain is separated by a broader valley than usual from its 
 neighbor to the east, and is higher than any other to the west. 
 
 West Cliff rises immediately over the sea to an elevation of between 200 
 and 400 feet. Charleston Point has an elevation of 100 feet over the 
 sea, and a quarter of a mile inland rises to between 300 and 400 feet. 
 Observation Cliff, which is twenty miles beyond, rises rapidly to 350 feet ; 
 and from this cliff to Fox Point, a distance of about fifty miles, the cliffs 
 become more prominent on the coast, rising almost perpendicularly at the 
 points, to heights of from 100 to 300 feet, while the indentations are more 
 numerous, producing more sharply defined valleys. The breadth which 
 the formation occupies, for about two thirds of the whole distance from the 
 west end, is between four and five miles, but it gradually diminishes 
 
224 GEOLOGY OF CANADA. [CHAP. X. 
 
 towards the east end. The summit of the formation to the westward is at 
 Junction Cliff, which is on the south side of the island, about four miles 
 from the extremity. 
 
 The peculiarly marked track-bed, 229 feet from the base of the section, 
 enters upon the land near the west end, at Otter or Indian Cove, and 
 finally comes out again upon the coast at Observation Cliff, the distance 
 being eighty-two miles, establishing a general strike of S. 81 E. Near 
 West cuff; West Cliff, two trap dykes occur on the beach. One of them, about half a 
 Trap dykes, mile west of the cliff, with a breadth of about twenty yards, is visible for 
 120 yards in a bearing N. 62 W. ; the other, close by the base of the cliff, 
 with a breadth of fifty yards, is seen for about twenty yards in the bearing 
 N. 47 W. Both dykes are composed of fine-grained greenstone, with 
 white feldspar and black hornblende, and neither appear to produce any 
 disturbance of the strata. 
 
 Proceeding eastward along the escarpment, from English Head, the 
 fossils which characterize the strata do not vary much from those given 
 in the section. In addition to most of these, there are met with at Charles- 
 ton Point, Carabocrinus tuberculatus, Dendrocrinus latibrachiatus, Pleuro- 
 cystites Anticostensis, Palasterina rugosa, Ptilodictya lanceolata, Stropho- 
 mena Ceres, Murchisonia turretiformis, M. ramosa, Pleurotomaria Progne, 
 Orthoceras Anticostense, 0. magnisulcatum, Nautilus Hercules, and 
 Proetus Alaricus. No specimens of Beatricea undulata, which occurs 
 188 feet over the track-bed at the west end, are met with until reaching 
 Cape Henry, where their vertical height above the track-bed is twice 
 as great as hi the section. The position at the base of the escarpment 
 equivalent to that bed in the section which holds Beatricea, would be 
 about the third of a mile eastward of Bear Head ; but as the coast line 
 here takes a turn more transverse to the strike than elsewhere, a bed 
 holding that fossil may have been passed over without observation. East: 
 of Salmon River, a cliff of about sixty feet in height presents itself, in> 
 Battery which the prostrate forms of this tree-like fossil protrude from the cliff 
 Pomt. ^ ^j ers ^ eac h fossil presenting a circular extremity, with an orifice in the 
 centre, giving the cliff the aspect of a battery of guns, which has led to the 
 name of Battery Point. 
 
 On the south side of the St. Lawrence, black graptolitic shales belonging 
 Gasps to the Hudson River formation, occur in several places in Gaspe*, be- 
 tween Cape Rosier and the Marsouin River. These will be farther alluded 
 to, in describing the rocks which are in contact with them to the south. 
 
CHAP. XI.J GEOLOGY OF CANADA. 225 
 
 CHAPTER XI. 
 
 THE QUEBEC GROUP. 
 
 LEVIS FORMATION. SECTION AT ORLEANS ISLAND ; MAGNESIAN SHALES AND LIMESTONES ; CON- 
 GLOMERATES; GLAUCONITE BEDS; GRAPTOLITIC SHALES; SlLLERY SANDSTONES AND RED 
 
 SHALES. POINT LEVIS ; FOSSILS. AGE OF THE GROUP ; DISLOCATION AND OVERLAP. 
 LOWER BLACK SHALES AND LIMESTONES; THEIR DISTRIBUTION. FARNHAM ; FOSSILS. 
 RICHMOND. DISTRIBUTION OF THE QUEBEC GROUP; ANTICLINALS AND SYNCLINALS; ST. 
 FLAVIEN ; SOMERSET ; DRUMMONDVILLE. ACTON ; COPPER ORES ; MILTON ; GRANBY. 
 METAMORPHIC ROCKS; EPIDOTIC, CHLORITIC, SPECULAR AND COPPER-BEARING SCHISTS; 
 SERPENTINE; ANORTHOSITES. ORFORD AND SUTTON MOUNTAINS. LAKE MEMPHRAMAGOG ; 
 STOKE MOUNTAINS. CHAUDIERE RIVER; L'lSLET; RIVIERE OUELLE; KAMOURASKA; Ri 
 MOUSKI; RIVER CHATTE; SHICKSHOCK MOUNTAINS; MARSOUIN, STE. ANNE, AND MAG- 
 DALEN RIVERS; CAPE ROSIER; BAY CHALEUR; CAPE MAQUEREAU; METAMORPHIO ROCKS. 
 MISSISQUOI BAY; PHILLIPSBURG ; HIGHGATE; BELLEISLE; NEWFOUNDLAND. 
 
 In the western portions of Canada, the Hudson River formation is suc- 
 ceeded by the Medina sandstone of the New York geologists ; and to the 
 south of Three Rivers, on the St. Francis and the Nicolet, red slates^ 
 described in the previous chapter, occupy a similar position, and probably 
 correspond to the red slates of the Medina formation. In the immediate 
 vicinity of Quebec however, the graptolitic shales which belong to the 
 Utica and Hudson River formations, are followed by a series of rocks, 
 which are not met with to the west in the same relations. Although from 
 their geographical position apparently superior to the Hudson River for- 
 mation, these rocks belong in reality to an older group, which is devel- 
 oped to a great extent hi eastern Canada, and presents somewhat differ- 
 ent characters in the various parts of its distribution. The rocks of this 
 series are still under examination, and the descriptions now given may 
 hereafter require to be somewhat modified. As these strata have been 
 more particularly studied in the neighborhood of Quebec, they have been 
 designated by the name of the Quebec group, which is divided into the 
 L^vis and Sillery formations. 
 
 At the upper end of the island of Orleans, on the north-west side, between Orleans 
 high and low water marks, there are exposed about 500 feet of black grap- Idand - 
 tolitic shales, such as belong to the Utica and Hudson River formations, 
 dipping S. E. < 50 ; resting upon which, is a series of different strata, 
 dipping in the same direction, and at the same angle with them ; the con- 
 tact between the two being visible. After a short distance across the 
 
 p 
 
226 
 
 GEOLOGY OF CANADA. 
 232-234 . BRTOZOA . 
 
 [CHAP. XI 
 
 232. Graptolithus octobrachiatus (Hall) ; scale one half. 
 
 233. G. bryonoides (Hall) ; natural size. 
 
 234. G. Logani (Hall) ; a, scale one half; 6, natural size, 
 
CHAP. XL] 
 
 QUEBEC GROUP. 
 
 227 
 
 measures, undulations occur. The effect of these on the distribution of 
 the beds has been partially ascertained, round the upper end, to the 
 south-east front of the island, and for several miles along it. The fol- 
 lowing is the sequence of the strata: the beds are, however, in some 
 places so corrugated and broken that the measurements here given can 
 only be taken as rude approximations to the truth : 
 
 Feet. 
 
 Levis for- 
 mation. 
 
 Magnesian 
 shales. 
 
 Dolomitic 
 conglom- 
 erates. 
 
 1. Green calcareo-magnesian shale, weathering to a yellowish or 
 
 reddish-brown, interstratified with thin bands of purplish-grey 
 argillaceous shale. Some of the magnesian shales are nearly grass- 
 green, and the surfaces of most of the green beds are marked with 
 fucoid-like forms of purplish-grey; the green shales hold about 
 twenty per cent, of dolomite. The mass is strong, and offers con- 
 siderable resistance to wearing influences, 100 
 
 2. Grey argillaceous shale, much softer than the magnesian shale,. . . 100 
 
 3. Grey limestone conglomerate ; the rounded masses are chiefly of 
 
 grey limestone ; the matrix in many parts weathers to a brown- 
 ish color, and is probably dolomitic. Fossils occur, some of them 
 replaced by silica, but those as yet obtained in this locality are 
 too obscure to be determined 5 the band in some parts appears to 
 break into lenticular patches, 10 
 
 4. Green yellow-weathering calcareo-magnesian shale, with grey 
 
 argillaceous bands of the same character as 1, 100 
 
 5. Grey soft argillaceous shale, 200 
 
 6. Yellowish-grey dolomite, weathering orange-brown. It holds occa- 
 
 sional *masses of ash-grey limestone, and in some parts of its 
 thickness a multitude of pebbles of quartz as large as peas, 
 and becomes towards the top a dolomitic sandstone, 70 
 
 7. Grey fine soft argillaceous shale, with compound graptolites (Phyl~ Graptolitic 
 
 lograptus typus) about thirty feet from the summit, 170 
 
 8. Grey limestone conglomerate ; the matrix in some parts weathers 
 
 to a reddish-brown, being dolomitic, and contains large concre- 
 tions of carbonate of lime in concentric fibrous layers like traver- 
 tine. The band holds fossils in some places, 35 
 
 9. Grey fine soft shale, with occasional bands of sandstone weathering 
 
 brownish, none of them over six inches ; the bands of sandstone 
 increase in number towards the top, 500 
 
 10. Olive-green argillaceous shale, striped with purplish-grey bands,.. 700 
 
 11. Olive-green arenaceous shale, with disseminated soft grains of a 
 
 green mineral, resembling glauconite, and approaching it in 
 composition. In the upper part of the deposit, the shale contains 
 so much grit as to become almost a sandstone ; and within about 
 100 feet of the top, it assumes a red color, in one or two bands, 400 
 
 12. Yellowish- white limestone conglomerate; the matrix assumes a 
 
 dolomitic aspect in some parts ; the rounded masses or boulders 
 are occasionally one or two feet in diameter, and some parts of 
 the bed hold fossils, 10 
 
 13. Grey, drab-weathering sandstones, in general slightly calcareous, 
 
 interstratified with grey argillaceous shales ; some of the sand- 
 stone beds towards the bottom are three or four feet thick, and 
 hold occasional calcareous pebbles. The sandstones become thin- 
 ner ascending, and then the shales prevail ; but these become by 
 
 Glauconite 
 beds. 
 
 Grey sand- 
 stones. 
 
228 
 
 GEOLOGY OF CANADA. 
 
 235-238. BKYOZO A. 
 
 [CHAP. XI. 
 
 2B5.Gra,ptolithusJlexilis (Hall) ; scale one half. 
 
 236. G. Headi (Hall) ; scale one half. 
 
 ZBl.Phyllograptus angustifolius (Hall) ; natural size. 
 
 238. P. i typus (Hall) ; a group of twelve, natural size, 
 
CHAP. XL] QUEBEC GROUP. 229 
 
 Feet. 
 
 degrees, more and more arenaceous, and a band or two, about 200 
 feet from the top, assumes a red color, 400 
 
 14. Grey limestone conglomerate ; the matrix, weathering to a brown 
 
 in some parts, is probably dolomitic, 30 
 
 15. Grey drab-weathering sandstones and shales, the sandstones slightly 
 
 calcareous, 300 
 
 16. Dark grey and green shales, with thin bands of grey quartzite, and Dark shales 
 
 occasional thicker beds of drab-weathering sandstone, some of and quartzites. 
 
 them being lenticular masses ; the dark shales appear in some 
 parts to pass into black, 900 
 
 17. Red and green shales, the red prevailing, interstratified with occa- 
 
 sional thin layers of grey hard sandstone or quartzite, and a few Red and 
 
 of grey hard limestone ; some of the bands of shale are of a deeper gieen 
 
 red than the general mass, approaching a maroon color. Towards 
 
 the top of the equivalents of these shales, at Cape Rouge, there 
 
 occur a small Lingula and Obolella pretiosa ; the thickness of 
 
 the deposit is from 1500 feet to 1000 
 
 5025 
 
 The strata from 1 to 17 are in ascending order, provided they are not 
 inverted, of which we have no evidence, unless it be the occurrence of an 
 Obolella in the red shales. Several species of this genus occur in the Pots- 
 dam group, and one in what is considered the equivalent of the Calcif- 
 erous portion of the Quebec group, at Troy in New York. The genus 
 being only recently established, it is not yet certain of what value it may 
 be in determining the horizon. For the purposes of generalization, in 
 describing the Quebec group, the series will be considered an ascending 
 one ; not so much, however,, with the view of asserting the order of the 
 strata, as to render more intelligible the facts connected with their geo- 
 graphical distribution. 
 
 These strata occupy the whole of the island of Orleans ; the magnesian 
 shales at the base running along the north-western side, flanked, to the 
 N. W., by the apparently underlying black bituminous beds of the Hudson 
 River or the Utica formation, as far as the neighborhood of Ste. Famille. 
 These black beds sometimes appear in the cliff which runs on that side of the 
 island, but their usual position is on the beach beneath. Below Ste. Famille, 
 the black shales are no longer seen on the beach, or in the cliff, which is 
 tccupied by the magnesian shales, and occasionally by the lowest band of 
 limestone conglomerates, to within a couple of miles of the lower extremity 
 of the island; while at the extremity, and for a mile above, the grey 
 sandstones, 13, appear. The red and green shales at the summit of the 
 series, make their appearance on the south side of the island, about two 
 miles and a half from the upper end, and leave it about four miles from 
 the lower end. Some of the sandstones beneath them, are brought to the 
 shore, in the intermediate space, by undulations. 
 
230 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XL 
 
 Point Levis. From the upper end of the island of Orleans, the lower part of the series 
 passes to Point LeVis ; but in so doing, the strata are supposed to meet with 
 a transverse upthrow dislocation ; which comes upon the margin of the river 
 in the upper part of Indian Cove, and brings the magnesian shales and their 
 accompanying conglomerates, 1 to 4, on the west, against the glauconite 
 shales, 11, on the east. On the west side of the fault, some of these con- 
 glomerates are carried about a mile and a half southward of Indian Point ; 
 and they can be traced sufficiently to show, that, through the effect of 
 three nearly parallel anticlinal folds, of which the axes run about south- 
 west and north-east, they are brought northward again to Indian Point ; 
 whence they are exposed almost continuously, along the south margin of 
 the river, for two and a half miles up. A feature occurring at Point LeVis, 
 
 239-241. BRACHIOPODA. 
 
 239. Obolella pretiosa (Billings) ; a, ventral, and c, dorsal view. 
 
 240. Lingula Irene (Billings) ; a, specimen from Point Le>is ; 6, speci- 
 men from a boulder of the Calciferous formation, island of Mont- 
 real. 
 
 241. L. Quebecensis (Billings) ; a, &, c, three different specimens. 
 
 and not observed on the island of Orleans, is the occasional interstratifi- 
 cation of red layers in the masses of shale which separate the lower con- 
 glomerate bands. 
 
 Quebec. From the south-east side of the St. Lawrence above Point LeVis, some 
 of these strata cross the river, folding, as is supposed, over an anticlinal axis 
 in its bed, and make their appearance on the opposite side, in Quebec. 
 Two of the conglomerate bands are there met with, and, though the strata 
 are much disturbed, one of these bands can be traced from Mountain Street, 
 round the extremity of Cape Diamond, and for nearly a mile on the north 
 side of the cape ; shewing that the measures are here arranged in a synclinal 
 form. There occurs here a series of black shales, with bands of lime- 
 stone and occasional sandstones, the precise place of which in the Orleans 
 
CHAP. XL] QUEBEC GROUP. 231 
 
 section is yet uncertain, though they appear to occupy the position of the 
 grey and green shales, 16, below the red and green shales, 17. 
 
 The red and green shales which occupy the south-east side of the island 
 of Orleans, after folding under a supposed synclinal in the river, are seen on 
 the south-east side of the St. Lawrence near the village of Beaumont. Beaumont. 
 Thence, affected by various undulations and dislocations which render their 
 outcrop difficult to trace, they sweep round at a considerable distance 
 inland, and come upon the St. Lawrence again, above Point LeVis, in the 
 neighborhood of the Grand Trunk Railway station. From this point, after 
 folding, in the bed of the river, over the same anticlinal which affects the 
 magnesian conglomerates, they reach the upper part of "Wolfe's Cove, and 
 
 242-247. BBACHIOPOD A. 
 
 244 
 
 a 242 & 
 
 246 
 
 242. Leptana sordida (Billings) ; a, dorsal, and &, ventral aspect. 
 
 243. L. decipiens (Billings) ; a, ventral, and 6, dorsal aspect ; c, 
 
 interior of dorsal valve. 
 
 244. Orthis Tritonia (Billings) ; a, exterior of dorsal valve ; &, interior 
 of the same. 
 
 245. 0. orthambonites (Pander) ; a, ventral valve ; 6, dorsal valve ; 
 
 '^ c, side view. 
 
 246. O. Electro, (Billings) ; a, ventral valve ; 6, side view. 
 
 247. Camerella calcifera (Billings); a, ventral valve; 6, dorsal ; c, inte- 
 rior of ventral valve, showing the small chamber beneath the 
 beak. 
 
 running inland behind Sillery Cove, re-appear at Cape Rouge, where cape Rouge, 
 they are seen forming the cliff, for some distance below the cape. 
 
 At its summit, this great mass of red and green shales is interstratified 
 with greenish drab-weathering sandstones, the shales prevailing. Higher 
 up, the sandstones exceed the shales, and appear as a well-marked series sniery sand- 
 of fine and coarse grained rocks, frequently assuming the character of fine 8tones - 
 conglomerates, with white quartz pebbles as large as peas. The sand- 
 stones are sometimes slightly micaceous, and occasionally hold small 
 scales of green and black shale, and a few spangles of graphite. They 
 
232 
 
 GEOLOGY OF CANADA. 
 
 {CHAP. XI. 
 
 Thickness of 
 the group. 
 
 are often slightly calcareous. They usually present massive beds ; and 
 at Sillery, many of the layers are quarried for building purposes, for 
 which the stone is used at Quebec. The breadth of the formation at Sillery, 
 including the interstratified masses of red shale, is upwards of half a mile. 
 The average inclination of the strata, which is towards the south-east, is 
 about fifty degrees, and the total thickness may be about 2000 feet. 
 
 The whole volume of the Quebec group, including the Sillery rocks, 
 would thus appear to be about 7000 feet. Its attitude, and its geographical 
 position in relation to the Hudson River formation, are such, that, without 
 the aid of fossils, it would be difficult to arrive at any other conclusion in 
 
 248, 249. GASTEROPODA. 
 
 249 
 
 248. Ecculiomphalus Canadensis (Billings). 
 249. . ___ intortus (Billings). 
 
 Fosefls of 
 Point Levis. 
 
 regard to its age than that it is a newer rock. It was in fact so considered 
 until 1860, when the discovery of a considerable number of fossils in the 
 group, at Point LeVis, furnished the means of comparing it with the Hudson 
 River and other Silurian formations. These fossils have been obtained from 
 the limestone conglomerates of the lie* vis formation, and from the interstrat- 
 ified slates ; but from the corrugated condition q$ the strata, it is not yet 
 quite certain from how many distinct bands the fossils are derived. The 
 fauna from this locality, as far as yet known, consists of one hundred and 
 thirty-seven species, of which forty-two are graptolites, fifty-five mollusks, 
 thirty-six articulates, and four radiates. 
 
 The graptolites include the genera Grraptolithus, Phyllograptus, Tham- 
 nograptus, Dendrograptus, Retiolites, and Dictyonema. The other genera 
 are Orthis, Lingula, Strophomena, Oamerella, Murchisonia, Pleuroto- 
 maria, Holopea, Helicotoma, Straparollus, Ophileta, Maclurea, Ecculi- 
 omphalus, Orthoceras, Cyrtoceras, Nautilus, Asaphus, Cheirurus, Baihy- 
 urus, Agnostus, AmpJiion, Menocephalus, Arionellus, Conocephalites, 
 Shumardia, Holematopus, Endymion, Ampyx, and DikelocepTialus. The 
 described species are Orthis Euryone, 0. Tritonia, 0. orthambonites, 0. 
 
CHAP. XL] 
 
 QUEBEC GROUP. 
 
 Electro,, Lingula Mantelli, L. Irene, Leptcena decipiens, L. sordida, 
 Camerella calcifera, Pleurotomaria calcifera, P. vagrans, P. Postumia, 
 Helicotoma uniangulata, H. perstriata, Holopea dilucula, Maclurea At- 
 lantica, Metoptoma Melissa, M. Orphyne, M. Hyrie, M. Augusta, Stra- 
 parollus Quebecensis, Ecculiomphalus Canadensis, E. intortus, Orthoceras 
 Autolycus, Oyrtoceras Metellus, Q. Dictys, C. Alethes, Asaphus Illce- 
 noides, A. goniurus, Cheirurus Apollo, O. Eryx, Bathyurus Saffordi, 
 B. capax, B. dubius, B. bituberculatus, B. armatus, B. oblongus, B. 
 Cordai, B. quadratus, Agnostus Americanus, A. Orion, A. Ganadensis, 
 Amphion Cayleyi, Menocephalus Sedgwicki, M. globosus, Arionellus 
 cylindricus, A. subclavatus, OonocepJialites Zenkeri, DiJcelocephalus 
 magnificus, D. Belli, D. Oweni, D. megalops, D. cristatus, SJiumardia 
 granulosa, Endymion Meeki, and Holematopus Angelini. Of these, 
 one species, Maclurea Atlantica, belongs to the Chazy, and the fol- 
 
 250 
 
 250-253. CBUSTACEA. 
 251 
 
 250. Jlgnostus Americanus (Billings); a, the tail; 6, the head? a little 
 
 magnified. 
 
 251. A. Orion (Billings) ; natural size. 
 252. Jl. Canadensis (Billings); a, the tail ; 6, the head ; magnified. 
 
 The crosses show the natural dimensions. 
 253. Conocephalites Zenkeri (Billings) ; the head. 
 
 lowing nine to the Calciferous : Lingula Mantelli, L. Irene, Camerella 
 calcifera, Helicotoma uniangulata, H. perstriata, Pleurotomaria calci- 
 fera, P. Postumia, Holopea dilucula, and Ecculiomphalus Canadensis. 
 Besides these, which are identical with Chazy and Calciferous forms, 
 there are many others closely allied to fossils found in the Calciferous 
 in Canada. The aspect of the trilobites is like those figured by Dr. D. 
 Dale Owen, from the oldest rocks of the Mississippi valley. Descrip- 
 tions of the graptolites will be found in Decade II. of the Survey. 
 
 The Quebec group would thus appear to be a great development of strata Age of the 
 about the horizon of the Chazy and Calciferous formations, which are gl 
 brought to the surface by an overturn anticlinal fold, with a crack and 
 great dislocation running along its summit, by which the group is made to 
 overlap the Hudson River formation. The supposed structure is illustrated 
 
234 GEOLOGY OF CANADA. [CHAP. XI. 
 
 structure in the accompanying transverse section from the falls of Montmorenci to 
 the island of Orleans ; in which it will be observed, that, without the aid of 
 fossils, the break on the island would never have been suspected from the 
 attitude of the strata. 
 
 A series of such dislocations traverses eastern North America, from Ala- 
 bama to Canada. They have been described by the Professors Rogers, in 
 
 254. SECTION PKOM MONTMOKENCI TO ORLEANS ISLAND. 
 Montmorenci. North Channel. Orleans Island. 
 
 Horizontal and vertical scale, one inch to a mile. 
 
 g 1 , Laurentian gneiss. q, Quebec group. 
 
 , t } Trenton limestone. F, Fault. 
 
 u, Utica and Hudson Eiver 0, Overlap. 
 
 formations. S, Level of the sea. 
 
 Great fault. Pennsylvania and Virginia, and by Mr. Safford, in Tennessee. The 
 dislocation in question comes upon the boundary of the province, in 
 the neighborhood of Lake Champlain. From this, it proceeds in a 
 gently curving line to Quebec, running nearly parallel with the Phil- 
 lipsburgh and Deschambault anticlinal, and keeping just north of the 
 fortress. It thence skirts the north side of the island of Orleans, leav- 
 ing a narrow margin on the island for the Hudson River shales. From 
 near the end of the island, it keeps under the waters of the St. Lawrence, 
 to within about eighty miles of the extremity of Gaspe, where it again 
 comes upon the land, and appears to leave a narrow strip of the Hudson 
 River or the Utica formation on the coast. 
 
 On the south-east side of this line, the, Quebec group seems to be 
 arranged in long narrow synclinal forms, with many overturn dips. These 
 synclinal forms are separated from one another, on the main anticlinals, by 
 
 Lower black dark grey and black shales, with occasional limestones, which resemble 
 the shales of the Hudson River formation, and, previous to the discoveries at 
 Point LeVis, were supposed to be equivalent to them. As they separate the 
 supposed synclinals of the Quebec group, their stratigraphical place is inferred 
 to be beneath them, and they would thus appear to have some relation 
 
 Potsdam with the Potsdam formation ; but it will require farther investigation 
 
 formation. ^ o Determine wna t that precise relation may be. No great body of rock 
 which can be taken for the Potsdam formation, in its typical form of a 
 sandstone, has been observed immediately above these shales, where they 
 occur in greatest force. In some other localities however, masses of 
 granular quartzite occur, not far removed from the magnesian rocks of the 
 
CHAP. XL] 
 
 QUEBEC GROUP. 
 
 235 
 
 Quebec group, and it will be necessary to re-examine these quartzites before 
 the absence of the Potsdam formation from above the shales can be 
 asserted. From the occurrence of wind and ripple marks on closely 
 succeeding layers of the Potsdam sandstone, where this rests immediately 
 upon the Laurentian series, we know that this arenaceous portion of the for- 
 mation must have been deposited in shallow water, along the coast of the 
 ancient Silurian sea. Out in deep water, the deposit may have been a 
 black partially calcareous mud, such as would give rise to the shales and 
 
 255. CBTTSTACEA. 
 
 255. Dikelocephalus magnificus (Billings) ; a, glabella ; 6, pygidium. 
 
 limestones which come from beneath the Quebec group. The worn frag- 
 ments of black shale, which, as has already been stated, are enclosed in the 
 sandstones of Hemmingford Mountain (p. 88), appear to indicate that such 
 an argillaceous rock must have preceded the arenaceous deposits of the 
 Potsdam, and that it may be a subordinate deep-sea member of the for- 
 mation. 
 
236 GEOLOGY OF CANADA. [CHAP. XI. 
 
 In different parts of their distribution, the rocks of the Quebec group seem 
 to vary considerably in the character of the sediments composing them. 
 They present moreover, over areas of considerable extent, two very dif- 
 ferent lithological aspects, being in the one much more crystalline than in the 
 
 Metamor- other. The subject of their metamorphism will be treated of hereafter, in 
 a separate chapter. The lower division of the group appears to be supplied, 
 in a greater or less degree, with ores of iron, lead, zinc, copper, nickel, 
 
 Metaie of the cobalt, chromium and titanium, as well as with silver and gold. Some of 
 tiiese are already known to exist in quantities economically available, 
 and others will probably be hereafter found to be so. This portion of the 
 group abounds also, in its more altered portions, in roofing slates, ser- 
 pentine, soapstone,potstone, whetstone, magnesite, and dolomite ; the latter 
 
 256-260. KU8TACEA. 
 
 257 268 
 
 Glabellae of the following species : 
 
 \ 
 
 256. Dikelocephalus planifrons (Billings). 
 
 257. D. megalops (Billings). 
 
 258. D. cristalus (Billings). 
 
 259. D. Oweni (Billings). 
 
 260. D. Belli (Billings). 
 
 existing' also in the unaltered area. The country over which the 
 group is distributed, is a mineral region of great importance. What 
 is considered the upper part of the group, composed of the Sillery sand- 
 stones, does not appear to be in any remarkable degree metalliferous, 
 nor is it yet certain whether the more valuable metals abound in the 
 dark shales which are at the base of the group. This whole series of rocks 
 however occupies a stratigraphical place which brings it to the horizon of the 
 upper copper-bearing series of Lake Superior, in which the Kaministiquia 
 slates may perhaps represent the dark colored shales underlying the 
 Quebec group. As the Kaministiquia strata are not wanting in those 
 inetals which give value to the Lake Superior series, it is reasonable to 
 expect that their supposed equivalents at the base of the Quebec group, 
 may also be metalliferous. 
 
CHAP. XI.] 
 
 QUEBEC GROUP. 
 
 237 
 
 With the exception of the ridge between Cape Diamond and the vicinity undulations, 
 of Cape Rouge, and of various islands between Cape Diamond and Father 
 Point, the Quebec group and the subjacent dark shales are wholly on the 
 south-east side of the St. Lawrence, where they occupy a breadth varying 
 from seven to forty miles, before becoming covered up by the uncon- 
 
 261-263. CBUSTACEA. 
 
 \ 
 
 261-263. Pygidia, supposed to belong to different species of Dikdocephalus. 
 
 formable Middle Silurian, Upper Silurian, and Devonian deposits. The axes 
 of the undulations of these lower rocks run rudely parallel with those which 
 have been mentioned as affecting the Trenton and Hudson River forma- 
 tions to the north-west, and with the dislocation which brings the Quebec 
 group to the surface ; the whole being subordinate to the Appalachian 
 system of mountains. Guided by the bearings of these undulations, the 
 strata come out somewhat obliquely upon the river, having a north-easterly 
 strike, with many minor modifications, as far as Cape Chatte ; they then 
 
 264-267. CBUSTACEA. 
 
 266 
 
 264. Arionellus cylindricus (Billings) ; the head. 
 
 265. A. subclavatus (Billings) ; a, glabella ; 6, side view. 
 
 266. Menocephalus Sedgwicki (Billings) ; glabella enlarged. 
 
 26 7. M. globosus (Billings) ; a, side view of the head ; 
 
 6, upper surface ; c, front view. 
 
 turn eastward, and finally southward of east, before quitting the continent 
 in Graspe'. 
 
 The corrugations of these strata are so numerous, and so frequently con- overturn 
 nected with overturn dips and dislocations, that it is almost impossible to ****' 
 follow them out in detail ; and for the present, it is only by the geographical 
 distribution of the larger masses that the position of some of the main anticli- 
 nals can be determined, and a notion of the general structure arrived 
 
238 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XI. 
 
 at. The overturns appear to be more frequently on the north-west than 
 on the south-east side of the anticlinals, producing a predominating south- 
 eastwardly dip in the strata, and giving to the anticlinals a more precip- 
 itous slope on the north-west than on the south-east. In this, they differ 
 from the anticlinals on the north-west side of the main overlap, which, as 
 has already been stated, have the down-throw, or more precipitous dip, on 
 the south-east. 
 
 Bayer and What appears to be one of the main anticlinal axes of the Quebec group, 
 anticu"af 6 en * erm g on ^ e south-east side of the St. Lawrence, at the mouth of the river 
 
 268-273. CRUSTACEA. 
 
 Glabellae of the following species : 
 
 268. Bathyurus oblvngus (Billings). 
 
 269. .B. Cordai (Billings). 
 
 270. B. bituberculatus (Billings). 
 
 271. JB capax (Billings) ; a, longitudinal section. 
 
 272. B. quadratus (Billings). 
 
 273. B. armatus (Billings). 
 
 Bayer, passes by St. Henry, between thirteen and fourteen miles from Que- 
 bec. Proceeding thence by the north part of Inverness and the south part 
 of Somerset, through Arthabaska, it maintains a south-westwardly course to 
 the south-east part of Stanbridge, and crosses St. Armand into Vermont. 
 Between Inverness and Vermont, this anticlinal brings to the surface the 
 lower black shales ; but in consequence of three or four undulations, 
 subordinate to the main geological ridge, the distribution of these shales pre- 
 sents an irregular perimeter, giving place to long parallel stretches of the 
 superior rocks, which occupy some of the intermediate synclinals in Acton, 
 Koxton, and Shefford. The greatest breadth of the shales is on the St. 
 
CHAP. XI.] QUEBEC GROUP. 239 
 
 Francis, where they extend nearly across Simpson and Kingsey, and Lower shales. 
 
 occupy about fourteen miles ; displaying on the banks of the river, in the 
 
 latter township, a very broken and corrugated condition. To the north-east 
 
 from this, the shales gradually grow narrower, and appear to come to 
 
 a point somewhere beyond Inverness, probably in the seigniory of St. 
 
 Croix, where however they are covered with drift. To the south-west, 
 
 the continuity of the distribution is very nearly interrupted by the 
 
 effect of the subordinate undulations which have been mentioned : the 
 
 narrowest part is near the line between Koxton and Shefford. South- intrusive 
 
 west of this, there is intruded among the shales, a mass of granitoid trachyte, trachytes. 
 
 forming Shefford Mountain ; beyond which, the ridge of the anticlinal 
 
 appears to be somewhat removed to the westward, and a large mass of 
 
 the same trachyte, occupying an area of twenty square miles, and forming 
 
 the Brome Mountains, bounds the shales to the eastward. Opposite to these 
 
 274-277. CRUSTACEA. 
 
 274 a 
 
 277 
 
 274. Bathyurus Saffordi (Billings) ; a, glabella ; 6, pygidium. 
 275. Cheirurus Apollo (Billings); glabella. 
 
 276. C. Eryx (Billings) ; glabella. 
 
 277. Jimphion Cayleyi (Billings) ; pygidium. 
 
 trachytic hills, the shales have a breadth of about five miles, which is 
 maintained with considerable uniformity to the province line. 
 
 Throughout their distribution on this anticlinal, these lower rocks consist 
 of dark grey and black clay slates, often carbonaceous, with some bands of a 
 lighter color. The slates are interstratified in some parts with thin grey 
 sandstones, and in others with thin black and dark grey limestones, which are 
 occasionally in sufficient quantity to be wrought for lime-burning. A mass ramham. 
 of this description is quarried for the purpose on the twenty-sixth lot of the 
 first range of Farnham, near the western limit of the area which has been 
 described. The rock contains very small, almost microscopic trilobites, 
 and fragments of small brachiopods. The genera are Ptilodictya, Gf-raptoli- 
 
240 GEOLOGY OF CANADA. [CHAP. XI. 
 
 thus, Orthi9,Leptcena,AmpyX) Dalmanites, Lichas, Triarthrus, and Agnos- 
 tus. The Ptilodictya strongly resembles P. acuta, and may be the same ; 
 while one Leptcena cannot be distinguished from L. sericea. These 
 Fossils. fossils have a less ancient aspect than might be expected in the Potsdam 
 formation; so that the Farnham slates, with similar ones in other localities, 
 may be brought into position by some of the many complicated disloca- 
 tions which affect the strata. Except, however, where such fossiliferous 
 strata are known to occur, the black slates and limestones will be pro- 
 visionally described as older than the Quebec group. At Cook's Corner 
 in St. Armand, near their eastern limit, these lower slates are cut by a 
 vein of white quartz, marked with spots of copper pyrites, galena, and 
 blende. The vein runs north-east and south-west, coinciding with the 
 strike, and presents a breadth of between five and six inches. 
 
 The anticlinal form which these slates are supposed to possess between 
 the province line and St. Croix, can scarcely be proved from a com- 
 parison of the dips. These are in general at high angles, and, though 
 sometimes to the one side and sometimes to the other of the strike, they 
 do not always coincide in direction with the results deducible from 
 the geographical distribution of the strata, several of them being no doubt 
 overturn dips. Such as are considered to be of this character generally 
 point to the south-east, but this is not the case in every instance. The 
 anticlinal form is rather to be inferred from the arrangement of the 
 superior rocks on each side, and from the fact that the black slates 
 and limestones are traceable nearly round the extremity of a trough of 
 those rocks, through a transverse gap on the west branch of the Nicolet, 
 into a long narrow valley ; which they occupy for the distance of about 
 fifty miles along an anticlinal, which runs from Danville to Sutton, in a 
 direction nearly parallel with the one already described. 
 
 Danville and In this valley, the slates, which are often plumbaginous, run under 
 Button anti- D anv ille and Richmond, in Shipton and Cleveland, and across Melbourne 
 
 clinal. x 
 
 and Ely, the southern line of which last township they intersect about the 
 middle ; proceeding thence across Stukely to the north-east corner of 
 Brome, where they point to Brome Lake, and to the valley of Sutton beyond. 
 The breadth of the slates varies from one to three miles ; at Melbourne 
 it is two miles, and in this breadth there would appear, to be two folds, 
 which gradually separate from one another. One of these proceeds towards 
 Sutton valley, as already stated, and the other turns up a tributary of the 
 Salmon River, in which it is traceable for between eight and nine miles, 
 to the twelfth lot of the eighth range of Brompton, where it points to the 
 north-east corner of Stukely, and to Potton valley beyond. On the line 
 between Stukely and Ely, these two anticlinal branches are about five 
 miles apart, and there are facts in Ely which indicate that another bifurca- 
 tion probably occurs in the geographical distribution of the slates, about the 
 
CHAP. XL] QUEBEC GROUP. 241 
 
 third lot of the third and fourth ranges of the township. This would 
 shew an anticlinal intermediate between the other two, the axis of which, 
 in its course southward, would apparently run through the highest part of 
 Sutton Mountain. 
 
 North-east of Danville, the slates have been traced about half way across 
 Tingwick ; and in their farther course, they would probably run through 
 the north corner of Ham, into Wolfestown. In the continuation of the anti- 
 clinal, which there brings them to the surface, they are seen again in a 
 narrow strip, running along the north-west side of Broughton, and crossing 
 the Chaudiere in the seigniory of St. Joseph ; but they have not yet 
 been observed on the same axis farther on. 
 
 Where the strata of the Quebec group come upon the St. Lawrence 
 above Cape Rouge, a considerable portion of the beds seen on the island of 
 Orleans, including the magnesian shales and their conglomerates, is wanting, 
 and it appears to be the second mass of sandstones, 15 of the section, 
 that is in contact with the Hudson River shales. A still farther portion is st. Nicholas, 
 deficient where the dislocation reaches the opposite side of the river, a little 
 above St. Nicholas church ; and here the red and green shales, 17, under- 
 lying the Sillery sandstones, constitute the strata which lean against the 
 Hudson River beds. It is not improbable, however, that in other places 
 the lower black slates may occasionally present themselves in a narrow 
 strip between the overlap and the margin of the Quebec group. In such 
 cases, the strong resemblance of these slates to those of the Hudson River, 
 would render it difficult to distinguish the one from the other, and to deter- 
 mine the exact position of the dislocation, unless through the presence 
 of fossils. The difference in age between the two sets of slates having 
 been only recently ascertained, it will require farther investigation to 
 trace out in detail the line that divides them. 
 
 In the general synclinal form that lies between the overlap and the Lauzon and 
 Bayer and Stanbridge anticlinal, the Quebec group is either completely ^ aniham 
 or very nearly divided into two areas, by the underlying black slates on 
 or near the St. Francis. The deepest part of the north-eastern area, which North-east 
 may comprehend a superficies of about 800 square miles, appears to be basin - 
 in Lauzon, where it is crossed by the Chaudiere ; on the banks and in the bed 
 of which, the Sillery sandstones, with their interstratified red shales, display 
 a breadth of nearly ten miles, while longitudinally they extend about the 
 same distance on each side. They present a complicated series of undu- 
 lations, which give to the perimeter of the space occupied by these sand- 
 stones, an irregular longitudinally indented figure, the details of which 
 have not yet been completely made out. 
 
 Within this north-eastern area, at St. Flavien, about five leagues above st. riavien. 
 the Chaudidre, and two leagues from the St. Lawrence, red shales occur, 
 underlaid by a band of amygdaloidal diorite, which appears to occupy the 
 
 Q 
 
242 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XI. 
 
 
 place of the magnesian conglomerates. It is between a quarter and half 
 a mile wide, and limestones occur both at the summit and at the base of 
 the band, which in those parts appears to be of a concretionary or con- 
 glomerate and brecciated character, being composed, particularly at the 
 base, of rounded and angular masses of amygdaloidal diorite, varying in 
 diameter fium two inches to two feet. Many of these appear to be 
 calcareoits, and much of the rock is red. The interstices among the 
 masses are filled with calcspar, which is transversely fibrous towards 
 the walls, and incloses crystallized quartz in the centre. This band is 
 highly cupriferous, and ores of copper occur both in the beds, and in 
 veins or lodes which cut them ; the bearing of the veins, however, being 
 with the strike. The ore in the beds is copper pyrites, large masses 
 of which have been met with associated with the limestones at the top. 
 The veins, in addition to copper pyrites, hold the variegated and vitreous 
 sulphurets. In one spot, native copper occurs in small masses in the 
 conglomerate at the base of the diorite, and the whole band has a 
 striking resemblance to some of the rocks of the upper copper-bearing 
 series of Lake Superior. 
 
 To the south-west of this, the country is very much covered by 
 drift ; but upon the Becancour and the Nicolet, there are many 
 exposures of red shales and of grey sandstones, which are supposed 
 to be lower than the Sillery division. No great exhibitions of the magne- 
 sian slates and conglomerates of the LeVis formation have been observed 
 near to the margin in this part, of the north-eastern area. Along its 
 southern border, through Nelson, Somerset, and Stanfold, red slates 
 approach to within a short distance of the lower black slates and lime- 
 stones ; but they are separated by intervening grey calcareous sandstones 
 and green slates, which may possibly represent the magnesian strata. 
 Somerset. On the fourteenth and fifteenth lots of the eighth range of Somerset, 
 there are interposed about 150 feet of grey coarse grained calcareous 
 sandstone, resting on ten feet of limestone conglomerate, followed by a 
 twelve-feet band of diorite, in which are disseminated small masses of 
 calcspar, giving it an amygdaloidal aspect. The conglomerate is marked by 
 the presence of copper pyrites, running in patches with the stratification. 
 Nearer to the St. Francis, grey calcareous sandstones occur on both 
 margins of the area, with red slates not far above them ; but they are not 
 associated with any observed limestone conglomerate. The only beds of 
 Quebec rocks belonging to this north-eastern area, which are exposed on 
 the St. Francis, consist of coarse grained greenish sandstones associated 
 with red shales, which occur at the rapid above Drummondville. The 
 sandstone has more of the character of the Sillery beds than of those lower 
 in the series, and it appears to form a portion of the south-western 
 extremity of the trough to which it belongs. It is underlaid by blackish 
 
CHAP. XL] QUEBEC GROUP. 24S 
 
 shales, and a band of good black limestone, which occurs about half a mile 
 farther up the river, and it is not improbable that the grey calcareous 
 sandstone may be concealed both above and below these exposures on 
 the stream. 
 
 These greenish sandstones on the St. Francis are intersected by several 
 dykes of diorite, the courses of which, in the short distance seen, are in a 
 general way down the stream. The rock of the fall at Drummondville, Drummond- 
 which is about two miles lower on the St. Francis, appears also to be vlUe * 
 a diorite, and is of a grey or greenish color ; it probably belongs 
 to the stratification, and is not known to have any connection with 
 the dykes. It has a breadth of about half a mile, and some Diorite. 
 parts are porphyritic from the presence of small crystals of light 
 greenish feldspar, while others are amygdaloidal, holding small portions 
 of white and pinkish calcspar, and occasional nodules of agate. Much of it 
 bears the aspect of a breccia, in which fragments of the diorite are held 
 together by a close grained but highly crystalline calcareous cement, 
 approaching in color to the general mass of the rock. This rock bears a 
 resemblance to that of St. Flavien, of which it may be a continuation, and 
 like it is highly cupriferous. On the first lot of the first range of 
 Wendover, it holds vitreous, variegated, and pyritous sulphurets of copper, 
 which run in six or seven thin veins or courses, formed by breaks and slips 
 in the diorite, within a breadth of about 350 yards. 
 
 The south-western portion of the above described synclinal of the south-west 
 Quebec group, has a length of about fifty miles, extending from Wickham basm ' 
 to Farnham. How near it may approach, on the north-west, to the band 
 of Trenton limestone running from St. Dominique towards Phillipsburgh, is 
 not quite certain. Between St. Pie and Farnham, the distance appears 
 to be not over a mile. The nearest observed strata of the Quebec group, 
 apparently belonging to the Sillery division, are on the Barbue, on the 
 road of the Seraphine range in the seigniory of St. Hyacinthe ; and other 
 exposures occur at the base of the Yamaska Mountain. The greatest 
 breadth of the area may be about fifteen or eighteen miles, across Milton and 
 Roxton. It appears to be divided into at least two subordinate syn- 
 clinals, running parallel with one another, and including many minor undu- 
 lations. The deepest part of the area seems to be in Roxton, Milton, and 
 Granby, in which the Sillery sandstones are largely displayed, with their 
 accompanying red shales. Along the margin of the area there is exposed, Dolomites. 
 in a great many places, a band of greyish-white and reddish-grey compact 
 sub-crystalline yellowish-weathering dolomite, from 200 to 300 feet thick. 
 It is in massive beds, associated with a good deal of chert, and often 
 incloses mammillated concretionary forms, resembling those of travertine. 
 At the summit, this rock often terminates in a breccia or conglomerate, 
 holding angular and rounded masses of limestone, intermingled with ragged 
 
244 GEOLOGY OF CANADA. [CHAP. XI. 
 
 irregular masses of chert. In some places, the conglomerate is separated 
 from the main body of the dolomite by dark grey or black shales, inter- 
 mixed with diorite. In these, the conglomerate lies in large isolated masses, 
 
 Acton; cop- running parallel with the summit of the main body of the dolomite. On 
 the thirty-eighth lot of the seventh range of Acton, the junction of the shale 
 and the dolomite is characterized by numerous well preserved branching 
 fucoids, resembling JButhotrephis flexuosa of Emmons. This magnesian 
 limestone is marked in a multitude of places by the occurrence of the vitreous, 
 variegated, and pyritous sulphurets of copper, which are found in irregular 
 masses running with the stratification. In the neighborhood of these, many 
 veins of quartz and calcspar intersect the rock in various directions, and 
 hold small portions of the sulphurets of copper. The copper ores, which 
 are olten slightly argentiferous, appear to be most abundant in the upper 
 part of the limestone, and in many places the quantity found has been suf- 
 ficient to give reasonable expectations of profitable mining. The largest masses 
 of ore which have been met with in this region, are at the Acton mine, 
 on the thirty-second lot of the third range of that township. Here the con- 
 glomerate presents a number of isolated masses at irregular distances from 
 one another, separated from the main band of limestone by between eighty 
 and ninety feet of dark grey shale and olive-green yellowish-weathering 
 amygdaloidal diorite. These isolated masses are overlaid by a considerable 
 amount of the same dark grey or black shale. On the opening of the mine, 
 the sulphurets, where most abundant, appeared to occupy a position imme- 
 diately near some of the isolated masses of conglomerate, and partially to 
 surround them, in certain parts constituting the paste of the conglomerate. 
 A description of this mine will be given in a subsequent chapter. 
 
 The Acton mine is situated on the south-east side of the more north- 
 western of the synclinals. The measures there dip north-west, at an angle 
 of between thirty and forty degrees, and the copper-bearing limestone finally 
 re-appears in Upton, seven miles to the north-west, where it is associated, 
 in some parts, with red shale. Intermediate undulations cause its appear- 
 ance about half way between the two points ; and in the north-eastern part 
 of the synclinal there are many exposures of the rock in Acton, Upton, and 
 Wickham, always more or less accompanied with the sulphurets of copper. 
 
 Milton. Towards the north-west side of this synclinal, in Milton^ where the band 
 of magnesian limestone has not yet been observed, indications of these 
 sulphurets occur in red slates, which can be readily traced, on the strike, 
 across Milton and Granby, for a distance of twenty-five miles, and prob- 
 ably represent the slates underlying the Sillery sandstones. On the south- 
 east side of the synclinal, from Milton to Farnham, these red slates, and the 
 underlying magnesian limestones, appear to be absent, as there is no room 
 for them, between what are considered the Sillery strata, and the lower black 
 shales to the east of them, by which they may possibly be overlapped. 
 
CHAP. XI.] QUEBEC GROUP. 245 
 
 The most eastern exposure of these sandstones, with the interstratified red 
 slates, is at the village of Granby, and presents an overturn dip of S. 50 
 E. < 70. Within a hundred feet of the base of these are included two 
 beds of green unctuous chloritic limestone, holding iron, manganese, nickel, 
 and chromium. In the more south-eastern synclinal of the south-western 
 area, the Quebec rocks appear to extend either uninterruptedly, or in 
 separate patches, from the fourth range of Durham to the neighborhood 
 of Shefford Mountain. The magnesian limestone crops out in several places, 
 and in Durham and Roxton is strongly marked with sulphurets of copper. 
 
 In the synclinal lying between the two anticlinal ranges of black shales Shipton and 
 and limestones, which have been described, the one running from Inver- 
 ness to Stanbridge, and the other from Broughton to Sutton, the rocks 
 of the Quebec group present themselves with a somewhat altered aspect. 
 The magnesian limestones, of which several bands, in two groups, occupy a Altered 
 place on each side of the synclinal, are more crystalline than before, and are rocks - 
 studded with crystals of magnetic iron and chromic iron, the former in 
 one place so abundant as to render the rock an iron ore, available for 
 economic purposes. Chlorite and greenish-white foliated talc occur in the 
 limestones, and red dodecahedral garnets are occasionally met with. The 
 colors of these magnesian limestones, which are often true dolomites, are 
 light grey and yellowish-white, and they usually weather to some decided 
 tint of yellowish-brown or reddish-brown. They sometimes exhibit an 
 obscurely brecciated or conglomerate aspect, and occasionally present, 
 in the direction of the stratification, short patches of peroxyd of iron, 
 passing into a blood-red jasper. They are almost always marked by a 
 net-work of white quartz veins one or two inches thick, cutting them 
 in various directions, and often by similarly reticulating veins of peroxyd of 
 iron, which is occasionally titaniferous. 
 
 These limestones are separated from one another by quartzo-chloritic chloritic 
 strata, made up of grains of quartz and scales of chlorite in various sL 
 proportions ; constituting in some places light greenish chloritic quartzites, 
 occasionally resembling coarse sandstones, and in others dark green chlo- 
 ritic slates. Towards the province line, the quartzites appear more conspic- 
 uous on the west side of the synclinal ; but towards the St. Francis, they are 
 well displayed on both sides, and in many places, losing all their chlorite, 
 they become nearly pure white. On the east side of the synclinal, towards 
 the province line, the dark green chloritic slates are sometimes interstrat- 
 ified with light grey micaceous slates with a nacreous lustre, and thin beds 
 of dark grey clay slates with a plumbaginous gloss. Associated with Specular 
 these, are other beds of a schistose rock, made up of specular iron mixed s< 
 with grains of quartz, and often with chlorite, forming varieties of what 
 has been named siderocrist and itabirite by some authors, and by others 
 has been called specular schist. In some of these beds, the oxyd of iron 
 
246 GEOLOGY OF CANADA. [CHAP. XI. 
 
 predominates, constituting a rich iron ore ; but in others, the earthy minerals 
 are in excess, and the rock passes into the ordinary slates of the country. 
 These iron ores often contain a portion of titanium. Thin leaves of talc 
 and chlorite lie in the divisions between the layers of the specular 
 schists, and their surfaces are sometimes stained with green carbonate 
 of copper ; which is also met with in small veins with quartz, orthoclase, and 
 chlorite, running with the stratification. These veins sometimes contain 
 
 Copper ores, sphene and rutile. In some parts, the nacreous slates abound in chloritoid ; 
 and occasionally the sulphurets of copper are so disseminated in them, 
 in grains, and in thin interlocking lenticular patches, as to constitute what 
 appear to be workable beds, traceable for considerable distances with much 
 regularity. Near to the St. Francis, in one or two places, bands of red 
 shale are associated with the magnesian limestones. 
 
 These magnesian limestones, on the opposite sides of the synclinal, are 
 traceable from the province line to the river St. Francis, and beyond it 
 nearly as far as the Nicolet, where they turn towards one another, and 
 probably join. The only difficulty in following them arises from the 
 intrusion of the granitoid trachyte of the Brome Mountains, which disturbs 
 them on the west side, and between which and Brome Lake they have not 
 
 Epidotic yet been observed. The interval between ttiese belts is occupied by 
 chloritic, micaceous, and epidotic rocks. Towards the province line, these 
 are of a slaty character, and of various shades of color, from very dark 
 bluish-green or blackish-green, to ash-grey. The green bands are more 
 abundant than the grey, and both have occasionally a talcoid lustre. The 
 grey bands appear to derive their color from a large amount of very 
 fine grains of white quartz, which are uniformly mixed with chlorite. 
 These beds often contain nodules of white granular quartz and crystalline 
 pistachio-green epidote, sometimes several inches in diameter, and fre- 
 quently elongated in parallel directions. The two minerals are often in 
 separate nodules, but as often intermixed : in the latter case, the epidote 
 is generally within the quartz. In the grey bands, fine blackish-green 
 lines of chlorite often run parallel to one another ; but these are contorted 
 by the nodules of quartz and epidote, with which orthoclase feldspar is 
 sometimes associated. Radiated actynolite often occurs in these rocks, 
 together with asbestus in short parallel veins, which, are found cut- 
 ting the epidote in the direction in which the nodules are elongated, and 
 occasionally between the layers of slate. Crystals of specular and magnetic 
 oxyd of iron are abundant in the chloritic and epidotic bands, the magnetic 
 species being more frequent where the chlorite prevails. 
 
 Near to the St. Francis, nodules of an epidotic character are thickly dis- 
 seminated through the chief part of these chloritic strata ; some of the nodules 
 being six, eight, and even ten inches in diameter. Some of the bands 
 hold small patches of finely granular white quartz, which occasionally 
 
CHAP. XI.] QUEBEC GROUP. 247 
 
 swell into beds of white quartzite, of some importance, while many of the 
 strata assume the aspect of fine quartzose conglomerates or coarse sand- 
 stones with a chloritic base. Except where intersected by transverse valleys, 
 these chloritic and epidotic rocks constitute a ridge in the middle of the 
 synclinal running from the Pinnacle Mountain in St. Armand, to Brooker's 
 Hill in Shipton. 
 
 The workable beds of the specular schists in this synclinal, appear, so 
 far as yet known, to be confined to St. Armand, Sutton, and Brome. They 
 may represent the red slates of other parts, which, being very ferruginous, 
 and often containing titanium, may give rise to these slaty iron ores by their 
 alteration. The number of localities in which the ores are met with in 
 these townships is no doubt in a great measure due to repetitions of the 
 same beds through undulations. These iron ores will be described more 
 at length in a subsequent chapter. 
 
 In the limestone on each side of the synclinal, and in two or three dif- Copper- 
 ferent stratigraphical positions among the- chloritic slates which occupy ^t" s " g 
 its centre, there occur beds or fahlbands, impregnated with the sulphurets 
 of copper. These beds, at intervals on the strike, appear to contain 
 such quantities of copper ores as may be economically available. Copper- 
 bearing beds are found in Shefford, Stukely, Ely, Melbourne, Cleveland, and 
 Shipton, and trial pits have been sunk on the outcrops of some of them 
 to depths varying from twenty to thirty feet. 
 
 The axis of the Danville and Sutton anticlinal would cross the boun- Danvuie and 
 dary between Canada and Vermont, near to the line dividing St. Armand ^^ a 
 from Sutton. On the east side of this axis, the magnesian rocks are 
 repeated. Here the dolomites inclose crystals of chromic and magnetic iron 
 ore, foliated talc, and chromiferous mica. They are associated with beds 
 of soapstone, often containing bitter spar, and with others of -magnesite and 
 serpentine. Almost all of these rocks contain chromium in some form, gene- 
 rally with traces of nickel. In these magnesian bands, the dolomites pre- 
 vail ; and they are separated from one another, as on the west side of the 
 axis, by chloritic slates, chiefly of a coarse quartzose character, and often 
 thickly studded with crystals of the magnetic and specular oxyds of iron. 
 Workable beds of these ores, however, have not been observed among the 
 strata on this side of the anticlinal. 
 
 This belt of magnesian strata runs nearly parallel to its equivalent on the sutton Moun- 
 west side of the anticlinal axis, and passes through Sutton, Brome, and tam< 
 Bolton, along the western base of Sutton Mountain. This mountain stands 
 on an area, which, near the province line, has a breadth of about ten miles : 
 it appears to be composed of coarse chloritic and micaceous slates. In many 
 parts, the slates become very quartzose ; and they frequently contain 
 a portion of feldspar, giving to them the characters of gneiss ; while in 
 
248 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XI. 
 
 Potton; 
 
 soapstone. 
 
 Melbourne 
 ant! mfr 
 
 some parts, they lose their schistose structure, and break into large solid 
 blocks. 
 
 Q n the east side of the area which includes Button Mountain, the belt 
 of magnesian rocks is repeated in Potton. It here consists of serpentine, 
 soapstone, and other magnesian minerals. The serpentine, usually in a 
 band of from 150 to 300 feet broad, is of a blackish-green; it has a 
 very uneven exterior, and weathers to a decided reddish-brown, or 
 to a marked opaque-white. Thin veins of a pea-green serpentine, which 
 is softer than the blackish-green, and reticulating veins of asbestus, inter- 
 sect the rock in various directions. Considerable masses of the rock are 
 sometimes of a light greyish-green, chequered by thin veins or seams of 
 a darker color, cutting and sometimes slightly dislocating one another in 
 rudely parallel directions, which, not being at right angles, divide the masses 
 into irregular rhombic prisms. Picrolite is very frequently met with 
 in irregular seams or veins, some of which are two or three inches in 
 breadth ; and as the fibres of the mineral run slightly oblique to the 
 veins, specimens may be obtained two or three feet long in the direction 
 of the fibres. Octahedral crystals of magnetic iron ore are often dissemi- 
 nated in the rock, and the mineral frequently runs in small beds in the 
 direction of the strike. Chromic iron also occurs in the same manner, and 
 workable quantities of it have been found. Iron pyrites is dissemi- 
 nated in small cubes, and the sulphurets of copper are found running in 
 patches with the stratification. 
 
 Soapstone or steatite is often associated with the band of serpentine, and 
 occurs in considerable quantity in some parts on the west side of it. It 
 seems also in some places to be present in the run of the serpentine, where 
 this is not observed, and it occurs in workable beds of several feet thick : 
 its color is light grey, occasionally banded with greyish-green. The soap- 
 stone sometimes contains veins of delicate greenish-white amianthus two 
 or three inches thick ; and it occasionally passes into an asbestiform talcose 
 slate, which breaks into long fibrous masses in the direction of the dip. 
 In some parts, the place of the serpentine is apparently occupied by dolo- 
 mite. On the west side of the serpentine band is a rock which appears 
 to be quartzose, strongly chloritic, and slightly calcareous, and beyond this 
 occurs a green translucent compact feldspathic rock, holding magnetic 
 iron ore and veins of asbestus. Both rocks together occupy a breadth 
 of about a hundred yards. 
 
 This belt of magnesian strata runs nearly north and south, on the west 
 s ^ e ^ *^ e Missisquoi Ri ver ? ' m Potton. A similar belt runs parallel with it 
 on the east side of the river, the one being a repetition of the other on the 
 opposite side of an anticlinal axis. The distance between them is upwards of 
 a mile ; and with the exception of a part concealed, in immediate succession 
 to the western band of serpentine, it appears to be occupied chiefly with beds 
 
CHAP. XI.] QUEBEC GROUP. 249 
 
 of a hard grey white-weathering feldspathic rock, and grey clay slates with Anorthosite 
 talcoid surfaces. Some parts of the feldspar rock assume a granular texture, rock8 ' 
 giving them the aspect of coarse-grained sandstones, and solid mas- 
 sive beds are separated by thinner bands of a more schistose structure, 
 holding mica. Interstratified with the grey clay slates are thin black, 
 and apparently carbonaceous bands, with glossy surfaces. It is difficult 
 to say what proportion the feldspar rocks may bear to the clay slates in this 
 section, but it appears probable that the latter predominate. 
 
 Before reaching the eastern band of serpentine, there are interposed 
 about 270 yards of green chloritic and epidotic slaty rocks. A portion of 
 these appears as if made up of large reniform or ovoid masses, 
 pressed on one another irregularly ; the epidote occupying the inter- 
 stices, and giving a marbled aspect to the surface. The colors are various 
 shades of light green, and the rock has in general a waxy lustre, and 
 a jaspery fracture. Thin fragments are imperfectly translucent on the 
 edges, and their texture is something like that of porcelain. In some parts, 
 there occur brecciated or conglomerate beds, enclosing slaty fragments, 
 weathering whiter than the matrix : this, under atmospheric influences, 
 becomes pale greenish-yellow, passing into white. This rock appears, 
 like that just described as occurring with the grey clay slates, to be com- 
 posed of an anorthic feldspar, and occasionally, by the presence of horn- 
 blende, passes into a diorite. 
 
 The breadth of the eastern band of serpentine is about the same as the 
 western, but perhaps may occasionally exceed it. It seems in some parts 
 to be interstratified with a band or two of what appears to be an inti- 
 mate mixture of feldspar and diallage. Crystals of the latter mineral 
 are often imbedded in the serpentine ; and in the north-eastern extension of 
 the band, layers of it frequently pass into diallage rock. Beds of soapstone 
 are common, and appear in general to be towards the east side. Magnetic 
 oxyd of iron and chromic iron often occur in imbedded crystals and small 
 seams. Interstratified workable masses of both are occasionally met with ; 
 and in one case, a large mass of ore consists of a granular mixture of 
 ilmenite and magnetic oxyd of iron. A limestone, generally magnesian, is 
 frequently met with either in contact with or very near to the serpen- 
 tine. It is generally grey ; and in a large number of cases, it presents such 
 an aspect, both externally and internally, as to leave little doubt that it is 
 of a brecciated or conglomerate character ; it is often spotted with bright 
 green stains, generally due to a chromiferous mica or garnet. On the pyroxene and 
 east side of Brompton Lake, associated with the serpentine, is a pale s arnet - 
 greenish pyroxene rock, in which occur druses lined with large twin crystals 
 of white pyroxene and cinnamon-colored garnets. Large masses of calca- 
 reous spar, probably filling a vein, are here met with ; sometimes nearly pure, 
 white and cleavable, at others penetrated and filled with small emerald- 
 
250 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XI. 
 
 Feldspathic 
 rocks. 
 
 Diorite. 
 
 green crystals of a chrome garnet. This mineral also forms granular 
 masses, mixed with a little calcareous spar and pyroxene, and containing 
 disseminated, small quantities of the sulphuret of nickel, millerite. 
 
 In Potton, a bed of rock, supposed to be a dolomite, with disseminated iron 
 pyrites, bounds the serpentine on the east side ; and after about 400 
 yards (in nearly a fourth part of which distance, grey clay slates 
 with glossy talcoid surfaces are exposed), appears a series of feld- 
 spathic strata. Some of these consist almost wholly of a white compact 
 anorthic feldspar, with a scaly fracture and a waxy lustre. In other cases, 
 the rock has an admixture of hornblende, constituting a variety of diorite. 
 This is sometimes fine grained ; and the two elements not being readily 
 distinguishable, the rock has a uniform greenish color and a compact 
 texture. It weathers to an opaque white, and in some degree resem- 
 bles serpentine in its aspect, although much harder. In some beds of this 
 character, small rounded or angular grains of quartz are imbedded ; and in 
 others, occasional fragments of indurated jaspery shale. Small veins of 
 asbestus, and occasional patches of serpentine, also occur in these rocks. 
 In some parts, the hornblende is replaced by pyroxene, or passes 
 into diallage ; the crystals of hornblende are sometimes dark green in color, 
 and of large size, giving rise to a coarse grained diorite. This, in one 
 locality, is intermixed with a white compact garnet, which in other localities 
 forms distinct beds, associated with the diorite or with the serpentine. 
 
 Large masses of these feldspathic rocks, sometimes equalling 400 yards 
 in breadth, and subdivided into layers, which present various modifications 
 of the varieties just mentioned, are separated by bands of dark grey 
 pyritiferous clay slate, sometimes 300 yards wide, and with very smooth 
 talcoid surfaces. Some parts of the slate appear to hold fragments and 
 nodules, differing slightly in color from the general mass, and weathering 
 to a much lighter color, while other parts of it are of a decided red. These 
 alternating rocks occupy about a mile beyond the last mentioned serpen- 
 tine, and the strength of the feldspathic portions causes them to form a 
 range of hills, which accompany the serpentine as far as it has been 
 orford Moun- traced, and constitute some of the highest peaks of the district ; Orford 
 or Victoria Mountain being one. Beyond these feldspathic rocks, to the 
 eastward, there are additional bands of dolomite, some of them passing into 
 magnesite. Both of these rocks contain a good deal of carbonate of iron. 
 
 The eastern band of serpentine of the Missisquoi valley, in its northern 
 prolongation, is traceable across Potton, Bolton, and a part of Stukely, into 
 Orford, where it presents a complicated distribution, through the effect of 
 undulations. Farther on, it can be followed through Brompton and Mel- 
 bourne, to the St. Francis, on the south-east side of the eastern branch 
 of the lower black shales and limestones. It has already been stated that 
 where these black shales cross the St. Francis, they have a breadth of 
 
 tain. 
 
CHAP. XL] QUEBEC GROUP. 251 
 
 about two miles ; and it will be observed, that while they are flanked on the 
 one side by the magnesian rocks which run to the east side of the anticli- 
 nal in Potton, they are bounded on the other by those which are traceable 
 to the west side of the anticlinal in Sutton ; the distance between the two 
 anticlinals increasing from two to about fourteen miles. 
 
 Sutton Mountain, standing between these two anticlinals, with a height sutton Moun- 
 said to be about 4000 feet, and gradually dying down before reaching the tain> 
 St. Francis, might be expected to present a synclinal structure. In three 
 transverse sections, however, the strata have been observed to maintain its structure, 
 dips, generally at high angles, in opposite directions from the axis of the 
 mountain, with much constancy, for upwards of twenty-five miles. 
 This accords with the apparent distribution of the underlying black shales 
 and limestones in the spur intermediate between the projections on the 
 Sutton and Potton anticlinals. Sutton Mountain would thus appear to be 
 composed of strata which overlie the magnesian portion of the Quebec 
 group. It may probably include the whole or a portion of the Sillery 
 sandstones, which, standing in an anticlinal attitude, would seem to have 
 resisted or escaped the denuding forces that have worn out the valleys 
 on the anticlinals of Sutton and Potton. The belts of magnesian rock, 
 which are at the base of the mountain, on its opposite sides, should by this 
 structure be carried to a junction on the central anticlinal axis, after 
 turning on the synclinals which must occupy the two flanks of the 
 mountain ; but though these belts have been traced northward for upward 
 of twenty-five miles, their point of union has not yet been observed. None 
 of the rocks of the mountain have been observed to be of a red color ; but 
 if any part be the equivalent of the red shales of the Orleans section, the 
 iron which forms the coloring matter of these may be represented in the 
 magnetic and specular oxyds, which, in the form of crystals, abundantly 
 characterize the strata in many parts. It may be remarked also, that if 
 this mountain were composed of strata lower than the Quebec group, 
 the argillaceous rocks, which are the next in succession, instead of dimin- 
 ishing to points in their southward course, should rather be spread over 
 a considerable part of the mountain, or constitute a broad zone of clay 
 slates on each side. 
 
 To the east of the main band of feldspathic rock in Potton, there is 
 met with a farther amount of a similar rock, with dolomite and magnesite, 
 associated with clay slates. On approaching Memphramagog Lake, a dif- 
 ferent series of rocks is met with, consisting of clay slates, followed by fos- 
 siliferous limestones. These strata, which appear to be of the Upper upper siiu- 
 Silurian and Devonian ages, belong to a synclinal area, which terminates 
 in a point at the base of the Owl's Head, a mountain on Memphramagog 
 Lake. The west shore of this lake, from the Owl's Head, inclusive, to the 
 
252 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XI. 
 
 Stoke Moun- 
 tains. 
 
 province line, is however composed of strata which appear to belong to the 
 Quebec group. 
 
 The rocks of this group, here branching off from a range of hills which 
 comes up from Vermont into Canada, take a north-easterly direction, 
 and, crossing Memphramagog Lake, run from the township of Stanstead 
 through Stoke, to Weedon, and constitute the Stoke Mountains, which are 
 bounded on each side by the more recent strata just mentioned. The 
 average breadth occupied by the Quebec group in these hills, seldom exceeds 
 two or three miles, except in Ascott and Stoke. On the St. Francis, 
 in the former township, through the influence of three undulations, the 
 Quebec rocks have a transverse measure of seven miles, extending from 
 the vicinity of Lennoxville to the north-west corner of the township ; and 
 in Stoke, they present two parallel ranges, included in a breadth of about 
 five miles. 
 
 In this range of hills, the strata consist chiefly of chloritic rocks in harder 
 and softer bands, the softer and more schistose constituting chlorite 
 slates, while the harder may be termed chloritic sandstones. With these 
 are associated micaceous and nacreous slates, often presenting a very 
 quartzose character ; and thin layers of agalmatolite of a somewhat fibrous 
 texture, are sometimes met with. Some of the micaceous and nacreous 
 slates are very fine grained, and on the south side of the range afford 
 excellent whetstones and hones. Many of the whetstone beds appear to 
 be micaceous slates, passing into argillite. Some bands of the slates 
 sherbrooke. are studded with chloritoid ; and in Sherbrooke, they inclose a bed of 
 blood-red jasper, passing into silicious red hematite, and another of a 
 somewhat coarse silicious conglomerate. In the same neighborhood, 
 the nacreous slates are marked by the occurrence of copper pyrites, con- 
 taining a little gold and silver, in a gangue of white quartz, running with 
 the stratification. The chlorite slates are often marked by iron and cop- 
 per pyrites ; and on Haskell Hill, on the eighth lot of the eighth range of 
 Ascott, a band of the slate, five feet wide, holds such a quantity of the 
 copper ore as to give promise of a profitable mine. A considerable portion 
 of the Owl's Head Mountain appears to be composed of petrosilex, or an 
 intimate mixture of quartz and orthoclase feldspar. 
 
 On the St. Francis, the breadth of the rocks of the Quebec group on the south 
 side of the lower black shales and limestones, is between four and five miles. 
 The lowest beds in the neighborhood consist of a grey soft very argillaceous 
 sandstone, yielding whetstones ; while some beds not far removed from 
 these, in Shipton, are composed of micaceous rock, somewhat resembling 
 potstone, cracks in which are frequently invested with thin films 
 of carbonate of copper. In Pine Hill, on the south-west side of 
 the St. Francis, the serpentine has a breadth of nearly one third of a mile ; 
 and above the serpentine on both sides of the stream, there occurs a band 
 
CHAP. XL] QUEBEC GROUP. 253 
 
 of very beautiful roofing slate, in which quarries have been opened. Richmond and 
 Between the slate and the serpentine, on the west side of the stream, a thin Cleveland - 
 
 r _ Roofing slates. 
 
 band of anorthic feldspar rock occurs ; and on the east side, white dolomite, 
 penetrated with asbestus, forms reticulating veins in the upper part of the 
 serpentine, some of the veins being five or six inches thick. In the ser- 
 pentine band, near to the roofing slates, is a layer of serpentine about a foot 
 in breadth, containing masses of chromic iron in nodules. 
 
 The serpentine enters Cleveland on the sixth lot of the fifteenth range ; and swpton 
 crossing the lines of the lots at a small angle, it attains the north-west side of Mountain - 
 Shipton Pinnacle Mountain. This hill, which is a narrow ridge, is composed 
 of a coarse conglomerate, in which the pebbles, many of them of two or 
 three inches in diameter, are of various descriptions, some of them con- 
 sisting of anorthic feldspar, and others of a mixture of this mineral with 
 crystals of diallage. In the matrix, there is much chlorite and epidote in 
 spots and patches. Pebbles of red jasper are met with, and patches of 
 it run in the rock. There is also a regular band of red jasper on the 
 south-eastward side of the hill, and a band of anorthic feldspar on the 
 north-west, between the conglomerate and the serpentine. 
 
 The conglomerate ridge is continued in a narrow chain of hills north- 
 east from the Pinnacle, and the band of serpentine is about 400 yards to 
 the north-west of the chain. From this, the serpentine gains West Nicolet 
 or Richmond Lake in Tingwick, where it is represented by an almost 
 unmixed diallage rock, and its course, nearly due east, points for the vicin- 
 ity of Ham Mountain. It is met with about half way to the mountain ; 
 and again on the south side of East Nicolet Lake, where it is associated with 
 workable masses of chromic iron. Ham Mountain, which is about three Ham Moun- 
 miles south-west of the lake, has here the same relation to the serpentine tain 
 as Victoria Mountain in Orford ; of which it is a repetition in almost every 
 respect, with perhaps a small addition in height. 
 
 Ham Mountain is not far removed from the extremity of the Stoke 
 Mountain range, and its position in regard to the range is somewhat anal- 
 ogous to that of the Owl's Head. These two hills, standing at the opposite 
 extremes of a rudely elliptical area, which is nearly surrounded by rocks 
 of the Quebec group, are about sixty-five miles asunder ; while the great- 
 est transverse measure of the area, from the Gosford Road, on the line between 
 Dudswell arid Westbury, to the Danville anticlinal near Shipton Pinnacle, 
 rather exceeds twenty-five miles. The interior of this area, for a breadth 
 of about fifteen miles, is filled with clay slates and fossiliferous limestones of 
 the same age as those of Lake Memphramagog, which indeed belong to 
 this basin. 
 
 From East Nicolet Lake, the serpentine turns northward, and runs along 
 several small lakes, on the line between Wolfestown and Garthby, to 
 the line between Ireland and Coleraine. In these two townships, there 
 
254 GEOLOGY OF CANADA. [CHAP. XI. 
 
 Ireland; is a great display of the rock. It lies on both sides of Black Lake, extend- 
 ine ' ing four miles to the south-west in Ireland, constituting Caribou Hill, and 
 probably two miles to the north-east in Coleraine, with an average breadth 
 of about two miles and a half, thus spreading over an area of about fifteen 
 square miles. On the twenty-first lot of the first and second ranges of Ire- 
 land, about a mile from this area, there is another exposure of serpentine, 
 without any observed rock between the two. What relation these may 
 bear to one another geologically, or what may be the course of the larger 
 mass beyond Coleraine, has not yet been ascertained. 
 
 Wolfestown. On the twenty-eighth lot of the fourth range of Ham, there occurs a band 
 of dolomite, running into Wolfestown, and marked by copper ore dissemi- 
 nated in a breadth of thirty feet. The relation of this dolomite to the serpen- 
 tine is uncertain. In the south corner of Wolfestown, and about six miles 
 from the dolomite, red slates, occurring at intervals on the Gosford Road, 
 appear to occupy a place on the north-west side of the band of serpen- 
 tine. On the south and south-east sides, the serpentine is accompanied by 
 a broad band of diorite, associated with coarse conglomerates, all the way 
 through Wotton, Ham, and Garthby, composing Ham Mountain in their 
 course. Associated occasionally with chloritic and epidotic rocks, it is 
 traceable still farther across Coleraine, Adstock, Thetford, and Broughton, 
 rising into the White Mountain in Adstock and into Broughton Mountain 
 in the township of that name. On the south-east side of this zone, another 
 band of serpentine makes its appearance to the south of Ham Mountain, 
 where it is partially calcareous. Accompanied occasionally with a 
 band of conglomerate, it can be traced across Garthby and Coleraine, where 
 it approaches to within a mile of Lake St. Francis. Associated with it, in 
 the twenty-first lot of the fourth range of Garthby, there is a considerable 
 mass of mingled yellow sulphurets of copper and iron, subordinate to the 
 
 Vaudreuii stratification. An exposure of serpentine occurs on the twenty-fourth 
 lot of the fourth range of Tring. Its precise relation to the previous masses 
 is uncertain, but its strike would carry it to a junction with other exposures 
 on the Bras and the Guillaume, in the seigniory of Vaudreuii Beauce. On 
 the Guillaume, there is a six-feet band of massive white garnet rock in the 
 middle of the serpentine, and a thicker one in contact with it on the south 
 side ; while farther south, there occurs a considerable band of diorite, 
 limited by clay slates which are supposed to be Upper Silurian. Dis- 
 seminated in the white garnet rock of the Guillaume, small grains of 
 gold have been met with. 
 
 Between the serpentine, where it crosses the Chaudi&re and attains the 
 Guillaume, and the lower black slates and limestones of the St. Joseph 
 anticlinal, exposures of red slate, and red and green sandstones, are frequent, 
 for -a breadth of between four and five miles. They have been traced to 
 the north-eastward, across Cranbourne into Standon, a distance of twenty 
 
CHAP. XI.] QUEBEC GROUP. ^ 255 
 
 miles ; and south-westward into Tring, about ten miles. In many parts of 
 this area, there are red colored rocks holding much epidote ; but accom- 
 panying these, are also large masses of epidotic rock with a greenish tinge. 
 On the right bank of the Chaudiere, proceeding north-westward across 
 the measures from the serpentine, after a concealed interval of a quarter 
 of a mile, there is a breadth of nearly half a mile of massive green sand- 
 stone, often conglomerate, which, dipping to the north-westward, becomes 
 interstratified with red slate, and is terminated by a red sandstone bed 
 of twenty-five feet. This is followed by five feet of highly crystalline st. Joseph, 
 red limestone, with patches of red slate, to which succeeds a peculiar 
 rock, which is well seen on the Riviere des Plantes in the seigniory of St. 
 Joseph, near the Chaudiere. It has a general grey color without; but 
 when examined, is seen in many parts to consist of flattened spheroidal or 
 reniform masses, sometimes a foot in diameter, standing on edge in the 
 direction of the strike. They are made up of an indurated purplish red 
 argillaceous rock, which is jaspery in its texture, and sometimes spotted 
 with grams of a soft greenish mineral. When sections of thesp spheroids 
 have been exposed to the weather, they present a concentric arrangement 
 of various shades of color, becoming lighter and greyer toward the exterior ; 
 the whole however being included in a band of deeper red. These masses, concretionary 
 which often have a nucleus of calcareous spar, show a tendency to divide e P idotic rock - 
 in concentric layers with the bands of color. Many of the larger spheroids 
 are traversed by a multitude of cracks, such as are seen in septaria ; and 
 in weathered sections, these cracks are bordered by a dark colored 
 ridge, raised above the rest of the surface. 
 
 The interstices between the spheroids, in some parts of the rock, are 
 filled with a mixture of dark green serpentine, chlorite, pistachio-green 
 ,epidote, white calcite, and occasionally colorless translucent quartz ; the 
 latter four minerals being highly crystalline. The epidote frequently 
 surrounds nodules of calcite. Interstratified between two masses made 
 up of these spheroids, there occurs a reddish schistose rock, which often 
 includes fragments of slate and small brownish jasper pebbles, and weath- 
 ers with a rough discolored surface. This conglomerate runs in bands 
 with the strike of the rock, which has a breadth of nearly 300 yards ; and 
 towards the middle, it includes a portion approaching in its characters to the 
 ordinary red slate of the region. We can scarcely doubt that the peculiar 
 characters of this rock are due to the alteration of layers of concretionary 
 masses like septaria, which were originally included in the red slates. Some 
 parts of this rock resemble the gabbro rossi of the Italian geologists ; and 
 the concretionary portions recall, by their arrangement, the green feM- 
 spathic rock, already described as occurring near the eastern band of ser- 
 pentine in Bolton, in the Missisquoi valley. The general bearing of this 
 epidotic rock is to the north-east, with the strata. It has been traced up 
 
256 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XI. 
 
 Sillery for- 
 mation. 
 
 Shipton and 
 
 Leeds 
 synclinal. 
 
 the Riviere des Plantes for a short distance, and about three miles in 
 continuation, on the road to Cranbourne, where it appears to be wholly 
 green, still retaining its reniform structure. Red and green epidotic rocks, 
 without the reniform masses, occur in different parts of the area which 
 includes the red and green sandstones and shales. 
 
 Many of the beds of these red and green rocks very strongly resemble 
 the strata of the Sillery sandstones, and it is highly probable that this por- 
 tion of the Quebec group is here represented. The area should therefore 
 have a synclinal form ; and in conformity with this, the dips on the opposite 
 sides are towards the centre ; while between the red and green sandstones, 
 and the black slates of the St. Joseph anticlinal, masses of serpentine and 
 dolomite make their appearance in the seigniory of St. Joseph. Similar 
 masses, associated with soapstone, occur in the same relation, farther to 
 the west, in Broughton. On the north side of the synclinal, at the base 
 of the red and green strata in St. Joseph, patches of red limestone are 
 associated with the sandstone and slate. Vitreous sulphuret of copper here 
 occurs, disseminated with talc, chlorite, and ferruginous oxyd of manganese 
 in a bed of quartz running with the strike. 
 
 On the Chaudi&re, the distance between the anticlinal of Sutton and St. 
 Joseph, and that of Stanbridge and the river Bayer, is about fifteen 
 miles. The synclinal between these, from the Nicolet River to the north- 
 eastward, is occupied by strata similar to those described in the same 
 synclinal between this river and the province line ; except that in the 
 vicinity of the Chaudi&re, and farther to the north-eastward, there is 
 a more frequent exhibition of red slates. The undulations subordinate 
 to the synclinal are too numerous to permit the distribution of the strata 
 to be followed out in detail. The general course of the magnesian 
 rocks on the south side of the synclinal, is, however, pretty well deter- 
 mined by a band of dolomite, occasionally passing into serpentine, which has 
 been traced from the thirteenth lot on the line between Chester and Hali- 
 fax, to the Chaudi&re, near the line between St. Mary and St. Joseph seignio- 
 r i es? a distance of about forty-five miles. Chloritic and epidotic rocks 
 occur on the north-west side of the band nearly the whole way ; while 
 dolomites and limestone conglomerates similar to those of Point LeVis 
 appear in many places along the north-west side of the . synclinal, and 
 become very frequent in Inverness, Nelson, Leeds, and the seigniories of 
 St. Giles and St. Mary. Nacreous and chloritic slates, the former often 
 studded with chloritoid, accompany the magnesian belt, and, as well as the 
 dolomites, often contain sulphurets of copper in Chester, Halifax, Inver- 
 ness, Leeds, and the seigniories beyond ; giving promise, in many places, 
 of quantities economically available. 
 
 At Harvey Hill, in Leeds, about two miles south of the stratigraphical 
 place of the main band of dolomite, and immediately near a bed of soapstone, 
 
CHAP. XL] QUEBEC GROUP. 257 
 
 nacreous and chloritoid slates occur, on the seventeenth lot of the fifteenth Leeds; 
 range. In a vertical thickness of about thirty fathoms, they include three c PP erore - 
 beds of from three to thirty inches thick, marked by vitreous, variegated, 
 and pyritous sulphurets of copper. The strata are here intersected by 
 several veins of quartz and bitter spar, running slightly oblique to the 
 strike. Some of these contain available quantities of the same ores ; and 
 in the workings of the English and Canadian Copper Mining Company, 
 they have been found to hold ore to a depth of more than thirty fathoms. 
 These veins are continued to the north-eastward, and similar ones are met 
 with in the Ste. Marguerite range of the seigniory of St. Giles, the distance 
 being about six miles, where they are characterized by the same ores 
 of copper. On the fourteenth lot of the same range of Leeds, a vein 
 occurs, cutting a bed of steatite, and containing, in a gangue of coarsely 
 crystalline bitter spar mixed with talc, copper glance, with specular iron 
 and small portions of native gold. 
 
 From St. Sylvester church in St. Giles seigniory, which is four miles st. aaes. 
 north-westward, across the measures, from the band of dolomite that has 
 been mentioned, there occur, in a transverse breadth of about five miles 
 farther, to the forks of the Beaurivage River, four bands of calcareo-magne- 
 sian conglomerate . Some of these are probably repetitions .of one another ; but 
 their outcrop appears to be due to an anticlinal, which divides the general 
 synclinal basin into two subordinate troughs. The most south-eastward of 
 these conglomerate bands appears to maintain a course about a mile to the 
 north-west of the road from St. Sylvester to St. Mary ; striking the Chau- 
 diere about the same distance below St. Mary church, and proceeding 
 thence to a position on the Etchemin about half a mile below St. Anselm 
 church. 
 
 A short distance south-eastward of this band, there occurs an area 
 occupied by red and green rocks which, probably representing the 
 Sillery series, show the deepest part of the synclinal, and in some places 
 present the same chloritic and epidotic characters as those of Cranbourne 
 and St. Joseph farther south. The area over which these strata occur, com- 
 mences in a point near the Chaudiere ; it has been traced about twenty miles 
 to the north-eastward, across the seigniories of St. Mary and Jolliet, into 
 St. Gervaise, and it probably extends much farther. In St. Gervaise, it 
 lies between the church of St. Lazare and the north line of Frampton, where 
 it has a breadth of about five miles. In the seigniory of St. Mary, it is char- 
 acterized, on its south side, by the occurrence of variegated sulphuret of 
 copper in red slate, in close proximity to a bed of ferruginous magnesian 
 limestone! The distance between this area and its equivalent to the south, Frampton. 
 across the eastern part of Frampton, is about ten miles. In this township, 
 the axis of the St. Joseph anticlinal appears to bear for the highest peak of 
 the mountains in Buckland, about ten miles to the eastward. The strata 
 
 R 
 
258 GEOLOGY OF CANADA. [CHAP. XI. 
 
 of these, although they have not yet been examined, are conjectured to 
 belong to the same part of the Quebec group as the peaks in Orford, 
 Ham, and Adstock, and to be composed of feldspathic rocks. 
 
 Before reaching the axis of the Bayer River anticlinal, two additional 
 areas of red and green rocks, considered to be equivalent to the Sillery sand- 
 stones, are met with in the synclinal of which that axis is the north-westward 
 limit. These lie on the opposite sides of the Riviere du Sud, in the lower 
 part of its course. The southern area extends from the Government road, 
 opposite St. Pierre church in Lepinay, about twelve miles to the south-west, 
 and probably as far to the north-east. It has been examined for a 
 breadth of four miles south-eastwardly, along the road ; and it appears prob- 
 able that to the north-east of St. Lazare, overlying the small anticlinal 
 indicated by the magnesian conglomerates of St. Mary, it may join the 
 St. Gervaise area of Sillery rocks, in their extension into Armagh and 
 Ashburton. The Sillery formation, on the north side of the Riviere 
 du Sud, occupies the chief part of the space between this stream and 
 the St. Lawrence. Its northern limit runs up the valley of the Bayer, 
 and the area extends longitudinally about twenty-three miles, from St. 
 Thomas to the vicinity of St. Charles, in Livaudiere. 
 
 The sandstones, in these two areas on the opposite sides of the Riviere 
 du Sud, are massive ; on the northern side, they are often very coarse 
 grained, and in general of a green color, while the shales which separate the 
 masses are usually red. Very coarse beds are not so frequent on the 
 south side ; and there the red color is not confined to the shales, but charac- 
 terizes the sandstones also, which are as often red as green. Along the 
 valley between the two areas, thick beds of white and grey granular quart- 
 zite, coming from beneath the Sillery strata, are extensively exposed, and 
 frequently enclose bands of a limestone conglomerate with an arenaceous 
 matrix, varying in thickness from one to six feet. 
 
 L'isiet. Quartzites similar to these, are somewhat extensively developed to the 
 north-eastward. About six or seven miles from the margin of the St. 
 Lawrence, at L'Islet, they rise into a considerable ridge, which occupies a 
 breadth of about two miles and a half in the seigniories of L'Islet and 
 Lessard. The quartzites are flanked on both sides by green sandstones, inter- 
 stratified with occasional red shales. On the south side, these appear to con- 
 tinue for between six and seven miles across the measures, and occur again 
 near the province line, about fourteen miles farther on. The interval between 
 these positions has not yet been examined. On the north side of the 
 quartzites, the green sandstones incline somewhat to grey ; and near the 
 St. Lawrence, they display interstratified bands of conglomerate, with 
 calcareous and silicious pebbles. 
 
 The quartzite ridge of L'Islet and Lessard appears to constitute an anti- 
 clinal corresponding with that of St. Joseph. Proceeding north-eastward, 
 
CHAP. XL] QUEBEC GROUP. 259 
 
 the ridge gradually approaches the coast ; and at Ste. Anne de la Pocati&re, 
 about twenty miles below L' Islet, the north side of the quartzites is scarcely 
 more than half a mile removed from the St. Lawrence, where the dip is north- 
 ward at an angle of about thirty degrees. The quartzites are there interstrat- 
 ified with a band of coarse conglomerate not far from a hundred feet thick. 
 Its included masses are calcareous and silicious, and some of them, composed 
 of light grey limestone, are two and three feet in diameter. Near the River 
 mouth of the river Ouelle, there are beds of grey calcareous sandstone, 9 uelle - 
 interstratified with a few layers of grey arenaceous limestone from two to 
 six feet in thickness, associated with occasional red shales. These are sup- 
 posed to be somewhat above the quartzites ; and they are interesting from the 
 fact, that in lenticular layers of limestone conglomerate, enclosed in the grey 
 limestones and red shales, black phosphatic nodules, resembling coprolites, 
 are abundantly disseminated in scattered patches. With these, was found 
 a curious hollow cylindrical fossil, an inch and a half long, and one 
 fourth of an inch in diameter. The smaller extremity is thin, but gradually 
 enlarges from the thickening of the substance, and the other extremity 
 becomes externally somewhat triangular, while the cavity remains nearly 
 cylindrical. The specimen very much resembles a fragment of bone, 
 and is composed of phosphate of lime ; but having no bony structure, it may 
 be part of a Serpulites. As already stated, Serpulites, with similar phos- 
 phatic nodules, occurs in the lower part of the Chazy formation, which prob- 
 ably would not be far above the horizon of this locality at the river Ouelle. 
 
 The quartzites come upon the coast between Kamouraska and St. Andrew ; Kamouraska. 
 and in this vicinity there are several hills, which rise parallel with one 
 another, and appear to be composed of granular quartzite. Just below 
 Kamouraska, the exposures are comprised within the breadth of about two 
 miles and a half; but they are narrower at St. Andrew, near which, at a 
 place designated, from the abrupt rocky eminences, by the name of Les 
 Caps, the width is only a mile. Here the sides and summits of three hills 
 appear to be cased over, in succession, by the same granular quartzites ; 
 the thickness of which, as displayed in one locality, appears to be about 
 200 feet. These hills correspond to three folds in the stratification ; and a 
 fourth one, less prominently shown, is found a little farther from the coast. 
 The Pilgrim Islands, lying off St. Andrew, are also composed of the same 
 rock ; and including them, the breadth of the quartzites would here be about 
 three and a half miles. 
 
 Beds subordinate to the same strata continue to Eiviere du Loup, Temiscouata. 
 many of them being of a conglomerate character ; and between the coast 
 at this point and Temiscouata Lake, a distance of about thirty miles, which 
 is the whole breadth occupied by the Quebec group in this part, no rocks 
 lower than these quartzites make their appearance. At the distances of 
 six and eight miles from the coast, there are indications of repetitions of the 
 
260 GEOLOGY OF CANADA. [CHAP. XI. 
 
 quartzite, very probably brought to the surface on 'two anticlinals ; but 
 none of the limestone conglomerates which are associated with them on the 
 coast, have here been observed. The highest strata of the series observed on 
 this line, occurs at twelve miles from the coast, across the measures, between 
 the Ruisseau des Roches, a branch of Green Island River, which is tributary 
 to the St. Lawrence, and the Little St. Francis, a tributary to the St. John. 
 The distance between these streams, which is four miles, is occupied by the 
 Sillery sandstones, here constituting a very rugged ridge. 
 
 cacouna On the immediate margin of the St. Lawrence, about two miles below 
 
 Riviere du Loup, there is a narrow strip of green sandstones of the Sillery 
 series, extending for about two miles along the shore. Another presents 
 itself a little lower down, including the island of Cacouna, and extending 
 thence to the mouth of Green Island River. It is altogether about twelve 
 miles in length ; and although only half a mile wide, it presents several folds 
 subordinate to a synclinal form. Inside of these positions about a mile, 
 the quartzites, with thin grey calcareous sandstones, grey arenaceous lime- 
 stones, and limestone conglomerates, appear at intervals all the way, with 
 red, green, and black shales both among and above them. Between 
 Green Island River and Metis, a distance of seventy-five miles farther, the 
 coast is occupied by the lower strata only. 
 
 Trois Pistoles. At Trois Pistoles, in a section of 700 feet of strata, 150 feet at the base 
 consist of grey calcareous sandstones and coarse limestone conglomerates, 
 the latter comprising one third of the amount, in nine separate layers of 
 from two to sixteen feet thick. The matrix of the conglomerates is a grey 
 calcareous sandstone ; and the rounded masses imbedded in it, in addition to 
 limestone, consist of quartz, and occasionally of amygdaloidal diorite. Of 
 the limestone and the diorite, there are masses weighing from a pound to a 
 ton, while the quartz pebbles seldom exceed an ounce. The remainder of 
 the strata consists chiefly of red and green shale, with greenish-white com- 
 pact limestone in thin beds, and an occasional band of black shale. 
 Bic Harbor. In the vicinity of Bic Harbor, there is a great display of the limestone 
 conglomerates and their associated grey calcareous sandstones ; and it is to 
 the resistance which these have offered to the destroying agencies that have 
 worn away the other rocks of the coast, that the formation of Bic Harbor 
 is due. A great deal of beautiful structural detail might be obtained 
 in the neighborhood of Bic ; but a very minute investigation of it has not 
 yet been attempted, for want of time. Many of the facts necessary for 
 the complete understanding of the arrangement of the rocks in this district, 
 are still wanting. One point ascertained, however, is the occurrence of a 
 small synclinal area of green sandstones of the Sillery series, which fur- 
 nishes the means of determining the summit of the subjacent rocks around. 
 Bic Point is about two miles below Bic Harbor, and the sandstones in 
 question are met with, about three quarters of a mile inland from the bight 
 
CHAP. XL] QUEBEC GROUP. 261 
 
 of the bay, below the point. The bearing of the synclinal axis is N. 
 65 E., and the area of the sandstone is three quarters of a mile in length 
 by 250 yards in width. The sandstones appear to be surrounded by red 
 and green shales, and the limestone conglomerates come into their proper 
 place on the outside of the shales. The relations of the strata are here 
 better shewn than in many other parts, as the sandstones are comparatively 
 flat, and none of the dips are overturned. 
 
 In the neighborhood of Metis, in a conglomerate band which may be a Metis. 
 continuation of the one at Trois Pistoles, enclosed masses occur, still larger 
 than those already mentioned. The band is altogether about 200 feet in 
 thickness, and consists of various alternations of white granular quart- 
 zite and limestone conglomerate, the proportions being about one half of 
 each. Among the boulders, one of dark grey limestone was measured and 
 computed to weigh twelve tons. Another, which had for a considerable 
 time been quarried for lime-burning, was, when measured, eleven feet long 
 by six feet broad, and was supposed still to contain twenty-five tons of lime- 
 stone. The boulders occur in separate but parallel exposures of the rock, 
 on the opposite sides of an anticlinal, one of them being at the outlet of 
 the Metis River, and the other about half a mile to the south. Both expo- 
 sures dip to the southward at an angle of between thirty and forty degrees ; 
 and the northern dip would thus appear to be an overturn. 
 
 Less than half a mile beyond the southern exposure of conglomerate, 
 there occurs an escarpment of green sandstones of the Sillery series, belong- 
 ing to a synclinal area which extends in a pretty straight course, for thirty- 
 five miles, from the south side of Little Metis Bay to the Rimouski River 
 in the rear of Rimouski seigniory, where its extremity is upwards of five 
 miles from the coast. Its greatest breadth is about two miles ; but on the east 
 side of the Rimouski seigniory it diminishes to a few yards, and farther west 
 increases to about half a mile, while it is probably cut into two parts by the 
 Great Metis River. At the mouth of the Little Metis River, the green sand- 
 stones fold over the axis of the anticlinal, which, as has just been men- 
 tioned, affects the band of coarse conglomerate a little to the south-west- 
 ward, and spread over the peninsula of Metis Point. On the south- 
 east side, they fold over another and parallel anticlinal axis, and extend into 
 a synclinal area, which runs along the valley of the Neigette on the north- 
 west side, crossing the Great Metis River about three miles below the mouth 
 of the Neigette. On the south-east side of the valley of the Neigette, 
 there extends still another parallel synclinal area of the sandstones, com- 
 posing Mont Commis, which has a length of about twelve miles, with a 
 breadth of about two, and is bounded at the north-eastern extremity by the 
 Great Metis River. 
 
 On the Rimouski River, the breadth of the Quebec group does not 
 exceed seven miles; but on the Great Metis, it augments to about 
 
262 GEOLOGY OF CANADA. [CHAP. XI. 
 
 Little Metis sixteen ; while on the Matanne, it is nineteen miles. Between Little 
 River. Metis Bay and Long Point, a distance of thirty-one miles, terminating 
 seven miles below the Matanne, the coast is occupied by the shales inter- 
 mediate between the conglomerates and the Sillery sandstones; with the 
 exception of a point about seven miles below Little Metis Bay, and a short 
 interval about a mile below Little White River, where strata of the Sillery 
 series, belonging to areas that lie under the St. Lawrence, just touch upon 
 the coast. Although there appear to be several small folds in the strata, 
 the coast-line and the strike seem nearly to coincide the whole way, and 
 most of the exposures consist of red, green, and black shales, which are 
 not far below the base of the Sillery formation. In one or two places, 
 however, the summit of the limestone conglomerates and calcareous 
 sandstones of the LeVis formation is exposed. Black shales near the 
 Tartigo River, display fragments of encrinites and broken shells, which 
 are too obscure to be determined. 
 
 Basins of Between Long Point and the river Marsouin, there is a distance of about 
 formation s i x ty" tnree niiles. In this, the coast-line intersects longitudinally four 
 synclinal areas, occupied by green sandstones of the Sillery series, with 
 occasional interstratified red shales. The first extends nearly twenty 
 miles, from Long Point to the vicinity of Les Crapauds, with an additional 
 mile inland at the eastern extremity, and has a breadth of between one 
 and two miles. The second, with a length of four miles between the Little 
 Michaud and Great Capucin Rivers, is a mere strip, with a breadth scarcely 
 exceeding a quarter of a mile. The third, between Cape Chatte and the 
 mouth of the Chatte River, with a length of four miles on the coast-line, is 
 extended in the interior, across and beyond the Chatte, about two miles more. 
 The fourth, with a length of eight miles on the coast-line, extends in the 
 interior about a mile farther each way, and has a breadth of perhaps three 
 miles, forming a mountain of about 1000 feet in height. The whole of 
 these areas are probably in the run of one synclinal ; subordinate to which, 
 in the first and last basins, there is an undulation dividing them each into 
 two troughs. The dips on the south sides of the whole appear in gen- 
 eral to be overturned. 
 
 Long Point. The sandstones in these four areas are usually green, weathering to 
 a drab, and are in general massive. The beds exposed about a mile 
 below Long Point are from six inches to six feet thick, and very even. The 
 rock composing them is fine grained ; and while the main body of it appears 
 to be free from carbonate of lime, there are included portions of various 
 shapes and sizes, from one to several inches in diameter, which are 
 calcareous. The sandstones, at irregular intervals, are interstratified with 
 red and green shales, which include greyish-green layers of from one to 
 six inches thick, weathering whitish-yellow, and probably magnesian. The 
 red shales are spotted and striped with green, and the green with red. 
 
CHAP. XI.] QUEBEC GROUP. 263 
 
 The coast along this mass of Sillery rocks is bold and rugged, and for the 
 most part inaccessible. At Whale Point, it rises into a bold headland, 
 which presents a vertical face of about 150 feet to the St. Lawrence, and 
 immediately inland attains a height of probably 800 feet. 
 
 As seen in the lowest area, the sandstones are a mixture of grains of 
 quartz and feldspar, with sometimes a little mica. They are in general 
 moderately fine grained, but occasionally rather coarse, and sometimes 
 approach the character of a fine conglomerate ; containing small pebbles of 
 white quartz, a few of calcspar resembling worn crystals, and sometimes a 
 larger number of small flat pebbles of black slate, with a few soft opaque 
 white flakes like kaolin. The rock frequently encloses arenaceous spheres of 
 various sizes, up to six inches in diameter, which are harder and lighter 
 colored than the mass. Under the influence of the weather, it becomes 
 pitted with deep holes of various shapes and sizes, having thin, but 
 well marked divisions between them, arising probably from an unequal 
 distribution of calcareous matter. The stone is rather soft, and appears 
 to wear away rapidly. When the strata are vertical or nearly so, the 
 action of the sea between high and low water marks divides them into 
 pillars, sometimes thirty feet in height and four or five across, which are 
 usually smaller at the base than at the summit, producing occasionally 
 a very picturesque effect in the landscape. Two of these pillars stand Cape 
 near a small fishing station below Ste. Anne des Monts, called from 
 them, Cape Tourelle, and the remains of many more are visible in the 
 vicinity. One of a similar description occurs at the lower end of the second 
 area of sandstones, near the mouth of the Capucin River. 
 
 The intervals on the coast between these four areas are for the 
 most part occupied by the red, green, and black shales which imme- 
 diately underlie the Sillery strata, and occasionally, as at the mouth of the 
 Great Capucin River, contain yellow sulphuret of copper. In some parts, the 
 still lower limestone conglomerates are very conspicuously displayed. The LesCrapauds. 
 chief of these exposures are at Les Crapauds and Les Islets, which are 
 both between the first and second areas, and at a prominent point east of 
 the Chatte River, between the third and fourth. The exposure at Les 
 Crapauds displays a thickness of nearly 700 feet ; the whole of which, with 
 the exception of twenty feet of black shale at the bottom, consists of light- 
 grey slightly calcareous sandstones, resembling quartzite, and of limestone 
 conglomerates, interstratified with one another in masses varying in thickness 
 from six to one hundred and fifty feet. A mass of conglomerate towards 
 the top presents pebbles and boulders of compact grey limestone, weigh- 
 ing from an ounce to several tons, with smaller masses of black limestone, 
 and occasionally masses of amygdaloidal diorite, weighing from one to 
 thirty pounds. One layer of the grey sandstone, towards the bottom, is 
 137 feet thick, without any observed subdivisions into beds. 
 
264 GEOLOGY OF CANADA. [CHAP. XI. 
 
 Les islets. The exposures at Les Islets consist of the same grey calcareous sand- 
 stones, composed of translucent colorless quartz grains of the size of pin- 
 heads, cemented together by calcareous matter. The beds are from one 
 to two feet thick. The sandstones are interstratified with an equal and per- 
 haps greater amount of beds of conglomerate, from one to three feet 
 thick ; consisting of rounded and flattened masses of compact grey and black 
 limestone, in a matrix of calcareous sandstone similar to that of the beds. 
 Cracks in these strata are often filled with a black carbonaceous mineral 
 resembling coal, which is identical with the altered bitumen of the island of 
 Orleans. Among these rocks are interstratified deep brownish-black shales, 
 with obscure graptolites, resembling some of those of Point LeVis. The 
 coast composed of these sandstones and limestone conglomerates, is, in 
 these localities, very rough and broken ; but though a somewhat bold cliff 
 rises from the beach, the country inland is moderately smooth, 
 chatte The rocks at the point east of the Chatte River, though considered to be 
 
 Kiver. immediately or proximately equivalent to the preceding masses, are some- 
 what different in character. They consist of a bed of grey oolitic limestone 
 of about twelve feet thick, followed by a thinner one of limestone conglom- 
 erate, and a mass of thin bedded, dark grey, yellow-weathering and probably 
 magnesian limestone, interstratified with thin bands of black bituminous 
 shale, and occasionally with thicker beds, holding large calcareo-arenaceous 
 nodules. These are very conspicuous in a bed of bituminous argillaceous shale 
 at the top, where the nodules resemble septaria, and are occasionally com- 
 posed of dark olive-grey chert, weathering to a dingy red ; in which cracks or 
 veins hold the black carbonaceous mineral mentioned above. These beds are 
 altogether about 240 feet thick ; and some of the black shales hold Phyllo- 
 graptus, one of the genera of graptolites found at Point LeVis. They are 
 followed by a series of argillaceous shales, which are green for about fifty 
 feet at the bottom ; red, striped and partially spotted with green, for 230 
 feet in the middle ; and green, striped with red for' 120 feet, at the 
 top. Upon these shales rests an unequal grey oolitic conglomerate 
 limestone bed, sometimes twenty feet thick ; followed by alternating 
 beds of black shale and light and dark grey sandstones, in some of 
 which specks of blende appear. To these succeed green shales striped with 
 black ; then very pyritiferous black shales, and alternating with them at 
 the top, thin grey calcareous sandstones and arenaceous limestones, termi- 
 nated by another band of grey oolitic limestone conglomerate, and one of 
 grey coarse grained calcareous sandstone. The thickness of this part may 
 be 500 feet, and of the whole mass about 1140 feet. Red, green, and 
 black shales and limestone conglomerates occur for several miles up from 
 the coast on the Matanne, the Chatte, and the Ste. Anne, in places which 
 would indicate the continuance of such strata along the south side of the 
 general synclinal holding the four areas of the Sillery series. None of 
 
CHAP. XL] QUEBEC GROUP. 265 
 
 the exposures however show such important masses of conglomerate as those 
 on the coast. 
 
 The Shickshock mountains, between the Matanne and Ste. Anne 
 Rivers, have a length of about sixty miles, with a breadth at the south- mountain8 - 
 west end of about five miles ; and opposite Ste. Anne des Monts, of about 
 nine miles. The axis of the range is nearly parallel with the coast of the 
 St. Lawrence, from which the north-westward flank is about sixteen miles 
 distant, opposite Long Point, and eleven miles on the Ste. Anne. As already 
 stated, their main peaks rise to heights ranging from 3000 to nearly 4000 
 feet above the St. Lawrence, and more than 2000 feet above the country 
 on each side. The whole range appears to possess a synclinal structure, with 
 an undulation along the middle, dividing the basin into two subordinate 
 troughs. The rocks of the range are composed in great part of epi- 
 dosite, which is an intimate mixture of epidote and quartz. Their general 
 color is yellowish-green, passing occasionally to olive-green, with a hard- 
 ness and texture like that of jasper. They sometimes present the ap- 
 pearance of a close grained green sandstone, in which the beds would 
 be obliterated were it not for fine lines of discoloration. In some parts, the 
 green rock is mottled with red. The existence of fragments of jaspery 
 red slate, which have been found in this vicinity, makes it probable that 
 there are strata of this character. Some of the beds are chloritic as well 
 as epidotic, and portions display a fibrous structure, breaking into hard 
 long splinters ; while others have the character of mica schist, and split 
 into plates, whose surfaces are covered by scales of mica. Beds of black 
 highly crystalline hornblende rock, of a slaty structure, and holding red 
 garnets, are occasionally met with ; and large fragments composed of white 
 quartz and red feldspar, indicate the existence of such a rock in the vicinity, 
 but whether hi beds or veins, is uncertain. 
 
 Close along the southern base of the Shickshock range, rocks appear 
 which belong to the unconformable Middle Silurian series ; but along the 
 northern base, the limestone conglomerates and their associated strata 
 seem to prevail. These are seen on the Matanne River, between its 
 tributaries the Little Matanne and the Trout ; and the general strike of 
 the measures would bring them out in front of the mountains, two 
 or three miles from their base. A mile and a half below the Trout 
 River, slaty epidosites occur, similar to those of the mountains, and most 
 probably a continuation of them. Along that part of the Ste. Anne River, 
 whose upward course turns east and runs close along the foot of the moun- 
 tain range, exposures of limestone conglomerates occur at moderate inter- 
 vals, for a distance of about thirteen miles. Although none of these have 
 been met with on the Chatte River, where it approaches the range and 
 runs parallel with it, sandstones are met with in the lower part of the 
 
266 GEOLOGY OF CANADA. [CHAP. XI. 
 
 mountain flank, which may be equivalent to those so often associated with 
 the conglomerates on the coast. 
 
 stratified At the eastern extremity of the Shickshocks, there is a great display of 
 serpentines. gerpenftne, w hich appears to come in above the limestone conglomerates, 
 with a thin band of black slate between, and to sweep round to the south- 
 eastern shoulder of the range, composing Mount Albert, one of the main 
 peaks. It continues south-westward for a considerable distance, along a 
 tributary of the Great Cascapedia River, there constituting the southern 
 flank of the range ; and it finally disappears beneath the Middle Silurian 
 series farther on. The thickness of this great mass of serpentine is 
 estimated to be about 1000 feet. The whole of it presents evidences 
 of stratification, in some parts remarkably clear and distinct, in 
 others more obscure. Much of the lower 600 feet is bottle-green in 
 color, with beds towards the top, of a streaked and mottled reddish and 
 greenish brown, much studded with small crystals of diallage. The upper 
 400 feet display the bedding very beautifully, by differences of color OH 
 the weathered exterior, as well as in freshly exposed surfaces. The weath- 
 ered surfaces are marked by a set of red and opaque white bands, the 
 white broader than the red ; varying from the eighth of an inch to an inch, 
 and becoming often interstratified with layers of a brownish-fawn color, 
 which vary in breadth in the same way. When cut and polished, 
 this serpentine displays dark brown parallel bands, with thin blood-red 
 vein-like lines, running through those which are red on the weathered 
 surface. These red lines are sometimes disposed after the manner of false 
 bedding. Very thin parallel bands of asbestus are found separating the 
 red layers, together with occasional crystals of diallage : both of these, in 
 certain lights, give golden-red reflections. With the red bands, chromic 
 iron ore is associated, which is sometimes diffused in grains along the 
 layers. Occasionally minute faults displace the layers ; and where they 
 cross those which contain chromic iron, the fissures connected with the 
 fault are filled with the ore, for some distance on each side. Beds of 
 chromic iron, of two and three inches in thickness, are met with in several 
 parts ; and somewhat above the well stratified serpentine, the ore occurs 
 on the surface in considerable quantity, in large loose angular blocks ; 
 which are traceable on the strike for some distance, showing that workable 
 masses are probably imbedded in the rock. 
 
 Lower Between the conglomerates south of the sandstones of the Sillery series, 
 slates near * ne ^* Lawrence, an ^ those nearer the Shickshock range, there is an 
 interval, seen alike on the Matanne,the Chatte,and the Ste. Anne Rivers, in 
 which the prevailing strata are black and dark grey slates, with bands of 
 dark colored limestone. To the eastward of the Ste. Anne, the breadth 
 occupied by these, increases towards the Marsouin River, the south boundary 
 of them gradually sweeping round parallel with the base of the Shickshock 
 
CHAP. XL] QUEBEC GROUP. 267 
 
 range, until they come up against the northern part of a great mass of 
 trachytic granite, at a distance of fifteen miles from the St. Lawrence. Here 
 they are overlaid by nacreous slates, holding chloritoid ; while their northern 
 limit, on reaching the Marsouin, turns down towards the coast, and comes to 
 within a couple of miles of it. These black and dark grey slates and lime- 
 stones are supposed to be those which underlie the Quebec group, and to 
 be here brought to the surface on an anticlinal between two synclinals^ 
 each of which has overturn dips on the south side. The metamorphic 
 strata of the Shickshock range may represent some of the finer grained 
 masses which overlie the limestone conglomerates of the Le*vis formation, 
 but it is uncertain whether they include any part of the Sillery division. 
 
 On the Marsouin, about a mile and a quarter from the coast, there is a 
 set of grey calcareous sandstones, which, running along the strike to the Kiver * 
 east, come out upon the St. Lawrence, and run along the coast for several 
 miles. The beds are from two to three feet thick, and some of them are 
 coarse grained, holding little pebbles of black and grey schist, small 
 translucent fragments of blackish quartz, with others of black shale 
 and brownish-weathering magnesian limestone. These sandstones are fos- 
 siliferous ; but the fossils, which consist of fragments of brachiopods, are too 
 obscure to be easily determined, though some of them resemble Leptcena 
 sericea and Orthis testudinaria. The sandstones are interstratified with 
 black shales holding graptolites, one of which appears to be G-. pristis. 
 On a small island at the mouth of the. Marsouin, beds of black and green 
 compact jaspery rock are met with, very similar to those previously 
 mentioned as occurring on the St. Lawrence, about a couple of miles above 
 Cape Rouge. They are there associated with the black graptolitic shales Hudson 
 of the Hudson River or Utica formation, and the fossils would seem to indicate ? iver 
 
 lonnatioii. 
 
 that these strata at the mouth of the Marsouin belong to one of these forma- 
 tions. Black shales holding abundance of graptolites, and among them r. 
 pristis, are exposed on the beach a little way above the Marsouin, while in 
 the cliff near by, red and olive-green shales, accompanied by brownish- 
 black dolomites, are supposed to belong to the Le*vis formation. The 
 strata are very much twisted ; and it appears probable that we have here a 
 continuation of the fault, and of the contact between the Hudson River for- 
 mation and the Quebec group. As the Hudson River strata on the eastern 
 side of the Marsouin appear to range farther south than those on the 
 west, it is probable that a dislocation runs up the valley of this tributary, 
 and may have some connection with the intrusion of trachytic granite, 
 against which the lower black shales partially abut, farther to the south. 
 
 This mass of trachytic granite extends probably eighteen miles to the 
 southward, with a general breadth of about four miles. About midway, 
 a spur appears to project for ten miles to the westward, crossing the 
 Ste. Anne, and coming against the serpentine at the southern base of 
 
268 GEOLOGY OF CANADA. [CHAP. XI 
 
 intrusive the Shickshock range. The granite forms a table-topped mountain, which 
 gramte. - g ^^ ' n j^g]^ t some of the main summits of the Shickshocks ; and 
 thus, although its axis is at right angles to the bearing of those mountains, 
 it appears to terminate the range, by falling about 1000 feet on the 
 east side, to the general level of the country beyond. This table-topped 
 mountain gives rise to the northern and middle branches of the Magda- 
 len River, and perhaps also to the south branch, the source of which has not 
 yet been ascertained. It appears probable that this mountain will be found 
 to come against Upper Silurian limestones at its south end ; but on the 
 east side, which is nearly straight, it is flanked by the black shales and 
 limestones which are supposed to underlie the Quebec group. These 
 extend at least as far south as the middle branch, with a breadth that 
 does not quite reach the junction of this with the north and south branches, 
 being about three miles. 
 
 Magdalen From the union of these three branches, to within about ten miles of its 
 River. niouth, the Magdalen runs altogether upon the conglomerates and other asso- 
 ciated rocks of the Quebec group. Of the last ten miles of its course, the 
 upper five miles present no exposures ; but in the lower five, there appears a 
 series of strata, consisting of black shales, interstratified with thin bands of 
 black dolomite, which yield an excellent hydraulic cement, and are accom- 
 panied by hard grey calcareous sandstones. The sandstones, where a part 
 of them come out upon the coast somewhat below the mouth of the river, 
 present two coarse grained beds about ninety feet apart, and each fifty feet 
 thick, which hold fossils. Among these can be recognized Stromatopora 
 fibrosa, Leptcena sericea, Orthis testudinaria, and fragments of what is 
 probably 0. plicatella, while Q-raptolithus pristis occurs in the accom- 
 panying black shale, leaving little doubt that these strata belong to the 
 Hudson River formation. We have seen that between these, and the rocks 
 of the Quebec group, upon the Magdalen, there is an interval of five miles, 
 in which the strata are concealed. It is not improbable that a portion of 
 this space may be occupied by an eastward continuation of the lower 
 black shales. Through this interval, too, runs a continuation of the great 
 break between the upper and lower parts of the Lower Silurian series. 
 
 Sandstones and shales, holding the fossils of the Hudson River forma- 
 tion, already mentioned, occur on the coast ten miles above the mouth of 
 the Magdalen ; and as the coast section all the way to the Marsouin presents 
 no great variety in its lithological aspect, it is reasonable to suppose that 
 the rocks are all of one age. The area between the coast and the Mag- 
 dalen has not yet been sufficiently examined to enable us to determine 
 the precise limits between the lower black shales and the Hudson River 
 formation, on the one hand, and between these same shales and the 
 Quebec group, on the other. 
 
CHAP. XL] QUEBEC GROUP. 269 
 
 From the Magdalen, almost to the extremity of Cape Rosier, a distance of Hudson 
 about fifty-five miles, the rocks of the coast possess the same lithological J 1 ^ 
 character as those of the thirty-five miles to the Marsouin. They consist of 
 black bituminous argillaceous graptolitic shales, interstratified with grey cal- 
 careous 'sandstones, and thin dark grey and black yellow-weathering dolo- 
 mites, with thicker black limestones in some parts. These rocks probably 
 belong to the Hudson River formation. Undulations in the strata appear 
 to be frequent the whole way from the Marsouin ; and instances of them 
 are visible along the shore, wherever points or indentations afford 
 transverse sections. At the mouths of a few of the chief valleys, 
 such sections are laid bare in the sides of mountains, which come 
 close upon the water, and rise to heights of 800 and 1000 feet. 
 An instance of this kind is seen on the east side of the river Pierre 
 (called the Claude on Bayfield's chart), where the summit of the hill shows 
 an overturn dip ; and the strata in the whole section, as viewed from the 
 opposite side of the cove, appear to be arranged in the form of a very flat Z . 
 There is one of less importance at Pointe Corbeau, on the upper side of 
 Mont Louis Cove ; and a third, of a striking character, in the mountain east 
 of the Grand Matte River. Minor undulations may be seen at each of the 
 two points next above Great Pond River ; and again at the points above 
 and below Little Fox River, and at that above Great Fox River. It is prob- 
 able that the last three examples, occupying a distance of six miles, are all 
 on the run of the same flexure, which in some parts exhibits an inversion 
 of the beds. 
 
 Many transverse cracks occur in the strata, accompanied by dislocations, Dislocations, 
 usually of small amount. One, however, which is seen near a point 
 a short distance below a brook called the Grande Coupe, four miles and a 
 half below Great Pond River, runs S. 20 W., obliquely across a thick 
 vertical bed of arenaceous limestone, and throws the measures 120 yards 
 northward, on the east side. On account of these undulations and disloca- 
 tions, it is not easy to arrive with certainty at the thickness of the Hudson 
 River strata along this coast ; but from some of the exposures, it appears 
 probaMe that it may equal about 1500 feet. 
 
 Below the Magdalen, the breadth of the formation has been ascertained by 
 transverse sections in two places only ; one of them being at the Great Pond 
 River, where it is about two miles, and the other at Griffin Cove, where 
 it is less. Approaching Cape Rosier, the breadth gradually diminishes ; 
 and the Hudson River strata finally disappear under the waters of the Gulf, 
 at Anse a la Tierce. The remainder of the distance to Cape Rosier is occu- 
 pied by the grey calcareous sandstones, red shales, and limestone con- 
 glomerates of the Quebec group. 
 
 In the Great Pond section also, the rocks which succeed to the Hudson 
 River strata, belong to the Quebec group, and they prevail for a breadth of 
 
Cove 
 section. 
 
 270 GEOLOGY OP CANADA. [CHAP. xr. 
 
 Great Pond about eleven miles, before becoming covered up by the Upper Silurian 
 section. limestones. Two miles in the middle of this section are occupied by sand- 
 stones of the Sillery series, with the red shales which usually accompany 
 them. The dips on both sides of the area occupied by these sandstones, 
 are to the southward; the inclination on the north side being fifty-one 
 degrees, and that on the south side, sixty-four degrees. It is probable, 
 however, that the strata are arranged in a synclinal form, and that those 
 on the south side are inverted : the general synclinal probably contains 
 several subordinate undulations of a similar character. The rocks on 
 each side of the sandstone appear to belong to the Le*vis formation : some 
 of the masses on the south side resemble the magnesian conglomerate 
 bands of Point LeVis. Towards the end of the section, on the south side, 
 chloritic and nacreous slates appear, and in the last mile rise into a con- 
 siderable hill, and are associated with a band of blackish-green serpentine, 
 "weathering to brownish-red, and supposed to be about 120 feet thick. 
 Like all the serpentines of the Eastern Townships, and of the Shickshock 
 mountains, this rock contains chromium and nickel. 
 
 Griffin On the section from Griffin Cove, at the distance of two miles south- 
 westward from the coast, about one eighth of a mile is covered with large 
 angular fragments of greenish sandstone, some of which are fine conglom- 
 erates, with quartz pebbles as large as peas. None of this rock has been 
 seen in place ; but the abundance and angularity of the fragments leave 
 little doubt that the beds cannot be far removed. The position of the 
 fragments may therefore be assumed as that of the Sillery sandstones, 
 particularly as they occur in what would be a continuation of the axis of 
 the Sillery synclinal on the Great Pond section. Between the position 
 of these sandstones and the Hudson River strata on the coast, there would 
 be room for the rocks of the Le*vis formation ; but none of them have been 
 there observed. Half a mile from the south-west side of the sandstones, 
 however, loose fragments of black slate and grey slightly calcareous sand- 
 stone, resembling those associated with the limestone conglomerates, cover 
 the bed of a brook in great abundance ; while half a mile farther south- 
 ward, at about five miles from Griffin Cove, large masses of conglomerate 
 are traceable for 200 yards each way on the strike. The conglomerate 
 consists of white quartz pebbles, some of them an inch in diameter, with 
 others of grey arenaceous limestone and yellowish-white feldspar, imbed- 
 ded in a greenish and strongly calcareous sandy base. A quarter of 
 a mile beyond these masses, the Quebec group becomes covered up by 
 strata belonging to the Gasp limestones, of Upper Silurian age. 
 
 Between Cape Rosier and the base of the Gasp6 limestones, a sudden 
 turn in the coast gives a natural section, nearly at right angles to the 
 strike, of two miles and a quarter in length. The coast is low and shelving, 
 and the violence of south-eastern storms has heaped upon it a great mass of 
 
CHAP. XL] QUEBEC GROUP. 271 
 
 grey limestone shingle, which covers nearly the whole of it, with the cape Rosier, 
 exception of three points. One of these ia Cape Rosier itself, where a 
 breadth of 450 yards of the strata, including what are seen between high 
 and low water-marks, is exposed. The strata consist of grey limestones, in 
 beds varying from six inches to a foot in thickness, with two thicker con- 
 glomerate beds, made up of grey limestone pebbles in a calcareous matrix, 
 very much resembling'the conglomerates of Ste. Anne des Monts ; the whole 
 interstratified with black and grey shales. Separated from the strata of the 
 cape by an interval of 1000 yards, covered by limestone shingle, there occur, 
 at the next point exposed, grey yellow-weathering limestones, probably 
 magnesian, interstratified with jet-black and gray shales, with a band of 
 conglomerate or brecciated limestone on the north-east side. The distance 
 across the strata is about 800 yards ; but there are intervals of concealment 
 in it, making up 300 yards of the amount, and, though the dip is 
 pretty uniform in direction to the south-west, there are variations in tite 
 inclination, which ranges from forty-four to sixty degrees. Another interval 
 of concealment occurs, of about 1000 yards across the measures ; but a partial 
 exposure at the end of the distance shews a continuation of the same alterna- 
 tion of shales, limestones, and sandstones. Red, purple, black, and olive-green 
 shales succeed, associated with grey sandstones ; some beds fine-grained 
 and close in texture, and others coarse with transparent quartz, silvery 
 mica, white feldspar, and very minute bright green grains, probably 
 of glauconite. A few thin layers of black bituminous limestone are 
 interstratified among the shales. Several corrugations are visible in a low 
 cliff, in which these beds are exposed ; but the measurement across the shales 
 is about 350 yards, and the dip, which is south-westward, varies in inclmar 
 tion from twenty-six to ninety degrees. 
 
 Between these beds and the base of the Gaspe* limestones, there is a 
 distance of about 800 yards, across the shales ; but the strata are only 
 obscurely seen at intervals at the beginning and end of the measurement. 
 The strike appears to be uniform, being N. 62 W. ; but only the extreme 
 edges of the beds are anywhere seen, and the dip is sometimes to the one 
 side and sometimes to the other, at inclinations varying from fifty to ninety 
 degrees. The strata consist of black shales and thin limestones, which 
 become somewhat arenaceous towards the south side ; and the last beds, 
 seen immediately in contact with the overlying Gaspe* limestones, are 
 of jet-black shale, yielding a black powder. This has induced some of the 
 fishermen of the place erroneously to suppose that coal cannot be far 
 removed. The rocks occupying these 800 yards most probably represent 
 the black shales and limestones which underlie the Quebec group. 
 
 Between Memphramagog Lake and the Chaudiere, portions of the 
 Quebec group appear through the Upper Silurian or Devonian strata 
 in two or three places, which will hereafter be mentioned in describing these 
 
272 GEOLOGY OF CANADA. [CHAP. XI. 
 
 newer rocks. The only other place in the eastern part of the province 
 in which any part of this group is at present known, is on the Bay of 
 Chaleurs. Thirteen miles of the coast, extending from the lagoon 
 of Grand Pabos to the south side of Cape Maquereau (with the exception 
 of a small patch belonging to the Carboniferous series, at a point called Jar- 
 din a Naveau), are occupied by a great mass of sandstones. Most of these 
 are grey or greyish-green, while some parts towards the Pabos side have a 
 light red or rusty-brown tinge. The sandstone has often a glazed or 
 vitreous aspect, and many of the beds contain white translucent quartz 
 pebbles, of the size of .swan and partridge shot. There are no coarse 
 conglomerates. The whole mass is more or less associated with bands of 
 slate, which often split with glossy surfaces, in the direction of the beds. 
 They are occasionally somewhat micaceous, and sometimes of a talcoid or 
 nacreous aspect, and present various shades of grey passing to black. 
 CapeMaque- Approaching Cape Maquereau, the proportion of sandstones augments, 
 and the crystalline condition of the rock gradually increases, until, in 
 the immediate vicinity of the cape, it assumes a highly metamorphic 
 Altered character. Layers of reddish crystalline feldspar, occasionally with white 
 quartz, occur in some beds ; while others, of a slaty character, split into 
 glossy talcoid laminae. A considerable portion of the rock is of a dark 
 green color, with the aspect of an imperfect greenstone or diorite. The 
 breadth of the belt composed of these rocks, is about seven miles, in a 
 straight line across the strike. The stratification is in general well 
 defined in the whole breadth ; and the courses of the streams from the inte- 
 rior, show that a uniform strike is maintained for some distance. The 
 direction is, with little variation, a few degrees south of west ; but the 
 dip, which ranges from forty-five to ninety degrees, is sometimes to the 
 one side and sometimes to the other. In a large proportion of the dis- 
 tance, however, it seldom varies more than from ten to twenty degrees 
 from the perpendicular. That there are undulations in these strata, is very 
 probable ; but if they exist, they are very sharp, and the rock is so uniform 
 in its character, that it would be difficult to determine their position, not- 
 withstanding that there are very few intervals of concealment in the whole 
 distance. The more highly altered strata of the cape are as near as 
 possible vertical; and in that attitude they run along the shore, which is 
 nearly in the strike, from the extremity of the point, towards Anse a la 
 Vieille. Here they are seen to be unconformably overlaid by an Upper 
 Silurian limestone, which in its turn supports an unconformable Carbon- 
 iferous conglomerate. These sandstones of Cape Maquereau strongly 
 resemble, in many parts, those of the Sillery series, to which they are 
 probably equivalent. 
 
 Deschambauit It has been stated in a previous chapter, that what has been called the 
 anticlinal. Peschambault anticlinal, brings to the surface, between St. Dominique and 
 
CHAP. XI.] QUEBEC GROUP. 273 
 
 Farnham, strata of the Trenton, the Birdseye and Black River, and the Trenton and 
 Chazy formations ; the exposures being almost wholly confined to a com- 
 paratively narrow strip on the east side of the anticlinal axis. The dis- 
 tance between the two extreme exposures is about twenty-five miles, and 
 the bearing of the axis, in this distance, is about S. 15 W. If continued 
 in the same direction for eighteen miles farther, it would reach Missisquoi 
 Bay on Lake Champlain, and run under the waters of this bay about 
 three quarters of a mile west of Phillipsburgh. From this, a gentle turn 
 a little more southward, would carry it, in four miles farther, to the shore 
 of the same bay, near the Franklin House, at Highgate Springs in Vermont. 
 At this spot, strata similar to those of St. Dominique, are brought to the 
 surface by an anticlinal, which may not improbably be a continuation of 
 that of St. Dominique and Farnham. 
 
 As already mentioned, the band of Trenton limestone running between 
 these two places, is only about a mile from an exposure of the Sillery 
 division of the Quebec group, on the Barbue. The dip of the limestone 
 is to the eastward ; and between it and the Sillery rocks, there would be 
 room for portions of Utica and Hudson River strata. Deposits lithologically 
 resembling some of those of the Hudson River, do occur in the interval, 
 but no fossils have been found in them to aid in determining their horizon. 
 The exposures of the Trenton band in this part, reach farther south than 
 those of the Chazy ; and approaching Farnham, their breadth gradually 
 diminishes, until they terminate in a point, not far from the Yamaska 
 River. This arrangement would seem to indicate a gentle slope on the 
 crown of the anticlinal : this would probably bring in higher strata farther 
 south, from beneath which the Trenton limestone would rise again in Mis- 
 sisquoi Bay, to join the exposures near Highgate Springs. The natural 
 inference, unless fossils were found to contradict it, would be, that on the 
 axis of the anticlinal, between Farnham and Highgate Springs, we should 
 find the Utica and Hudson River formations. 
 
 The lowest rock brought to the surface on the anticlinal at Highgate 
 Springs, is a dove-grey limestone, similar to that of St. Dominique. It Sprin s s - 
 occurs on what is considered the axis of the anticlinal, near a wharf and an 
 old lime-kiln, on the shore of the bay, less than half a mile northward from 
 the Franklin House. It is associated with bands of brownish-grey, buff- 
 weathering dolomite, from one to three feet thick, and is flanked on both 
 sides by greenish-grey calcareous fine grained sandstones. These on the 
 west side of the axis have a thickness of probably between fifty and a 
 hundred feet, becoming at the top interstratified with greenish shale. No 
 fossils have been found in the dove-grey limestone ; , but in the upper part 
 of the sandstone there occur one or two undetermined species of trilobites, 
 probably of the genus Asaphus. These sandstones are followed, on each 
 side, by blackish thin bedded shaly nodular limestones, partially magnesian. 
 
 s 
 
274 GEOLOGY OF CANADA. [CHAP. XI. 
 
 They are fossiliferous, but the species do not appear to be numerous. Among 
 tlon ' the fossils met with on the east side are Ptilodictya fenestrata, Orthis 
 platys, and Ampyx Halli, all Chazy species ; the last, already mentioned 
 as occurring in the Chazy limestone at St. Dominique. The thickness of 
 these shaly beds is not certain, but they probably exceed sixty feet. 
 
 The shaly nodular beds are followed, on each side, by about thirty feet 
 of massive black limestone. Southward from the lime-kiln, these bands, 
 
 278. BRACHIOPODA (CHAZY?) 
 
 278. Lingula Perryi (Billings) ; dorsal valve. 
 
 which are about 300 paces apart, run parallel with one another for some 
 
 distance inland ; and then gradually curve round so near one another, as to 
 
 make it probable that they may join not far beyond the spot where they 
 
 Black River become concealed. Both bands hold masses of black chert ; that on the 
 
 lon ' west contains Orthoceras recticameratum, 0. anellum, and 0. Allumet- 
 
 tense; while that on the east has Columnaria alveolata, Stromatopora 
 
 rugosa, Petraia profunda, Helicotoma planulata, Murchisonia peran- 
 
 gulata, and Orthoceras Bigsbyi ; leaving little doubt that these beds 
 
 279. CKU8TACEA (CHAZY). 
 
 279. Ampyx Haiti (Billings); a, head; 6, pygidium; c, side view. 
 
 represent the Birdseye and Black River formation. These black calca- 
 reous bands are succeeded, on each side, by a series consisting chiefly of 
 Trenton black thin bedded shaly nodular limestones, interstratified occasionally 
 formation, ^ith thicker beds of the same color. These strata, on the west side, 
 appear to have a thickness of between 300 and 400 feet, and contain, 
 towards the middle, about thirty feet of massive black limestone. They 
 are highly fossiliferous on both sides, and contain, among other species, 
 Stenopora fibrosa, S. petropolitana, Ptilodictya acuta, Orthis lynx^ 
 Rhynchonella increbescens, Orthoceras strigatum, Calymene Blumen- 
 
CHAP. XL] QUEBEC GROUP. 275 
 
 bachii, and Trinudeus concentricus. On the west side of the axis, these utica for- 
 strata are followed by black brittle slates, which occupy a breadth of mation - 
 about seventy yards, and reach to the margin of the bay. They are 
 fossiliferous, but, having a cleavage independent of the bedding, it is dif- 
 ficult to obtain specimens. Orthis testudinaria, however, occurs in them 
 in some abundance ; and as there is no doubt that the limestones to the 
 east of them belong to the Trenton, these black slates would appear to 
 come into the place of the Utica formation. 
 
 On the west side of the anticlinal, the strata have a more precipitous dip 
 than on the east. The inclination on the former side appears to range from 
 about seventy to ninety degrees, and it occasionally shows an inversion of 
 the strata. Plunging under Lake Champlain in this attitude, the Trenton 
 formation is not known to emerge again before approaching the opposite 
 side of the lake in New York. It is probable that the shales which fill a 
 great part of the interval between these two outcrops, may belong to the 
 Utica and Hudson River formations, as these are known to occupy a consid- 
 erable part of the promontory separating Missisquoi Bay from the Riche- 
 lieu River. On the east side of the anticlinal, the inclination of the 
 strata does not appear to exceed forty-five degrees ; and to the west of the 
 Franklin House, a subordinate undulation repeats the Birdseye and Black 
 River limestone, and carries the Trenton farther east. After a short 
 interval of concealment to the east of the house, the latter formation 
 rises again, near the mineral spring, with an attitude not far removed from 
 vertical. This is very probably a final outcrop, as some magnesian strata, 
 which seem to belong to the Quebec group, appear not much more than 
 a quarter of a mile beyond. 
 
 The eastern outcrop of the Birdseye and Black River limestone, connected 
 with the subordinate undulation which has been mentioned to the west 
 of the Franklin House, is traceable northward to the margin of the bay, 
 about a quarter of a mile from the axis of the main anticlinal ; where its dip 
 becomes S. 30 E. < 39. The corresponding north-eastward strike 
 would carry the band towards the mouth of the Rock River ; and about a 
 quarter of a mile in this direction, we meet with the subjacent grey calca- 
 reous sandstone, inside of a promontory which shows a considerable mass 
 of the dove-grey limestone. Less than a quarter of a mile farther in the 
 same direction would bring us to the probable position of the Quebec 
 group, as inferred from the run of the rocks of this group from the Barbue 
 southward. 
 
 In this direction, the most western edge of the group comes upon Mis- rhiiiipsburgi. 
 sisquoi Bay, at Phillipsburgh, preserving a well marked escarpment for 
 four miles before reaching the bay, and continuing along the shore of the 
 bay in a pretty straight line, for upwards of three miles more, to within 
 about half a mile of Rock River. Instead, however, of the Sillery portion 
 
276 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XL 
 
 L6visfor- of the group, as on the Barbue, the strata here displayed appear to 
 mation. j^i^g t the L^ v is formation. On the province line, and a mile north 
 of it, they occupy a breadth of two miles, extending from the shore of 
 Missisquoi Bay to the valley of Rock River ; and in Canada, they are trace- 
 able from the province line to the village of Bedford on the Yamaska, a 
 distance of eight miles. They have a general dip to the eastward ; but it 
 appears not improbable that they are affected by longitudinal dislocations, 
 which may be upthrows on the east side, arranging partial repetitions of 
 the strata in long parallel belts. The strata are also disturbed by trans- 
 verse faults, throwing them eastward and westward, at right angles to the 
 strike ; the whole producing a complicated structure, the details of which 
 will require farther investigation. 
 
 On the province line, and on a parallel line about a mile north of it, run- 
 ning east from Phillipsburgh, longitudinal dislocations are suspected to occur 
 
 Bay< 
 
 280-282. GASTEROPODA . 
 
 281 
 
 280. Murchisonia Vesta (Billings). 
 
 281. Metoptoma Niobe (Billings); a, side view; 6, view of upper side. 
 
 282. M. -- Oritkyia (Billings) ; a, side view ; b, outline of the base. 
 
 in the west half of the two miles ; while in the east half, the measures 
 appear to be arranged in the form of a trough, with a moderate dip on the 
 west side, and a precipitous one on the east, which often becomes perpendic- 
 ular, and sometimes presents an inversion of the strata. What appear to 
 be the lowest strata, occur on the shore of Missisquoi Bay. They consist of 
 dark grey and yellowish-white dolomites, weathering grey and yellowish- 
 brown, and divided into massive beds. Some of these hold geodes of calc- 
 spar, and others, geodes of quartz, which also occurs in patches and nodular 
 portions ; while towards the top, are beds similarly marked with black and 
 grey chert, which sometimes occurs in angular masses. The average general 
 dip of these beds is about E. S. E. < 12, and their thickness appears to 
 
CHAP. XL] 
 
 QUEBEC GROUP. 
 
 277 
 
 be about 400 feet. A few feet at the top become mottled with patches of 
 ash-grey pure limestone, and these are followed by from fifty to a hundred 
 feet of ash-grey, dove-grey or greyish-white, pure compact limestone, in 
 massive beds. The weathered surfaces of these are marked by a multitude of 
 
 283. CEPHALOPODA. 
 
 283. Lituites Farnsworthi (Billings). 
 
 thin raised reticulating lines of crystalline dolomite, more numerous in the 
 lower than in the upper beds. At the summit, the dove-grey color merges in 
 some places into an opaque slightly yellowish-white. These beds occupy a 
 belt, lying between the margin of the bay and a parallel valley occurring 
 
278 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XI. 
 
 about 800 yards to the east. The only indications of fossils associated with 
 them are confined to the dove-grey and white limestones, in which the 
 genera Pleurotomaria and Holopea have been observed, but too indistinct 
 to be specifically determined. 
 
 Farther eastward from Phillipsburgh, these beds are followed by reddish- 
 grey, brown-weathering dolomites in thick beds, succeeded by black 
 massive dolomites. In contact with these, there are, in two or three places, 
 some thin bedded black limestones, which resemble beds much higher 
 in the series, and may be here brought into place by some complicated 
 
 284. CRUSTACEA. 
 
 
 L5vis for- 
 
 284. JLmphion Salteri (Billings) ; a, the head ; b, the tail. 
 
 structure not yet understood. The thickness of these grey and black 
 dolomites is by no means certain, but it is supposed to be about 200 feet. 
 Beyond this ridge, these black dolomites are succeeded by a series of 
 strata which appear to be as follows, in ascending order : 
 
 Feet. 
 
 i t White and dove-grey limestones, -with thin raised chain-like lines 
 of crystalline dolomite, reticulating over the surfaces of the beds. 
 Interstratified with them, are a few beds of magnesian limestone, 
 some light grey, weathering yellowish, and some dark grey, 
 weathering white ; a bed of mottled red and white dolomite a foot 
 thick occurs about the middle of the mass. The white and dove- 
 grey limestones hold fossils, of which the genera appear to be 
 Pleurotomaria and Ophileta, but the species are not yet deter- 
 mined. In what is considered the equivalent of these beds on the 
 province line, there occurs Bathyurus Saffordi, ........ . ......... 120 
 
 2. Dark grey and black limestone, some of the beds being highly 
 magnesian. Some are mottled and weather light grey, and others 
 are reticulated by thin raised lines of yellowish weathering 
 dolomite. These beds are very fossiliferous, and contain, among 
 other genera, Orthis, Orthisina, Camerella, Maclurea, Ophileta, 
 Ecculiomphalus, Pleurotomaria, Murchisonia, Holopea, Metoptoma, 
 Orthoceras, Cyrtoceras, Nautilus, Jlmphion, Bathyurus, and Dikelo- 
 cephalus. The described species are Orthis Electra, Camerella cal- 
 cifera, Maclurea matutina, Ophileta sordida, 0. levata, 0. com- 
 planata, Ecculiomphalus Canadensis, E. intortus, E. spiralis, 
 Lituites Farnsworthi, Amphion Salteri, and Bathyurus Saffordi,.. 120 
 3. Dark bluish-grey, reddish-grey, and black, thin bedded nodular 
 limestones, interstratified with thin layers of bluish-grey slate, 
 probably magnesian. Although thin bedded, the layers are 
 aggregated in considerable masses, which have little tendency 
 
CHAP. XI.] QUEBEC GROUP. 279 
 
 Feet. 
 
 to separate in the planes of deposit. In the escarpments of 
 these strata, the more calcareous parts of the rock being dis- 
 solved away by atmospheric waters, the slaty portions stand out 
 in bands, which weather yellowish. On the surface of some of 
 the beds, the rock weathers into a red or yellow ochery arena- 
 ceous earth, in which the moulds of fossil forms are numerous. 
 The genera and the described species are nearly all identical 
 with those of the previous division. Towards the top, Lituites 
 appears to be very frequent, 150 
 
 4. Black slaty thin bedded nodular limestone, with a cleavage inde- 
 
 pendent of the bedding. The rock generally weathers to a 
 grey, occasionally tinged with yellow ; it has a somewhat 
 scaly fracture, and breaks with the cleavage, rather than with the 
 bedding. It holds fossils, of which the genera appear to be chiefly 
 Pleurotomaria, Orthoceras, and Lituites; the only described spe- 
 cies being Lituites imperator, SCO 
 
 5. Black limestones, some of them massive, weathering light bluish- 
 
 grey, interstratified towards the bottom with occasional black 
 and dark grey magnesian bands, some of them weathering 
 yellowish and others white ; they are much intersected by joints 
 running in various directions. Towards the top, they are 
 interstratified with thin bedded dark grey limestones. About 
 150 feet from the summit, beds of this kind rest upon a massive 
 layer of black limestone, filling up hollows in its surface. The 
 fossils met with in this division are chiefly of the genera Eospongia, 
 Pleurotomaria, Murchisonia, Holopea, Orthoceras, Cyrtoceras, 
 Nautilus, and Bathyurus ; the only described species being Bathy- 
 L urus Saffordi, 350 
 
 1040 
 
 The whole of these strata occur on a line east from Phillipsburgh, on 
 which they occupy about a mile and a quarter, terminating at the road 
 from Moore's Corners to Bedford. On the province line, the last two Province line 
 divisions, 4 and 5, appear to be absent. On this line, the three lower eection - 
 divisions, 1, 2, and 3, constitute a hill, which, immediately west of the valley 
 of the Rock River, rises to a height of about 300 feet over Lake Cham- 
 plain. The summit of this hill is composed of the thin bedded limestones, 3. 
 The upper part of them is there arranged in the form of a trough, the 
 axis of the synclinal being a few yards east of one of the iron posts which 
 mark the boundary of the province. To the south, the hill slopes down 
 to a road ; and between the road and the hill, the black limestones, 2, can 
 be traced round from the position which they occupy west of the hill on 
 the province line, to another close by the same line, on the east side of the 
 hill. Here they are nearly vertical, with a dip north-westward, and the 
 outcrop of one of the bands can be traced north-eastward, without any break 
 or concealment, for three quarters of a mile, in which distance it becomes 
 
280 GEOLOGY OF CANADA. [CHAP. XI. 
 
 occasionally overturned. Its bearing, in the more northern half of this 
 distance is N. 54 E., which would carry it much to the eastward of the 
 most eastern exposures of the higher limestones, 4 and 5 ; but the posi- 
 tion where these divisions turn on the synclinal axis, has not yet been 
 observed. The white limestones, 1, have been observed on both sides of 
 the trough, to the southward of the province line ; but their turn upon the 
 axis appears to be covered by drift. Farther south-westward, there are 
 exposures of black limestones and dolomites, whose arrangement has not 
 yet been investigated ; it is conjectured, however, that their structure 
 will conform to that on the north side of the province line. 
 
 Swanton A short distance southward from Highgate Springs, the rocks connected 
 with the anticlinal which occurs there, become covered with drift ; but in the 
 bed of the Missisquoi River at Swanton Falls, about five miles in that 
 direction, and not far out of the course of the anticlinal, dark grey shales 
 and thin interstratified limestones occur, which resemble those of the 
 Hudson River formation. About three miles farther south, we again meet 
 with a group of strata similar to those of the Springs, which are traceable, 
 at intervals, for upwards of six miles, to St. Alban's Bay. On a recent 
 examination of one of the exposures of these rocks, occurring near Smith's 
 lime-kiln, under the guidance of the Reverend J. B. Perry and Dr. Gr. 
 M. Hall, of Swanton, who have devoted much attention to the geology of 
 their own neighborhood, it was ascertained that strata of the Trenton, 
 of the Birdseye and Black River, and probably of the Chazy formation, are 
 
 inverted there presented in an inverted attitude. Between sixty and seventy 
 lon- feet of thin bedded black limestones, dipping eastward, and marked by 
 Calymene Blumenbacliii and Trinucleus concentricus, support from 
 eighty to one hundred feet of thick bedded black limestones, with Colum- 
 naria alveolata and Orthoceras Bigsbyi. After a very small interval of 
 concealment, these are followed by about sixty feet of grey calcareous 
 sandstone, on which rest about 200 feet of dove-grey limestone ; becoming 
 interstratified towards the top with beds of yellow-weathering dolomite, 
 and finally overlaid by 150 or 160 feet of yellow and brown weather- 
 ing magnesian limestones. Except that Chazy fossils have not been 
 observed between the thick bedded black limestone and the grey calcareous 
 sandstone, the sequence sufficiently corresponds with that of the series 
 at St. Dominique and at Highgate Springs, and, without much doubt, 
 represents it. 
 
 overturn The dip, which is to the eastward, has an inclination varying from 
 
 dips. forty-five degrees on the west, to fifteen on the east ; being thus in some 
 places forty-five, and in others seventy-five degrees beyond the perpen- 
 dicular. The overturn, it will be perceived, is greatest on the east side. 
 Within 150 yards of the most eastern exposure of the magnesian rocks 
 belonging to the section, there occurs a yellowish dolomitic sandstone, or 
 
CHAP. XI.] QUEBEC GROUP. 281 
 
 sandy dolomite, which appears to be associated with a series of red and 
 white mottled dolomites, largely displayed on the property of Mr. C. 
 Bullard in the neighborhood ; where they have been, to a small extent, 
 quarried as marbles. These red and white dolomites slope in the same 
 direction, and at about the same angle, as the strata to the west of them, 
 their dip being about E. < 12 ; while there is nothing in the physical 
 attitude of the rocks to indicate that there is any considerable break 
 between them, or that the one does not regularly and conformably pass 
 under the other. Such may very possibly be the case ; but the evidence of Dislocation, 
 the fossils would seem to prove, that, whether the strata are so arranged or 
 not, there must be a break of many thousand feet between the two series, 
 and that the apparently overlying strata to the east are greatly the older 
 of the two. 
 
 These dolomites, with sandstones, generally red, and occasional shales, Red sand- 
 constitute what is called the Red sandrock of Vermont. From the position rock> 
 of their western outcrop, on the public road, at Mr. Bullard's, they are 
 traceable southward in an almost unbroken course, not only to St. Alban's 
 Bay, but in a line, which is in a general way parallel with the margin 
 of Lake Champlain, to Burlington. Here they are exposed at Sharp 
 Shins, and they are represented on the map of the State Geological 
 Survey of Vermont, as extending still much farter to the south. To the 
 northward, they come upon the Missisquoi River, upwards of a mile east 
 of Swanton Falls, and, crossing the river, are traceable thence, by the 
 residence of Mr. Church, to the neighborhood of Saxe's mill, within two 
 miles of the province line. 
 
 As far as our investigations have gone, the following appears to be the swanton 
 ascending sequence and the approximate thickness of the series of strata section - 
 to which the red mottled dolomites belong : 
 
 Feet. 
 
 1. White and red dolomites with sandy layers ; some of the strata are mottled 
 
 rose-red and white, and a few are brick-red or indian-red. Some beds 
 contain a considerable amount of silicious sand, and all weather to a 
 reddish or yellowish brown. In the cliff opposite the residence of Mr. 
 Church, some of the red beds contain Conocephalites Jldamsi and 
 C. Vulcanus, 370 
 
 2. Grey argillaceous limestone, partially magnesian, weathering brownish, and 
 
 holding a great abundance of tangled specimens of Palceophycus incipiens, 110 
 
 3. Buff sandy dolomite, weathering brown, 40 
 
 4. Dark grey and bluish-black slate, partially magnesian, with thin bands 
 
 of sandy dolomite, weathering yellowish. The slate is fossiliferous, but, 
 having a cleavage independent of the bedding, it is somewhat difficult 
 to obtain specimens. Towards the top there occur Obolella cingulata, 
 Orthisina festinata, Camerella antiquala, Conocephalites Teucer, Para- 
 doxides Thompson^ and P. Vermontana, 130 
 
 5. Measures not well exposed, but consisting in part of bands of bluish mottled 
 
 dolomite, weathering to a red ochery earth ; mixed with patches of grey 
 pure limestone and grey dolomite, weathering grey. There are also 
 
282 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XI. 
 
 Paradoxides 
 slates. 
 
 Conoceph- 
 alites. 
 
 bands of light grey fine-grained and slightly micaceous flagstones, 
 weathering reddish-yellow, with abundance of fucoids. Some bands 
 of bluish slate are also visible, and it is supposed that the chief part of 
 what is concealed, probably more than three fourths of the mass, may 
 also consist of slate. . 
 
 Feet. 
 
 60 
 710 
 
 This section occurs over a mile east of S wanton Falls, where, as well 
 as near Mr. Church's residence, we were aided by Dr. G. M. Hall and 
 the Reverend J. B. Perry, in the examination of the fossiliferous beds. 
 From the neighborhood of Swanton, the Paradoxides slates, 4, have been 
 followed southward by these gentlemen, to their junction with similar beds 
 at Georgia, where the two species of Paradoxides mentioned in the section, 
 were long ago discovered by the late Rev. Zadock Thompson. Mr. Thompson 
 and the late Prof. C. B. Adams, then State Geologist of Vermont, also 
 obtained Conocephalites from the Red sandrock in 1847 ; but until speci- 
 mens were presented by Messrs. Hall and Perry to the officers of the 
 Canadian Survey in 1861, which was the first announcement to us of their 
 occurrence, the true horizon of the rock from which these fossils were 
 derived, had never, we believe, been established on palseontological evidence. 
 There is little doubt that they belong to the Potsdam group, and may 
 very possibly represent its lowest member. 
 
 As has already been stated, the rocks of the foregoing section can be 
 followed northward to the vicinity of Saxe's mill ; beyond which, on the 
 road to the province line, additional strata are met with. They appear to 
 be as follows in ascending order : 
 
 Ft*. 
 
 6. Light grey brown-weathering, more or less dolomitic sandstones, some of 
 
 which are fine grained, while others are fine conglomerates, with white 
 quartz pebbles as large as swan-shot. These are interstratified with 
 bands of white sandstone, varying in thickness from five to fifteen feet, 
 and making an aggregate of about one eighth of the whole mass. A 
 band of bluish-grey dolomite near the top holds one or two species of 
 Orthis and Orthisina, 630 
 
 7. Bluish thin-bedded, argillaceous, dolomitic flagstones and slates, cleaving 
 
 with the bedding. These flagstones contain Conocephalites arenosus, 
 together with many fucoids, 60 
 
 8. Bluish and yellowish mottled dolomite, with reddish and whitish mottled 
 
 dolomite at the summit, 120 
 
 9. Yellowish and yellowish-grey brown-weathering sandy dolomite, not well 
 
 exposed ; about half the amount towards the lower part being concealed, 600 
 
 1410 
 
 Across the measures, on the province line, there occurs a still farther 
 amount of strata belonging to this series, occupying a breadth of a little 
 more than a mile. A large portion of the measures in this part, how- 
 ever, is concealed ; and in those exposed, it is often difficult to determine 
 
CHAP. XL] 
 
 QUEBEC GROUP. 
 
 283 
 
 the planes of bedding. It is, in consequence, not easy to estimate the 
 volume of strata to be added to the preceding series ; they may however 
 be described in a general way as follows : 
 
 Feet. 
 
 10. Buff and whitish, brown-weathering, sandy dolomite, holding a great 
 amount of black and grey chert in angular fragments of various sizes 
 up to a foot in length and six inches wide. The chert occasion- 
 ally forms layers of a few inches, in which different shades of color 
 coincide with the stratification. In some beds the fragments of chert 
 make up the chief part of the rock, while in others it lies in scattered 
 pieces. It is often associated with masses of white quartz, which 
 occasionally appear as if filling geodes or druses. The thickness given 
 is in a great degree conjectural, 790 
 
 The whole volume of these magnesian rocks of the Potsdam group, Potsdam 
 would thus seem to be about 2200 feet. On the province line, the most group- 
 western exposure belonging to them, approaches to within a quarter of a 
 
 285, 286. ZOOPHYTA (POTSDAM GBOUP). 
 a 
 
 
 285. Archeocyathus Atlanticus (Billings) ; a, exterior of a fragment; 
 
 6, transverse section of the same ; c, longitudinal section. 
 286. Jlrcheocyathus ? weathered extremity of a specimen 
 
 with more numerous and regular septa, probably a distinct 
 
 species. 
 
 mile of the most eastern exposure of the Phillipsburgh limestones, showing 
 the proximate position of a dislocation, that must run between the two. 
 It would thus appear that from the neighborhood of Smith's lime-kiln, 
 northward, there proceed two diverging lines of fault: the one running 
 
284 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XI. 
 
 to Phillipsburgh, and thence to the Barbue ; and the other, by Saxe's 
 mill, to the Rock River at the province line, and to Moore's Corners 
 Dislocations, beyond. On the western side of the one, the Trenton and its associated 
 Black River and Chazy rocks, and, on the same side of the other, the 
 Phillipsburgh strata, appear to stand with a nearly vertical western dip, 
 or with an inverted eastern dip. The rocks on the east side of the two 
 dislocations, on the contrary, present a moderate slope to the eastward ; 
 
 287. BBACHIOPODA (POTSDAM GROUP). 
 
 287. Obolella cingulata (Billings) ; a, ventral valve ; 6, dorsal valve ; 
 c, cast of interior of dorsal valve. 
 
 being at the same time, in each case, much older than those on the west 
 In other words, we have here two diverging anticlinal folds, often over- 
 turned, with upthrow dislocations on their eastern sides, running along the 
 axes, and probably producing overlaps. They are thus analogous to the 
 
 288-291. BRACHIOPOD A (POTSDAM GROUP). 
 
 288. Obolella chromatica (Billings) ; a, ventral valve ; 6, dorsal valve ; 
 c, interior of supposed ventral valve, showing the muscular 
 impressions ; d, outline restored from detached valves. 
 
 289.Orthisina festinata (Billings) ; a, side view ; 6, ventral valve ; c, 
 area of the same valve enlarged. 
 
 290. Camerella antiquata (Billings). 
 
 291. Obolus Labradoricus (Billings) ; dorsal valve. 
 
 great dislocation on the north side of the island of Orleans (p. 234), 
 of which the eastern one is probably a continuation. 
 
 While the strike of the strata on the west side of the eastern anticlinal 
 is north-eastward, that of those on the west side is about north. The 
 strikes on the opposite sides, thus converge northwardly, demonstrating 
 
CHAP. XL] QUEBEC GROUP. 285 
 
 that the crown of the anticlinal sinks in that direction. In conformity 
 with this, the Potsdam rocks narrow in that direction, and become 
 concealed between two and three miles north of the province line. The 
 facts, however, which have been ascertained in connection with their dis- 
 appearance, are not sufficient to authorize a detailed description. Where 
 the two breaks nearly meet, at Smith's lime-kiln, the displacement would 
 appear to become not much less than about 4000 feet. 
 
 To the eastward, the Potsdam strata are succeeded by dark grey or 
 blackish calcareo-magnesian slates, weathering yellowish; interstratified 
 with thin nodular layers of dark grey limestone, and occasional beds of 
 six or eight inches in thickness. The rock is fossiliferous in some places ; 
 but in consequence of a cleavage independent of the bedding, it is diffi- 
 cult to obtain good specimens. Among the genera are Orthis, Amphion, 
 Asaphus, Hlcenus, and Bathyurus. Of these, the only determined species 
 
 292. AXNELIDuB (POTSDAM GKOTJP). 
 
 292. Salterella rugosa (Billings). 
 
 is Batliyurm Saffordi. These calcareo-magnesian slates occupy a breadth 
 of probably not far from a mile, in the neighborhood of Herrick's mills, 
 near the province line, in the valley of the Rock River. They have been 
 traced southward of the province line, up the valley, about a mile and 
 three quarters to Stimet's mills. They probably reach Highgate Falls on 
 the Missisquoi, upwards of four miles farther south, and may continue in 
 the same direction beyond. A mile north of the province line, on the road 
 from Moore's Corners to Frelighsburg, they appear to be covered up by 
 drift ; but their breadth must here be less than three quarters of a mile, as 
 at that distance eastward from the chert-bearing Potsdam dolomites, there 
 occurs an argillaceous slate, without ascertained fossils, which seems to 
 belong to the series of black slates that have been mentioned as separating 
 the main synclinals of the Quebec group. 
 
 The lithological character of the calcareo-magnesian slates at Herrick's 
 mills, as well as the general aspect of their fossils, would very well accord 
 with the view that they occur in ascending succession to the highest strata 
 of the Phillipsburgh series, although they have only one species (Bath- 
 Saffordi) in common. But the fact that they follow directly 
 
286 GEOLOGY OP CANADA. [CHAP. XI. 
 
 the Potsdam chert-bearing strata, without the intervention of the great 
 mass of the Phillipsburgh rocks, and without any apparent disturbance, is 
 one that will require farther investigation to explain. On the province 
 line, the Potsdam strata terminate less than half a mile to the east of 
 BockKiver. Rock River, the highest beds dipping S. 76 E. < 24, The concealed 
 interval between them and the slates, is only about fourteen paces; and 
 although the slates present several small undulations, their general dip 
 appears to be in the same direction, and at about the same angle as that 
 
 293-297. CRUSTACEA (POTSDAM GROUP). 
 
 295 296 
 
 297 
 
 Glabellse of the following species : 
 
 293. Conocephalites miser (Billings). 
 
 294. C. Adamsi (Billings). 
 
 295. C. Teucer (Billings). 
 
 296. C. Vulcanus (Billings). 
 
 297. C. arenosus (Billings). 
 
 of the older rock, which would thus seem to pass conformably under the 
 slates. On the Rock River, about 150 paces below the bridge near Her- 
 rick's mills, the slates and dolomite are seen together in the same bank, the 
 slates about fifteen feet above the dolomite. They both appear to dip 
 S. 80 E. < 33. If notwithstanding this appearance of conformity in 
 the two rocks, there should be a dislocation between them, it would in this 
 instance, probably be a downthrow to the east. 
 
 298, 299. CRUSTACEA (POTSDAM GROUP). 
 
 298. Bathyurus senedus (Billings) ; a, head ; 6, pygidium, supposed to be 
 
 of the same species. 
 299. B. parvulus (Billings) ; the head. 
 
 The calcareo-magnesian slates have not been as yet traced continuously, 
 much farther northward than Herrick's mills ; but it may be here remarked, 
 that they resemble lithologically, the slates which have been mentioned as 
 occurring on the twenty-sixth lot of the first range of Farnham. The 
 distance between the exposures is about sixteen miles, but they apparently 
 strike for one another ; and as they have both, palaeontologically, an aspect 
 somewhat newer than that of the Phillipsburgh series, it might be sup- 
 
CHAP. XL] QUEBEC GROUP. 287 
 
 posed that they belong to one and the same band. They have not how- 
 ever been found to contain any species in common ; and a larger number 
 of facts connected with these exposures must be accumulated, before any 
 decided opinion can be formed regarding their true horizon. On the Dunham. 
 twenty-fifth lot of the sixth range of Dunham, which is about four miles 
 south-eastward of the Farnham exposure, there occurs a band of limestone 
 of about thirty feet thick, traceable for about a hundred yards, and prob- 
 ably having a lenticular form, in which the Leptoena and the Orthis of 
 Farnham are present, but without any of the other fossils. Its strike 
 appears to be parallel with that of the Farnham band ; and it would seem to 
 occupy about the same place on the east side of the general mass of shales, 
 that the Farnham rock does on the west. 
 
 No strata with the combined palseontological and lithological characteris- 
 tics presented by those of the Potsdam group, which come from Vermont into 
 St. Armand, are yet known to crop out from beneath the Quebec group, in its 
 extension on the south side of the St. Lawrence. On the north side of the 
 Gulf of St. Lawrence, however, at the Straits of Belle Isle, about 900 miles straits of 
 from St. Armand, the rocks alluded to in Chapter VI. as occurring at Belle lsle< 
 Anse aux Blanc Sablons, have been found, on an examination made since 
 that chapter was written, to be characterized by fossils which appear to 
 show that they belong to the same horizon as the Red sandrock of Vermont. 
 
 At the east horn of Pillage Bay, on the main coast, opposite to Hunter's 
 
 Island of the Mingan group, a white sandstone about eight feet thick has Is 
 been met with, resting on Laurentian gneiss. The position of this sand- 
 stone, and the moderate dip of the palaeozoic strata in that neighborhood, would 
 bring it to within two feet of the nearest strata of the Calciferous formation. 
 It is probable that it may belong to the Potsdam group, and represent 
 its summit. Between this exposure and Bradore Bay, the distance is about 
 300 miles. The shore, which is very much indented by bays and inlets, 
 and fringed with a multitude of islands, presents an almost continuous 
 line of bare rocks ; but in no part of it have there been observed any strata, 
 but such as belong to the Laurentian series. On the east side of Bradore Bradore 
 Bay, which is situated near to the entrance to the Straits of Belle Isle from Bay- 
 the Gulf of St. Lawrence, the palaeozoic rocks again present themselves. 
 Resting on the Laurentian gneiss, they run along the north coast for 
 nearly eighty miles, with a breadth of probably ten or twelve miles, and a 
 slope, towards the water, of about sixty feet in a mile. In this stretch 
 along the coast, they are divided into five or six tabular masses, separated 
 from one another by narrow denuded portions of the gneiss, which in every 
 case terminates in a deep bay- These areas of nearly horizontal strata, 
 in most cases present abrupt escarpments on all sides ; and on the water- 
 line in Anse aux Blanc Sablons, the gneiss shows itself at the base. These 
 tabular masses consist, in ascending order, of the following strata : 
 
288 GEOLOGY OF CANADA. [CHAP. XI. 
 
 Feet. 
 
 1. Red and grey sandstones, sometimes of a reddish-grey ; consisting, in the 
 
 lower part, of a conglomerate composed of rounded pebbles of white 
 quartz from an eighth of an inch to three inches in diameter, in a 
 matrix of fine-grained sandstone, made up of whitish and reddish quartz, 
 and white and red feldspar. A similar fine-grained mixture constitutes 
 the great mass of the rock in the upper part. The beds vary in 
 thickness from three inches to three feet, and many of them are 
 penetrated vertically by Scolithus linearis, about a quarter of an inch in 
 diameter, and always of a lighter color than the surrounding mass. 
 Four feet below the summit, there is a bed three and a half feet thick, of 
 a mammillated or concretionary character ; the concretions, which are 
 from one to ten feet in horizontal diameter, being composed of concen- 
 tric layers from a quarter to half an inch thick, 231 
 
 2. Grey, reddish, and greenish limestones, presenting on the strike great 
 
 diversities of character. They sometimes consist of yellow-weathering, 
 massive, nodular, argillaceous limestones, probably magnesian, holding 
 lenticular patches of pure limestone, as well as of red and green shale 
 from three to six feet in horizontal diameter. On the strike, these yellow- 
 weathering limestones pass in some parts into grey, compact, pure 
 limestone, in thick, massive beds, while in others they are evenly divided 
 into layers of only two or three inches thick. In Forteau Bay, the whole 
 mass appears to be more or less fossiliferous, and among the species are 
 Palcsophycus incipiens, Jlrcheocyathus JLtlantlcus, A. Minganensis, Obolus 
 Labradoricus, Obolella chromatica, 0. cingulata, two new species of Orthis, 
 one new species of Orthisina, Paradoxides Thompsoni, P. Vermontana, 
 Conocephalites miser, JBathyurus senectus, B. parvulus, Salterella rugosa, 
 S. pulchella, and S. obtusa, 143 
 
 374 
 
 The general aspect of the fossils, with the fact that Obolella cingulata, 
 Paradoxides Thompsoni, and P. Vermontana are common to these strata 
 and to the Red sandrock of Vermont, appears quite sufficient to establish 
 the equivalency of the two deposits. In front of these rocks, the strait 
 has a width of between ten and fifteen miles ; and on the opposite side, 
 Newfound- the shore of Newfoundland is occupied by a series of limestones, appa- 
 rently of Calciferous age, which rise from the water at so small an angle 
 that it is nearly impossible to determine it by the eye. From Anchor 
 Point, and perhaps from Cape Norman, which is the most northern point 
 of Newfoundland, they stretch along the coast for upwards of a hundred 
 miles, to Hawke's Bay, in the bight of which they are underlaid by a 
 white sandstone. The attitude of the rocks on the opposite sides of the 
 strait, would appear to indicate that they lie in the form of a shallow trough ; 
 and it is therefore to be inferred that the limestones of the south side, and 
 the white sandstones which underlie them, must be concealed by the water 
 Ascending on the north side of the trough. In ascending succession to the rocks 
 section. fa^ k ave jj een gi ven> \ ^ 2, we should therefore have 
 
CHAP. XL] QUEBEC GROUP. 289 
 
 Feet. 
 
 3. White fine-grained silicious sandstone ; the beds vary in thickness from one White sand- 
 
 to three feet, and, while some are a little coarser than others, a few stone, 
 
 hold scattered pebbles of white quartz of an inch in diameter, and 
 several enclose flat worn pieces of black slightly micaceous shale. 
 Many of the beds are streaked with a reddish color, running with the 
 stratification. This sandstone is identical in character with that 
 
 ; which underlies the Calciferous formation of the Mingan Islands, and 
 
 specimens of it cannot be distinguished from the white sandstone 
 associated with the track-beds of Beauharnois. The small worn 
 patches of shale enclosed in some of the strata, strongly resemble 
 those which are imbedded in the sandstone of Hemmingford Mountain. 
 Though only twenty feet of the rock were seen in place in Hawke's 
 Bay, the occurrence of large flat angular fragments of it, over 
 
 ^ a transverse breadth of several miles, in the rear of the overlying 
 limestones, makes it probable that it is a formation of some impor- 
 tance. The small slope of the lower rocks on the north side of the 
 strait, and the narrowness of the channel, will however scarcely 
 allow a greater thickness than about, 250 
 
 4. Grey and reddish magnesian limestones in massive beds, weather- 
 
 ing grey and yellow ; interstratified with thin beds of light 
 greenish magnesian limestone, weathering buff, and with occa- 
 sional thin layers of a yellow and light greenish limestone not 
 magnesian. In grey magnesian limestones, supposed to be near 
 the top of the mass, Lingula acuminata occurs, ... 150 
 
 5. Dark grey limestones, occasionally argillaceous, and often mag- 
 
 nesian, weathering yellowish, and then holding geodes of 
 white quartz and calcspar, in some abundance ; the beds appear 
 to be from three inches to four feet thick. The only fossils 
 observed are undetermined species of Lingula and fragments of 
 undetermined trilobites, 400 
 
 6. Dark grey limestone, associated with dark bluish and yellowish Geodiferous 
 
 calcareo-argillaceous layers ; the beds are from one inch to dolomites, 
 five feet thick, and the thicker ones, which are probably mag- 
 nesian, hold in abundance, geodes of white quartz and calcspar. 
 At about one third from the bottom, a bed of three feet thick 
 contains, in some abundance, geodes holding white, pink, and 
 red fluor spar. Fossils are abundant in some of the beds, and 
 occasionally occur in a silicified condition ; in the great mass 
 of the rock, however, they have not been met with. The genera 
 observed are Orthis, Strophomena, Ophileta, Ecculiomphalus, 
 Orthoceras, Bathyurus, and Leperditia ; the only species deter- 
 mined being Bathyurus Cordai, 400 
 
 7. Dark grey limestones similar to the previous, more geodiferous and 
 
 probably more magnesian ; they are at the same time more 
 fossiliferous. The genera which they contain are Strophomena, 
 Orthis, Ophileta, Maclurea, Ecculiomphalus, Pleurotomaria, Mur- 
 chisonia, Orthoceras, jlsaphus, Bathyurus, and Leperditia; the 
 only determined species appears to be Murchisonia Anna, 130 
 
 8. Greyish-blue even bedded limestones, purer than before ; the thick- 
 
 ness of the beds ranges from one inch to one foot. These lime- 
 stones are very fossiliferous, but the fossils are often obscure. 
 Among the genera are Orthis, Strophomena, Ophileta, Maclurea, 
 Ecculiomphalus, Pleurotomaria, Murchisonia, Orthoceras, Pilo- 
 
 T 
 
290 GEOLOGY OP CANADA. [CHAP. XI. 
 
 Feet. 
 
 ceras, Jlsaphus, Bathyurus, Leperditia, and trilobites of two or 
 three undetermined genera ; Murchisonia Anna and Piloceras 
 
 Canadense are the only determined species, 340 
 
 9. Light yellowish-grey mottled yellow-weathering magnesian lime- 
 stone j some of the beds hold in great abundance geodes of 
 white crystallized quartz and yellowish-white calcspar. The 
 fossils in these strata are few and obscure ; the only genera 
 met with are Ophileta and Orthoceras, 150 
 
 1570 
 
 Point Rich 10. Light-grey and yellowish-white mottled magnesian limestone, of the 
 limestones. same general character as the previous mass, but in some parts 
 
 suddenly changing on the strike, for a thickness of from ten to 
 thirty feet, into a bluish-grey pure limestone, in which the fossils 
 are better preserved than in the magnesian parts. It might be 
 supposed that the two limestones, in these cases, are thus 
 brought into juxtaposition by dislocations, were it not that the 
 thicknesses of the beds on the opposite sides of the junction 
 precisely agree, and that there occasionally runs evenly through 
 both of them, an unbroken interstratified band of dark grey or 
 black compact limestone. The fossils are Strophomena, Orthis, 
 Ophileta, Maclurea, Ecculiomphalus, Pleurotomaria, Murchisonia, 
 Holopea, Orthoceras, Nautilus, dsaphus, Illcenus, Bathyurus, Am- 
 phion, Leperditia, and several undetermined genera of trilobites. 
 In the upper ten feet, the yellowish-white magnesian limestone 
 is replaced by a similar rock of dark grey. This portion becomes 
 black on the strike, and then contains no observed fossils, .... 130 
 
 11. Light bluish-grey tough limestones of a uniform texture ; in beds 
 
 varying from an inch to two feet in thickness, which hold a 
 greater abundance of fossils than any of the strata lower down. 
 Among the genera met with are Eospongia, Stromatopora (like 
 S. compacta, but larger), Strophomena,0rthis, Ophileta, Maclurea, 
 Ecculiomphalus, Pleurotomaria, Murchisonia, Holopea, Bathyurus, 
 Jlmphion, Leperditia, and several trilobites of undetermined 
 genera, 130 
 
 12. Light bluish-grey limestones of the same description as the previous 
 
 mass ; they are however thicker bedded, but their fossils are 
 more obscure. The upper third is rather darker in color than 
 the rest, and contains trilobites in abundance, and a few ortho- 
 ceratites, which are often badly preserved, 550 
 
 13. Black bituminous limestone, in beds of from one to three inches thick, 
 
 interstratified with fine brittle black shale, in layers varying 
 from a quarter of an inch to three inches ; the limestones hold 
 fossils, but not in abundance, 200 
 
 1010 
 
 [Fossils were collected from the last two divisions ; but it became 
 
 necessary to abandon them on the coast, the surf being too heavy 
 to permit the approach of the boat to take them on board.] 
 
 Grey sand- 14. Grey calcareous sandstones, generally fine grained ; in beds of from six 
 stones. inches to two feet, interstratified with black and greenish shales, 
 
 which predominate towards the top. The sandstones are sometimes 
 of a conglomerate character, and include pebbles of white quartz, 
 and black limestone, varying in diameter from the eighth of an inch to 
 two inches ; with small fragments of red and black jasper, and flat pieces 
 
CHAP. XI.] QUEBEC GROUP. 291 
 
 Feet. 
 
 of black and green shale. The sandstones and the shales are aggre- 
 gated in masses varying from six up to sixty feet in thickness. No 
 fossils have been met with in this rock, 700 
 
 15. Grey, drab, and whitish limestone conglomerates, interstratified in the Limestone 
 
 lower part, with bands of black and greenish shale from forty to a conglom- 
 hundred feet thick ; and associated with black limestone holding layers 
 of black chert from one to three inches thick. Graptolites occur in the 
 black limestones, and fragments of trilobites in the chert. In the upper 
 part, the conglomerate is more massive, great thicknesses showing 
 no trace of bedding. The enclosed pebbles, boulders, and fragments 
 of limestone, range in weight from one ounce to a ton, and in color from 
 white, through various shades of drab and grey, to black. Associated 
 with the masses of limestone, are occasionally others of grey cal- 
 careous sandstone, specimens of which cannot be distinguished from 
 those of the sandstone, 14, which is beneath. Some masses, which 
 are of the same character as smaller inclosed blocks, are 200 feet long 
 by thirty feet thick. It is difficult to decide whether these are sedi- 
 ments deposited in the bed, or enclosed transported masses, notwith- 
 standing that they are divided into beds with partings of black shale. 
 Some of the conglomerate beds are filled with pebbles of black 
 chert. Near to the top, patches of several hundred yards, in the 
 supposed direction of the strike, but without observed bedding, con- 
 sist of light reddish-grey pure limestone, in part highly crys- 
 talline, abounding with convoluted shells and other fossils. The 
 genera found in these conglomerates and their interstratified masses, 
 are Graptolithus, Orthis, Rhynchondla, Camerella, Ophileta, Maclurea, 
 Orthoceras, dsaphus, Illcznus, Jlmp/iion, Bathyurus, Holematopus, 
 Nileus, Jlmpyx, Jlgnostus, Endymion, and several trilobites of unde- 
 termined genera. The determined species are Graptolithus Headi, 
 Camerella Calcifera, Maclurea ponderosa, Bathyurus Saffordi, Holemat- 
 opus Jlngelini, Endymion Meeki, and Nileus scrutator, TOO 
 
 16. Greenish sandstones of a chloritic aspect, made up apparently of fine grains Green sand- 
 
 of quartz and feldspar, with a few scales of mica, mixed with greenish stones. 
 
 argillaceous matter. Some beds are of a conglomerate character, the 
 
 pebbles consisting of white quartz and reddish feldspar, varying from 
 
 the sixteenth of an inch to an inch in diameter ; the quartz pebbles 
 
 are somewhat larger and much more numerous than those of feldspar. 
 
 They are accompanied by occasional pebbles of red jasper, and by flat 
 
 pieces of green shale. In some beds, the masses enclosed consist of 
 
 grey limestone. The finer beds are aggregated in thicknesses of 
 
 several hundred feet, and the conglomerates are from ten to twenty 
 
 feet. These fine and coarse sandstones are interstratified with Eed and 
 
 several bands of red shale, from ten to twenty feet thick ; and one of green shales. 
 
 sixty feet, consists of red shale interstratified with green layers. The 
 
 thickness of the whole was not measured, but it is supposed to be not 
 
 much under, 2000 
 
 6230 
 
 The limestones, 4 to 9, succeeding to the white sandstones, 3, were exam- 
 bed along the coast of Newfoundland at intervals, for fifty miles, extending 
 from Anchor Point to Hawke's Bay. In a large part of this distance, the 
 
292 GEOLOGY OF CANADA. [CHAP. XI. 
 
 beds come obliquely upon the coast, with a S. S. W. slope of between ten 
 and thirty feet in a mile ; and along the water line, they are apparently 
 turning from the extremity to the side of the shallow trough to which 
 
 Point Rich, they belong. With the small slope just mentioned, they run under the 
 limestones of St. John's Island and Point Rich, 10 to 13 ; the contact being 
 visible at Port au Choix, near the latter place In Hawke's Bay there is 
 probably a transverse dislocation, again bringing the lower limestones, 
 4 to 9, forward to the coast, along which they run for about twenty-five 
 miles to Table Point. Here, with a south-west slope of about five degrees, 
 they pass under the Point RicR limestones, the dip gradually increasing, 
 between the base and summit of these, to eighteen degrees. With this 
 increased dip, the Point Rich limestones sink beneath the grey sandstones, 
 14; the nearest approach of the two rocks across the measures being 
 about twenty feet. 
 
 Dislocation. South-eastward from Table Point, another transverse break occurs, 
 which brings the base of the Point Rich limestones opposite to the 
 base of the grey sandstones. On the south-east side of the dislo- 
 cation, the dip, which is still to the S. W., becomes thirty degrees. With 
 this slope, the limestones and the sandstones, 10 to 14, again come in suc- 
 cession; and the conglomerate limestones, 15, follow at a distance of 
 Portland about a mile across the measures. The exposures showing this succession 
 eek ' are at Daniel's Harbor ; and at Portland Creek, three miles beyond, 
 there is a great display of the conglomerate limestones ; but in their south- 
 eastward course, these are cut off by another transverse dislocation, and 
 on the south side of the creek the grey sandstones are brought forward to 
 the coast. They here present a dip about S. < 4 - 8 ; and the conglom- 
 erate limestones are again seen about four miles, in the direction of the 
 dip, from Portland Creek. 
 
 Seventeen miles farther on, the grey sandstones again appear ; being 
 this time arranged in the form of an anticlinal, the axis of which runs about 
 N. 37 E. and S. 37 W. The slope on the north-westward side ranges 
 from seventy to ninety degrees, while that on the south-eastward gradually 
 diminishes to fifty-eight degrees. Here the sandstones sink under the con- 
 glomerate limestones, the contact being visible. The bearing of the axis 
 of the anticlinal would carry the sandstones between Steering Island and 
 Cow Head, both of which are composed of the conglomerate limestones. 
 The rocks of these two localities thus appear to be equivalent masses on 
 opposite sides of the fold. 
 
 Bonne Bay. Bonne Bay is situated about twenty-five miles still farther along the 
 coast, from Cow Head. It is a deep indentation, running south-eastward 
 into the land ; and at the distance of about six miles from the entrance, it 
 splits into two parts, the East Arm and the South Arm. The portion 
 of land separating these two arms is from three to five miles wide, and, 
 
CHAP. XI.] QUEBEC GROUP. 293 
 
 although the strata which compose it are somewhat broken by small 
 dislocations, the whole succession of deposits, from 4 to 15, can be par- 
 tially seen, the one in contact with another. They stand at a high 
 angle, with a general slope to the south-west ; and on the South Arm, in 
 addition to the rocks already given, we have the greenish sandstones, 16, 
 in immediate succession to the conglomerate limestones. 
 
 These greenish sandstones have so striking a lithological resemblance sniery for- 
 to the Sillery series, both in the aspect of the arenaceous beds and mation - 
 in their interstratification with red shales, that there can scarcely be much 
 doubt of the equivalency of the two. The whole succession of the Belle 
 Isle rocks, attaining a thickness of about 6000 feet, would appear to bear 
 a remarkable general analogy to th'e Potsdam and Quebec groups. As Potsdam 
 already stated, the Scolithus sandstones and the Paradoxides limestones, group - 
 1 and 2, of the north shore, are the equivalents of the Red sandrock of 
 Vermont and its associated strata; while the white sandstones, 3, of 
 Hawke's Bay, are the representatives of the Beauharnois strata, at the 
 summit of the Potsdam group. The magnesian limestones, 4 to 9, of 
 Anchor Point and Port au Choix, appear to occupy the position of the 
 Calciferous formation. Four species, Lingula acuminata, Murchisonia 
 Anna, Piloceras Canadense, and Bathyurus Cordai, are common to the 
 two, and there is a striking resemblance in the aspect of the whole faunas 
 of both series. The Point Rich limestones, 10 to 13, appear to be a higher 
 part of the same series, possibly not represented to the westward, in 
 Canada ; while the grey sandstones and conglomerate limestones, 14 and 15, L<vis for- 
 seem to be equivalent to a part at least of the rocks of Point Le'vis, and mation> 
 to the higher portion of those of Phillipsburgh. In addition to the great 
 general resemblance of the faunas, these strata have, in common with 
 the two western localities, G-raptolithus Headi, Oamerella calcifera, 
 Maclurea ponderosa, and Bathyurus Saffordi. But while some of their 
 fossils strongly resemble in general aspect those of the Farnham lime- 
 stones, the Newfoundland rocks have none of the trilobites, such as Oon- 
 ocephalites, Dikelocephalus, Menocephalus, and others, which give to a 
 small portion of the Point Le'vis series a primordial aspect. 
 
 The apparent physical structure, both at Quebec and at Bonne Bay, 
 would seem to place the Sillery sandstones above the conglomerate 
 limestones of the Quebec group ; but it is to be kept in mind, that, although 
 the greenish sandstones at Bonne Bay appear upon the east side of the 
 South Arm, in conformable sequence to the conglomerate limestones, both 
 are tilted up to a high angle, the dip being W. S. W. < 45 - 80. It is Altered 
 to be farther noted, that on the west side of the South Arm, the rocks Serpen tine. 
 become highly metamorphosed. After exposures of other conglomerates 
 and succeeding sandstones, which are associated with white talcose slates, 
 there rises, to a height of between 2000 and 3000 feet, a mountain of 
 serpentine, similar in character to that of the Eastern Townships. 
 
294 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XI. 
 
 Marginal 
 outcrops. 
 
 It has been shown, that, with the exception of a small area of the Pots- 
 dam sandstone at St. Ambroise (p. 96), we have no evidence of a marginal 
 outcrop of this formation between the St. Maurice River and the Mingan 
 Islands. No marginal outcrops of the Calciferous and Chazy fonna- 
 ^ ong k aye k een ^ serve( j from the longitude of Lake St.. Peter to the same 
 group of islands ; and between the vicinity of Kingston and the north 
 shore of Lake Huron, all three of these formations appear to be wanting. 
 From the Mingan Islands to the Mohawk River in New York, the mar- 
 ginal outcrops of the Potsdam, Calciferous, and Chazy united, do not in 
 any part much exceed 1000 feet in thickness ; while the thickness of the 
 Extent of Quebec group alone, is about 7000 feet. This, constituting the great 
 the Quebec metalliferous formation of the continent, is traceable, under various designa- 
 tions, from Gasp^ to Alabama ; thence sweeping round on the west side 
 of the Mississippi, through Kanzas, to Lake Superior, where it appears 
 without any diminution in its volume. 
 
 From these facts, it would appear probable, that, during the Potsdam 
 period, the older rocks, which formed the coast of the Lower Silurian sea, 
 extended, under comparatively shallow water, south-eastwardly from the St. 
 Lawrence and the Ottawa, to the fault which brings up the Quebec group 
 between Gasp^ and the Mohawk ; and south-westwardly from a line between 
 * ne Mohawk and Lake Superior, as far as Alabama. All around this 
 shallow area, they descended quickly into deep water ; thus constituting a 
 subaqueous promontory from the Laurentian and Huronian rocks of the 
 north, and forming, with these, what Mr. James D. Dana has termed the 
 nucleus of the North American continent. 
 
 But although the great volume of the Quebec and Potsdam groups, 
 shows that over the area occupied by them, there must have existed a 
 deep sea during the Potsdam period ; it is to be remarked, that many of the 
 members, both of the lower and upper parts of the Quebec group, have by 
 no means the characters of deep-sea deposits. It has already been stated, 
 that the beds of passage between the littoral portions of the Potsdam 
 and Calciferous formations, suggest the opinion, that, towards the termina- 
 tion of the Potsdam era, a gradual sinking of the surface had occurred. 
 In order to obtain the conditions for the accumulation of the coarser sedi- 
 ments, which commence near the base of the Quebec group, it must be 
 supposed, that, shortly after the beginning of the Calciferous period, a 
 great continental elevation occurred ; carrying the littoral deposits of the 
 Potsdam, and the beds of passage just mentioned, high above the sea, 
 and bringing the area at the base of the Quebec group comparatively 
 near to the surface. The successive coarse deposits of the group indicate a 
 subsequent gradual subsidence, at unequal intervals, probably with subor- 
 dinate oscillations, until the early shallow-water strata were again sub- 
 merged ; to be first partially covered over by deposits of the Chazy forma- 
 
 Ancient 
 continent, 
 
 Deep 
 02010 8ea> 
 
 continental 
 elevation. 
 
CHAP. XI.] QUEBEC GROUP. 295 
 
 tion, and then, almost universally, by those of the Trenton and Hudson 
 groups. 
 
 In this way may be explained the break which occurs in the succession 
 of life between the Calciferous and Chazy, in the shallow-water deposits of cal breaks - 
 these formations between the Allumettes Island and Montreal, as well as 
 among the Mingan Islands. The interruption in the succession of deposits 
 between the base of the Trenton group and the Potsdam, at St. Ambroise ; 
 and that between the same base and the Laurentian, from the north shore 
 of Lake Huron to Kingston, as well as in the vicinity of St. Paul and Murray 
 Bays, and at Lake St. John on the Saguenay, is in the same way accounted 
 for. The break in the succession of life between the Chazy and the Trenton 
 group, is not so great as that between the Calciferous and the Chazy. It is 
 not yet quite certain, that, at the marginal outcrop of the latter formations in 
 Canada, a single species passes upwards into the Chazy ; while about one 
 sixth of the species of the Chazy are known to occur in the Birdseye and 
 Black River formation, at the base of the Trenton group. It seems to be Base of the 
 in accordance with this, that we have evidences of a somewhat sudden Trenton - 
 submergence at the commencement of the Trenton period, and a some- 
 what rapid accumulation of its lower strata, the Birdseye and Black River 
 limestones. Where these rest upon the Huronian and Laurentian series, 
 the beds of contact are often composed of angular fragments of the 
 underlying rock ; and it frequently happens that the surface on which these 
 beds rest, is rough, and broken into sharp projecting ledges and deep 
 fissures, which were filled up and covered over by the deposits in question, 
 before sufficient time had elapsed to permit the surface to be worn down. 
 Instances in illustration of this occur on the Snake Islands, west of 
 Lacloche, in Lake Huron, where the Birdseye and Black River for- 
 mation rests on the quartzites of the Huronian series ; and at Marmora, 
 where it is supported by Laurentian rocks. Dr. Dawson has pointed out 
 a striking instance of these phenomena at Hog Lake in Huntingdon ; 
 other examples occur at Sloat's Lake in Loughborough and its vicinity, as 
 well as at Kingston Mills. The same conditions may be observed in the 
 neighborhood of Murray Bay. 
 
 As an instance of the probably rapid slope of the bottom of the Lower 
 Silurian sea from shallow to deep water, during the Potsdam period, in the 
 neighborhood of Quebec, we see that the surface of the quartzose gneiss 
 now supporting the Trenton formation at the Falls of Montmorenci, must 
 have been 7000 feet above the gneiss under the island of Orleans ; while 
 the distance between the two positions does not much exceed a mile and 
 a half. This would give a slope of nearly forty-five degrees ; and perhaps slope of the 
 it would not be extravagant to take this as representing the inclination ancient coast - 
 along the whole line to Alabama. As the Potsdam and Quebec groups 
 accumulated, the edges of their strata would abut against this slope ; and 
 
296 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XI. 
 
 ultimately both these, and the early shallow-water deposits on the higher 
 terrace, would be covered over by the Birdseye and Black River, the 
 Trenton, the Utica, and the Hudson River formations. This we have 
 endeavored to represent in the accompanying ideal diagram ; in which it 
 
 300. SUPPOSED ARRANGEMENT OP THE STRATA BEFORE THE BREAK. 
 
 G. Laurentian gneiss. 
 
 Black shales. 
 Littoral sandstones. 
 
 Northern 
 shallow sea. 
 
 Conglomerate limestones, 1-8. 
 
 Green shales, 9-12. 
 
 Grey sandstones, 13-15. 
 
 Dark grey shales, 16. 
 
 Red and green shales, 17. J 
 
 Green sandstones. Sillery formation, j 
 
 The above numbers refer to the section, page 227. 
 
 T. Trenton group of limestones. 
 u. Utica shales. 
 
 H. Hudson River sandstones and shales. 
 L. L. Sea level at the commencement of the Quebec period. 
 s. s. Sea level at the close of the Potsdam, and also at the beginning 
 of the Trenton period. 
 
 Vertical scale of the section, one inch to a mile. 
 
 will be perceived that the lowest of these formations is shown as resting 
 (at P.) on one of those littoral deposits of Potsdam sandstone, like that at 
 St. Ambroise, which are still met with along the marginal outcrop. 
 
 The strike of this rapid slope in the bottom of the ancient sea, coinciding 
 ^ith the break, had, as already indicated, a general north-eastward bearing, 
 from Lake Champlain to the vicinity of Cape Chatte. The present trend 
 of the Laurentian gneiss, from the neighborhood of Quebec to Pointe des 
 Monts, has a rude parallelism with it; but farther down the valley of 
 the St. Lawrence, while the line of break turns gradually eastward, and 
 ultimately south of east, in Gaspd, the trend of the gneiss becomes north- 
 ward for about sixty miles, then eastward for three hundred miles, and 
 finally north-eastward for two hundred miles more, to the Atlantic ex- 
 tremity of the Straits of Belle Isle. This divergence of the two lines 
 would lead us to anticipate an area of shallow water during the Lower 
 Silurian period ; so protected from disturbance that any strata occurring 
 there, might be expected to present a comparatively horizontal attitude, 
 
CHAP. XL] 
 
 QUEBEC GROUP. 
 
 297 
 
 like that of the Lower Silurian formations on the same side of the break 
 to the west. We accordingly find, in the Mingan Islands, in Anticosti, 
 and on the Straits of Belle Isle, the Lower Silurian deposits in such an 
 attitude. In the latter locality, however, the volume of the undisturbed 
 strata would appear to indicate that the bottom shelved more gradually 
 before reaching the slope. The increase of the dip in approaching Bonne 
 Bay, suggests that we may expect to find the break somewhere in that 
 neighborhood. 
 
 Without enquiring into the origin of the forces which may have produced 
 the corrugations of the earth's crust, we may suppose that if a sufficient 
 lateral pressure were applied to the strata thus accumulated and arranged, 
 there would result a series of parallel folds running in a direction at right 
 angles to that of the force, with prevailing overturn dips towards the line 
 of resistance. The solid crystalline gneiss in the case before us, offering 
 more resistance than the newer strata, there resulted a break coinciding 
 with the inclined plane at the junction of these with the gneiss. The 
 lower palaeozoic strata, pushed up this slope, would then raise and fracture 
 the formations above, and be ultimately made to overlap the portion of 
 these resting on the edge of the higher terrace ; after probably thrusting 
 over to an inverted dip, the broken edge of the upper formations. The 
 shallow-water strata of the higher terrace, relieved from pressure by the 
 break, would remain comparatively undisturbed ; and thus the limit of the 
 more corrugated area would coincide with the slope between the deep and 
 shallow waters of the Potsdam period. The resistance offered by the 
 buttress of gneiss would not only limit the main disturbance ; but it 
 would probably also guide or modify, in some degree, the whole series 
 of parallel corrugations, and thus act as one of the causes giving a direc- 
 tion to the great Appalachian chain of mountains. 
 
 Anticosti 
 area. 
 
 Results of 
 lateral pres- 
 sure. 
 
298 GEOLOGY OF CANADA. [CHAP. XII. 
 
 CHAPTER XII. 
 
 THE ANTICOSTI GROUP AND THE GUELPH FORMATION. 
 
 THE ROCKS OP ANTICOSTI; THEIR EQUIVALENTS IN WESTERN CANADA. GUELPH FORMATION; 
 MIDDLE SILURIAN. FOUR DIVISIONS OF THE GROUP IN ANTICOSTI; THEIR DISTRIBUTION 
 AND THICKNESS. ANTICOSTI GROUP IN GA8PE; IN WESTERN CANADA. ONEIDA CONGLOM- 
 ERATE; MEDINA AND CLINTON FORMATIONS; THE GREY BAND. RED AND GREEN SHALES 
 AND SANDSTONES; THEIR DISTRIBUTION. NIAGARA FORMATION; SHALES AND MAGNESIAS 
 LIMESTONES; THEIR DISTRIBUTION. GUELPH FORMATION; DOLOMITES; ITS DISTRIBUTION. 
 
 At the close of Chapter IX., we have given a section of the Hudson 
 River rocks, as they occur at the west end of Anticosti. The strata of 
 this formation occupy nearly the whole of the north side of the island ; 
 and extend from Fox Point, which is towards the east end, to Junction 
 Cliff, on the south side, about four miles from the west end. The remain- 
 ing portion of the island is occupied by newer rocks, to which the name 
 of the Anticosti group has been given. Their position hi the geological 
 series, is that occupied by the Oneida conglomerate, the Medina sand- 
 stone, the Clinton group, and the Niagara group, of the New York 
 geologists ; but these subdivisions, although apparent in the western basin, 
 disappear in the Anticosti strata, which are lithologically unlike their 
 
 Middle equivalents in Western Canada. In that region, the Niagara formation, 
 which corresponds to the summit of the Anticosti group, is followed by 
 what we have named the Guelph formation, and makes up with it the 
 Middle Silurian. 
 
 First division. The rocks of this group on the island of Anticosti, may be considered 
 in four divisions ; the first and lowest of which, in immediate succession to 
 the Hudson River formation, is as follows, in ascending order : 
 
 1. 
 
 Ft. in. 
 
 1. Greenish argillo-arenaceous shale, interstratified in the upper half 
 
 with beds of grey limestone, from one to three inches thick,. ... 26 
 
 2. Yellowish-grey compact argillaceous limestone, with few observed 
 
 fossils, 10 
 
CHAP. XIL] ANTICOSTI GROUP. 299 
 
 Ft. in. 
 
 3. Yellowish-grey compact argillaceous limestone, interstratified with 
 
 light reddish-grey limestone beds of from one to three inches 
 
 thick, with many fossils, 20 
 
 The preceding beds compose Junction Cliff, as well as White 
 Cliff, in Ellis Bay. The fossils consist chiefly of the following 
 species : Stenoporafibrosa, Holy sites catenulatus, an undetermined 
 Heliolites, Favosites Gothlandica, Petraia gracilis, two undescribed 
 species of Ptilodictya, Leptana sericea, Strophomena rhomb oidalis, 
 S.pecten, Orthis lynx, 0. Salteri, O. Huxleyi, O. Panderi, 0. 
 'v porcata, 0. Laurentina, an undescribed species of the same genus, 
 
 Orthisina Verneuili, Lingula Forbesi, Pentamerus reversus, Atrypa 
 marginalis, a new species of Athyris, Murchisonia papillosa, with 
 two undetermined species of the same genus, Pleurotomaria Amer- 
 icana, Bellerophon bilobatus, B. acutus, JLmbonychia radiata, an 
 undetermined species of Orthoceras and one of JLscoceras, two 
 undetermined species of dsaphus, one of Encrinurus, and one of 
 Dalmanites. 
 
 4. Measures partly concealed ; but supposed to be of the same character 
 
 as the preceding, both lithologically and palaeontologically, .... 25 
 
 5. Ash-grey argillaceous limestone, in beds of from one to three inches 
 
 thick, alternating with beds of calcareo-argillaceous shale of 
 from five to seven inches. Both of these are interstratified with 
 light grey pure limestone beds, one or two inches thick ; no fossils 
 have been observed in this part, 6 
 
 6. Ash-grey argillaceous limestones and shales, interstratified as before 
 
 with pure limestones. These beds occur about one mile east of 
 Junction Cliff, and contain very nearly the same fossils as before ; 
 with the addition of Lingula quadrata, Pleurotomaria Thalia, and 
 an undetermined Cyrtoceras. All of the species are found loose 
 and well preserved in the debris, as well as standing out in relief 
 on weathered surfaces, 20 
 
 7. Ash-grey argillaceous limestones and shales, with purer limestones, 
 
 as before. The fossils are not so well preserved, in consequence 
 
 of the action of the sea, 41 o 
 
 8. Measures concealed, . 21 
 
 9. Grey limestone, interstratified with grey and sometimes greenish 
 
 calcareo-argillaceous shale ; the lowest bed is characterized by 
 Beatricea undulata, and Murchisonia gigantea. The Beatricea is 
 here of a larger size than the examples found in the Hudson River 
 formation. One specimen obtained is ten feet and a half long, 
 six inches in diameter at the larger end, and five inches at 
 the other. Some fragments of others were found to be ten or 
 even fifteen inches in diameter, and, if the length were propor- 
 tionate, must have been probably over thirty feet long, 12 
 
 10. Light yellowish-grey limestone, in beds of from half an inch to an inch 
 
 in thickness, with occasional partings of calcareo-argillaceous 
 shale. They contain abundance of Strophomena pecten, and two 
 small and probably undescribed species of Atrypa, 5 Q 
 
 11. Yellowish-white coralline limestone ; the corals consist chiefly of 
 
 four genera, comprehending Stenopora fibrosa, Favosites Goth- 
 landica, Halysites catenulatus, and an undetermined Heliolites. 
 They are aggregated in dome-shaped masses, from one to three 
 
300 GEOLOGY OP CANADA. [CHAP. XII. 
 
 Ft. in. 
 
 feet in height, and sometimes as much as six feet in diameter. 
 These are surrounded by an ash-grey argillaceous limestone, and 
 cause the overlying beds, conforming to the masses, to have the 
 
 appearance of slightly undulating strata, 5 
 
 This coral bed is met with at Point Laframboise, at Cape Henry, 
 which is the west horn, and at Cape Eagle, the east horn of Ellis 
 Bay ; the three points comprehending four miles on the strike. 
 In addition to the fossils already mentioned, there are in the last 
 twenty-two feet, undetermined species of Palceophyllum and Ptilo- 
 dictya, with Petraia gracilis, Leptana sericea, Strophomena 
 rhomboidalis, Orthis lynx, O. Laurentina, 0. Salteri, 0. Huxleyi, 
 Pentamerus reversus, and an undetermined Encrinurus. 
 
 12. Grey limestone, with argillaceous partings ; some of the beds contain 
 
 Strophomena rhomboidalis , S. pecten, and dmbonychia radiata; 
 
 with some undescribed species, 62 
 
 13. Grey compact argillo-calcareous beds, slightly bituminous, interstrat- 
 
 ified with argillaceous bands ; these beds form Bear Head. They 
 contain but few fossils, which are mostly obscure ; among them 
 are Orthis Salteri and Pentamerus reversus, 42 
 
 14. Measures supposed to be similar to the last, but not thoroughly exam- 
 
 ined ; they constitute Long Point, 35 
 
 306 6 
 
 The dip of these beds is S. 13 W. at Junction Cliff, and S. 10 W., one 
 mile east of it; at White Cliff it is S. 4 W., at Eagle Cape, S. 18 W., 
 and at Bear Head Point, S. 21 W. : the average would be about S. 13 W. 
 The inclination is a little over 100 feet in a mile, and the direct distance 
 across the strata is three miles. The distance occupied by these rocks, 
 alongthe coast, from Junction Cliff to Long Point, is eight miles and a 
 quarter. As a whole, they appear to be softer than those of the Hudson 
 Biver formation, and offer no very remarkable cliffs along the coast; while 
 their erosion has given rise to Ellis or Gamache Bay, as well as to the 
 depression which holds Gamache Lake, and the creek emptying it at the 
 head of the bay. 
 
 2. 
 
 second Immediately overlying the upper beds of the last division, there occur, 
 
 at Long Point, about twenty feet of light grey limestone, in beds of from 
 two to six inches thick, filled with Pentamerus Barrandi. These beds 
 can be traced along the coast, sometimes in the cliff, but generally on the 
 beach, and in the reef between high and low water as far as Becscie 
 River ; a distance of nine miles. Additional strata, characterized by the 
 same fossil, are occasionally seen in the cliff, for fourteen miles farther, 
 to Otter River. That part of the following ascending section which over- 
 lies the Pentamerus beds, 1, is observed in the twelve miles beyond 
 Otter River, and reaches to within a mile of Jupiter River. 
 
CHAP. XII.] ANTICOSTI GROUP. 3d 
 
 Ft. in. 
 
 1. Ash-grey and light reddish-grey limestones, in beds of from two to six 
 
 inches thick ; interstratified in the upper part with conglomerate 
 beds of some thickness, at intervals of from two to ten feet. The 
 pebbles are calcareous, from one to three inches in diameter, and 
 lie flat in the beds. Many of the strata are filled with Pen- 
 tamerus Barrandi ; with this, however, are associated in some 
 beds, Favosites Gothlandica, Haly sites catenulatus, Stromatopora 
 concentrica, with undetermined species of Petraia and Ptilodictya, 
 Strophomena pecten, an undetermined species of Rhynchonella, and 
 an Obolus or dthyris, 100 
 
 2. Dark ash-grey slightly bituminous limestone, in beds of from two to six 
 
 inches, with calcareo-argillaceous partings, weathering to a light 
 orange-brown ; conglomerate layers with limestone pebbles occur 
 at irregular intervals. The lowest six feet are characterized by the 
 occurrence, in some abundance, of an undescribed species of JLthy- 
 ris, and the following additional fossils are met with throughout 
 the mass : Favosites Gothlandica, Stromatopora concentrica, Holy- 
 sites catenulatus, undetermined species of Petraia, Plilodictya, and 
 Diphyphyllum ; Strophomena Philomela, S. Leda, Orthis Salterij 
 an undetermined Pleurotomaria, Murchisonia gracilis, and several 
 undetermined species of Orthoceras, 20 6 
 
 3. Dark ash-grey slightly bituminous limestone ; with calcareo-argilla- 
 
 ceous partings, weathering light orange-brown, as before. It 
 contains Stenopora fibrosa, undetermined species of Petraia and 
 Ptilodictya, Strophomena Leda and Orthis Salteri, 34 6 
 
 4. Reddish-grey slightly bituminous limestone, with calcareo-argillaceous 
 
 partings as before, and holding Stenopora fibrosa, Favosites Goth- 
 landica, undetermined species of jlulopora, Petraia, and Ptilodic- 
 tya, Strophomena Leda, Orthis Salteri, undetermined species of 
 Rhynchonella, Leperditia, and Beyrichia, with Calymene Blumen- 
 bachii. Some of the beds near the top are characterized by deep 
 serpentining grooves, about a quarter of an inch wide, with raised 
 edges ; apparently the track of some species of mollusk, 36 
 
 5. Reddish-grey limestone, in beds from one quarter of an inch to three 
 
 inches thick, some of which weather to a reddish-brown ; inter- 
 stratified with occasional conglomerate layers of from two to 
 four inches thick. Some beds at the base are marked by the same 
 grooves as before, and others, in one or two places, contain Steno- 
 pora fibrosa, Favosites Gothlandica, an undetermined Petraia, 
 Strophomena Leda, and Orthis Salteri } 73 
 
 6. Measures concealed, 40 
 
 7. Grey yellowish-weathering limestone, containing but few fossils ; 
 
 those met with are Stenopora fibrosa, Favosites Gothlandica, Haly- 
 sites catenulatus, an undetermined Petraia, Strophomena Leda, 
 Orthis Salteri, Atrypa congesta, in some abundance towards the 
 base, and an undetermined Rhynchonella. The surface of one bed 
 towards the middle is characterized by marks, which are probably 
 the result of weathering. The bed is a couple of inches thick, 
 and is worn into a multitude of rather deep connected pits, about 
 an inch wide and two or three inches long, in each of which is 
 perceived a fragment of a shell, standing with its edge up. There 
 is generally a rude parallelism in the pits, but some of them cross 
 others, and some descend nearly through the bed, 34 
 
302 GEOLOGY OP CANADA. [CHAP. XII. 
 
 Ft. in. 
 
 8. Measures concealed, 17 o 
 
 9. Ash-grey, smoke-grey, and reddish-grey, slightly bituminous lime- 
 
 stones, in beds of from one quarter of an inch to ten inches thick, 
 weathering yellowish-brown in some parts. About two thirds 
 from the bottom, there occur slender serpentining fucoids of a 
 yellowish-white, very conspicuous from the contrast of color. In 
 addition to these, there are met with, in different parts of the 
 mass, Stenopora fibrosa, Favosites Gothlandica, Holy sites catenula- 
 tus, with undetermined species of Petraia, Ptilodictya, and Helio- 
 pora ; Strophomena pecten, S. Leda, Orthis Salteri, Jltrypa reticu- 
 laris (occurring for the first time, near the bottom), undetermined 
 species of Pleurotomaria and Murchisonia, a small undetermined 
 Orthoceras, Calymene Blumenbachii, and an undetermined Encri- 
 
 nurus, 65 
 
 10. Measures concealed, 27 
 
 447 
 
 The total distance which these rocks occupy along the coast, from Long 
 Point to within a mile of Jupiter River, is thirty-six miles. 
 
 3. 
 
 Third divi- The third division of the group commences where the previous series 
 sion - terminates, and reaches to South-West Point ; occupying a distance of a 
 
 little more than seven miles, in a direction very nearly S. S. E. The dip 
 of the strata is very constant in direction, not varying in any part more 
 than about five degrees from the average, which is S. 7 W. ; while the 
 inclination is sometimes 200 feet in a mile, and at other times quite inap- 
 preciable. With the exception of some portions concealed at the base, and 
 more at the summit, the measures are visible the whole way ; forming cliffs 
 of from twenty to one hundred and fifty feet. 
 
 The following is the sequence of the strata in ascending order : 
 
 Ft. in. 
 
 1. Measures concealed, 27 
 
 2. Greenish-grey and brown fine arenaceo-argillaceous shales, inter- 
 
 stratified with one another, in thin beds ; no fossils are seen, .... 60 
 
 3. Yellowish-grey and light drab argillaceous limestone, slightly bitu- 
 
 minous ; in beds of from one to five inches, cut by parallel joints 
 running N. 85 W., with an occasional joint running oblique to 
 that course. The jointed structure and the soft nature of the 
 rock, cause large masses of it to fall from the cliff by the action of 
 the sea, which is here encroaching rapidly on the land. Among 
 the fossils, which are generally in a good state of preservation, are 
 Favosites Gothlandica, an undetermined Graptolithus, Strick- 
 landia like S. lens, jltrypa reticularis, A. hemispheric a, undeter- 
 mined species of Rhynchonella, JLthyris, Cyrtodonta, dvicula, Mya- 
 lina, Cydonema, Orthoceras, dscoceras, and Cyrtoceras, Calymene 
 Blumenbachii, Phacops Orestes, and Illanus orbicaudatus, 80 
 
CHAP. XII.] ANTICOSTI GROUP. 303 
 
 Ft. in. 
 
 4. Light-drab argillaceou3 limestone, slightly bituminous, weathering 
 
 white ; inters tratified with yellowish limestone, weathering yellow- 
 ish-brown ; both in beds of from two to three inches thick. The 
 fossils are not numerous, but weathered surfaces present well 
 preserved specimens of an undetermined Ptilodictya, Strophomena 
 Leda, S. pecten, Atrypa reticularis, A. hemispherica, Stricklandia 
 brevis, Phacops Orestes, and Calymene Blumenbachii, 22 6 
 
 5. Ash-grey and light drab limestones interstratified, both slightly bitu- 
 
 minous, in beds of from half an inch to two inches. The exposed 
 surfaces are nearly white, and show fossils, of which a large 
 number are weathered nearly black. Among them are Stenopora 
 fibrosa, undetermined species of Ptilodictya and Petraia, Leptcena 
 transversalis, Strophomena pecten, S. antiquata, Orthis Salteri, 
 JLtrypa congesta, A. reticularis, A. hemispherica, an undetermined 
 jlthyris, Stricklandia brevis, an undetermined Cyclonema, Phacops 
 Orestes, Calymene Blumenbachii, with undetermined species of 
 Encrinurus and Lichas, 42 6 
 
 6. Ash-grey and light drab limestones interstratified ; both slightly bitu- 
 
 minous, in beds of from two to three inches, holding in the upper 
 
 part Stricklandia lens in some abundance, 10 3 
 
 7. Ash-grey and light-drab limestones interstratified, both slightly bitu- 
 
 minous and crowded with Stricklandia lirata, 2 6 
 
 The position of the beds is just west of the last brook but one, 
 in approaching South- West Point. 
 
 8. Measures concealed, with one foot of light drab argillaceous slightly 
 
 bituminous limestone in the middle, 51 
 
 9. Light drab argillaceous limestone, slightly bituminous, in beds of 
 
 from half an inch to three inches, containing numerous fossils, of 
 which exposed surfaces present excellent specimens, weathered 
 black ; while the edges of the beds along the cliff, yield others 
 quite detached from the rock. Among them are Stenopora fibrosa, 
 *j| Favosites Gothlandica, undetermined species of Petraia, Heliopora, 
 
 and Ptilodictya ; Leptozna transversalis, Strophomena Philomela, S. 
 pecten, Orthis Salteri, Stricklandia lens, Spirifera radiata, an un- 
 described JLthyris, Jltrypa reticularis, undetermined species of 
 Cyclonema and Orthoceras, Calymene Blumenbachii, Phacops 
 
 Orestes, and an undetermined Encrinurus, 87 6 
 
 The position of the beds, 9, is a little east of the last brook, 
 in approaching South-West Point. 
 10. Measures concealed at the bight of the cove, north of South- West 
 
 Point, 157 6 
 
 540 9 
 
 4. 
 
 In immediate sequence to the concealed beds which constitute the Fourth divi. 
 summit of the last division, the following strata occur, in ascending order, 810n< 
 and form the whole of the area of what is called South- West Point. 
 
304 GEOLOGY OF CANADA. [CHAP. XII. 
 
 1. Light smoke-grey somewhat granular limestone in beds from two to 
 
 six inches thick, with thin partings and patches of green argillo- 
 calcareous shale. Iron pyrites is disseminated through the 
 lower four feet, sometimes in single cubes, and sometimes in 
 aggregations of these, forming nodules of one or two inches in 
 diameter, and extending, at the top of the four feet, into patches 
 of from six to eighteen inches in diameter, and from half an inch 
 to an inch thick. The upper eight or nine feet hold fossils, which 
 are well displayed in the same beds, at the Jumpers, between two 
 and three miles east of South- West Point. They consist chiefly 
 of Stromatopora concentrica, Stenopora fibrosa, Favosites Goth- 
 landica, F. favosa, Halysites catenulatus, Zaphrentis Stokesi, 
 Jllveolites Labechei, one undetermined species of Petraia, two 
 of Heliolites, two of Cyathophyllum, and one of Ptychophyllum, 
 Leptcena transversalis, an undescribed species of Strophomena, 
 with S. rhomboidalis, S. Philomela, S. pecten, Orthis Salteri, O. 
 elegantula, O. Davidsoni, Pentamerus oblongus, Stricklandia 
 brevis, S. lens, Spirifera radiata, two undetermined species of 
 jUthyris, one of Rhynchonella, JLtrypa reticularis, A. hemispherica, 
 A. congesta, two undetermined species of Cyclonema, and one or 
 two of Pleurotomaria, Murchisonia turricula, two undetermined 
 species of Seller ophon, and three or four of Orthoceras, Calymene 
 Blumenbachii, Phacops Orestes, with undetermined species of 
 Illcenus, Encrinurus, Lichas, Dalmanites, Leperditia, and Beyrichia, 10 
 
 2. Yellowish or reddish white granular limestone, with thin vein-like 
 
 patches of calcareo-argillaceous shale disseminated through it. 
 The beds of limestone are from three to seven inches thick. Among 
 the organic remains, almost all of which are included among 
 those of the preceding beds, is an undetermined and characteristic 
 Ptychophyllum, some specimens of which are a foot in diameter. 
 Favosites Gothlandica also occurs in tables of half an inch thick, 
 and sometimes three feet in diameter, 7 
 
 3. Yellowish-white granular limestone, in beds of from six to eighteen 
 
 inches thick ; often separated by thin partings of green argillo- 
 calcareous shale, which is also disseminated in small patches 
 through the bed. The fossils are few in species, being chiefly 
 the ruins of crinoidal columns, which in some cases form the 
 entire mass of a bed, 39 
 
 4. Yellowish-white granular limestone, in beds of from six to eighteen 
 
 inches thick ; consisting of masses of organic remains, of which 
 crinoidal columns constitute the larger part ; some of them being 
 three quarters of an inch in diameter. Other fossils are met 
 with ; among which are Stromatopora concentrica, Favosites Goth- 
 landica, F. favosa, Halysites catenulatus, jUlveolites Labechei, with 
 undetermined species of Petraia, Fenestella, Cystiphyllum, andCya- 
 thophyllum; Strophomena rhomboidalis, Orthis Davidsoni, Atrypa 
 reticularis, A. hemispherica, an undetermined Rhynchonella and an 
 undescribed Cyrtia, Cyclonema varians, C. percingulata, an unde- 
 termined Orthoceras, Illcenus orbicaudatus, I. grandis, Calymene 
 Blumenbachii, with undetermined species of Lichas and Cheirurus, 16 
 
GSAP. XII.] ANTICOSTI GROUP. 305 
 
 This is the highest series of strata met with on the island, and its litho- 
 logical characters are so well marked that it is scarcely possible to mistake 
 it for any of those which precede. The South-West Point light-house 
 stands on the beds, 4 ; and similar beds occur in the cliffs on both sides 
 of a cove, about two miles west from the Chicotte River ; while the rocks 
 met with at the intermediate points which have been visited, appear to 
 correspond with one part or other of this series. 
 
 The rocks in these cliffs, exhibiting about thirty feet of the strata, ap- 
 pear to be somewhat disturbed ; the dip and strike are irregular, and the 
 inclination sometimes amounts to as much as twelve degrees. These 
 strata can be traced to within about half a mile of the Chicotte River, and 
 
 301-303. ZOOPHYTA.. 
 
 301. Heliolites inter stincta (Linnaeus). 
 302. Favosites Gothlandica (Goldfuss). 
 303. Halysites catenulatus (Linnaeus). 
 
 as no instance of them has been observed farther to the eastward, the 
 Chicotte River may be assumed as their limit. This would give to the 
 second division, a stretch of thirty miles along the coast. 
 
 Eastward from the Chicotte River, the upper beds of the subjacent or third Third dm- 
 division of the series, preserve a nearly horizontal attitude in twelve sepa- S1< 
 rate exposures, in a distance of about twenty-five miles, to South Point. 
 What are considered to be the same measures, are continued to Cormorant 
 Point, about twenty miles still farther ; in the course of which, they suffer a 
 few moderate undulations. Beyond this point, which presents a cliff of 
 twenty or thirty feet high, the coast gains upon the measures ; and at the 
 distance of about two miles and a half, there occurs a dislocation running 
 N. 37 E. ; producing a downthrow on the east side, of forty-five feet. 
 Between Cormorant Point and this dislocation, there is exposed a thickness 
 of 123 feet of ash-grey limestone, supposed to include the equivalents of the 
 strata exposed from Chicotte River, and to represent the summit of the 
 third division ; which is concealed near South- West Point. The fossils 
 observed in these strata, from the Chicotte River to the fault, are Steno- 
 pora fibrosa, Stromatopora concentrica, an undetermined Heliopora, Favo- 
 
 u 
 
306 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XII. 
 
 sites G-othlandica, F. favosa, Halysites catenulatus, Zaphrentis Stokesi, 
 Alveolites Labechei, with undetermined species of Cyathopliyllum, Ptilo- 
 dictya, Petraia, and G-raptoliihus, Leptcena transversalis, Strophomena 
 rhomboidalis, jS. pecten, S. Philomela, Orthis Salteri, 0. Davidsoni, 
 0. elegantula, Pentamerus oUongus, an undetermined Stricklandia, 
 and S. brevis, Spirifera radiata, Atrypa reticularis, A. congesta, A. hem- 
 ica, undetermined species of Rhynchonella, Athyris, Cyrtodonta^ 
 
 304-309 . ZOOPHYTA , 
 
 305 
 
 304. Syringopora reteformis (Billings). 
 
 305. S. verticillata (Goldfuss). 
 
 306. S. Dalmani (Billings). 
 
 307. S. compacta (Billings). 
 
 308. Strombodes pentagonus (Goldfuss). 
 309.^. gracilis (Billings). 
 
 Avicula, Cyclonema, Murchisonia, Pleurotomaria, Conularia, and Ortho- 
 ceras ; with 0. persipJionatum^ Calymene Blumenbachii, Phacops Orestes^ 
 and undetermined species of Encrinurus and lllcenus. 
 
 The remaining part of the third division composes the coast eastward to 
 Heath Point, and northward round East Point ; where the strata present a 
 cliff of 120 feet, and reach to the west side of the cove immediately beyond 
 the point. They consist of ash-grey, light smoke-grey, and yellowish- 
 grey limestones, containing fossils similar to those in the corresponding 
 portion of the division to the westward. Their thickness is about 428 feet ; 
 making the whole volume of the third division, at the east end of the 
 island, about 550 feet. 
 
CHAP. XIL] ANTICOSTI GROUP. 307 
 
 The rocks on the north side of the island, at the east end, which, from second dm- 
 their position in the succession there, are supposed to represent the second 6:on * 
 division, have as yet been too imperfectly examined to determine accu- 
 rately their volume ; which however is estimated to be about 480 feet. 
 Nothing has been observed to establish their exact equivalency ; so that it is 
 from the relations which they bear to what is above and below them, rather 
 than from what the north and south exposures have in common, that they are 
 considered as equivalents. On the north coast, they occupy ten miles and 
 a half, and deep water prevails along the whole distance. In most places, the 
 sea beats against a precipitous cliff at high water, and in some parts even 
 at low water ; while there are but two or three coves at which a landing can 
 be easily made. It would require very calm weather to effect a thorough 
 examination ; and on account of the storms at the time of our visit, it was 
 only at the two extremes of the distance that measurements were made. 
 
 The upper part of the series consists of grey limestones ; twenty-five feet 
 of which, at the summit, of a yellowish tinge and slightly bituminous, are a 
 yery marked coral-bed, which can be followed a considerable way along 
 the coast. This bed is irregular in its surface, some masses of coral rising 
 from one to five feet high, with a horizontal diameter of from two to ten 
 feet. The overlying bed conforms in some degree to these inequalities, and 
 gives the strata the aspect of having been disturbed. The corals consist 
 of Stenopora fibrosa, Favosites G-othlandica, Halysites catenulatus, with 
 undetermined species of Heliolites and Cyathophyllum. In a lead-grey 
 limestone beneath the coral-bed, Leperditia Anticostensis occurs in consid- 
 erable abundance. 
 
 After an unexamined interval, giving about 200 feet in thickness, 
 sixty feet of yellowish-grey slightly bituminous limestone occur, in beds of 
 from half an inch to four inches. These are separated by thin layers of 
 calcareous shale, and hold two or three undetermined species of Ptilodictya 
 and Petraia, Stenopora fibrosa, Favosites Grothlandica, Halysites cate- 
 nulatus, Orthis Salteri, Strophomena pecten, S. Leda, S. rhomboidalis, 
 undetermined species of RhyncTionella and Atrypa, with A. congesta, 
 Stricklandia lirata, S. brevis, undetermined species of Murchisonia, 
 Pleurotomaria and Orthoceras, Calymene Blumenbachii, Illomus orbi- 
 caudatus, and an undetermined Asaphus. This mass occurs in Sandtop 
 Bay, between which and Gull Cape, there is an unexamined interval, giving 
 eighteen feet. In Gull Cape, and in Gull Cove beyond, a section of 128 
 feet consists, at the top, of fifty-eight feet of dark grey slightly bituminous 
 limestone, followed by twenty feet of light yellowish-grey bituminous lime- 
 stone. This rests on thirty feet of greenish calcareo-arenaceous crumbling 
 shale, and is terminated by twenty feet of lead-grey thin bedded limestone, 
 which are interstratified with similar shales. The fossils observed in 
 this section are an undetermined Petraia, Favosites Crothlandica, an 
 
308 GEOLOGY OF CANADA. [CHAP. XII. 
 
 undetermined Strophomena, Orthis Salteri, Rhynchonella robusta (occur- 
 ring in great abundance in the shale), an undetermined species QiAthyris, 
 Pentamerus oblongus, P. Barrandi (one valve seen in the shale), with 
 undescribed species of Cyclonema, Murchisonia, and Orthoceras ; Phacops 
 Orestes and Hloenus orUcaudatus. 
 
 First division. The first division stretches on the north side of the island, from Gull Cove 
 and Reef Point, to Table Head, a distance of about seven miles, and is again 
 partly visible in the bight of Prinsta Bay ; where it occupies about two 
 miles. As is the case in the neighborhood of Ellis Bay, the, cliffs composed 
 
 310, 311. ZOOPHYTA. 
 
 310. Petraia calicula (Hall). 
 
 311. Zaphrentis Stokesi (Edwards and Haime). 
 
 of the rocks of this division at Fox River, are low, not exceeding thirty or 
 forty feet. The deep excavation which here forms the harbor, shows another 
 feature, which the two extremities of the first division have in common. The 
 upper part of this division is concealed in the lagoon of Fox River, as well 
 as on the outside of Reef Point, which is the eastern horn of Fox Bay ; 
 but about 180 feet of the lower part, consist of grey argillaceous and arena- 
 ceous limestone, with greenish and grey calcareo-argillaceous shales. The 
 total thickness of the division is computed to be about 296 feet, and the 
 fossils collected from the strata exposed, are undetermined species of 
 Petraia, Ptilodictya and.Paseeolus; Stenopora fibrosa, Strophomenarhom- 
 boidalis, iS. pecten, Orthis lynx, 0. Salteri, 0. Laurentina, undescribed 
 species of Rhynchonella and Aihyris, undetermined species of Avicula, 
 Pleurotomaria and Murchisonia y with M. gigantea, undetermined species 
 of Straparollus, Orthoceras,&nd> Cyrtoceras; Oalymene Blumenbachii^ and 
 an undetermined species of Asaphus. 
 
CHAP. XII.] ANTIC OSTI GROUP. 309 
 
 The total thickness of the Anticosti group, as displayed at the opposite Thickness of 
 ends of the island, would thus appear to be very nearly the same ; the the group> 
 comparison being as follows : 
 
 WEST END. 
 
 Ft. in. 
 
 Istdivision, 306 6 
 
 2nd " 447 
 
 3rd " 540 9 
 
 4th " 69 3 
 
 1363 6 1396 3 
 
 It is only the coast of the island that has yet been examined ; so that the 
 geographical distribution of these divisions in the interior, is for the present 
 conjectural. The very moderate slope which the measures everywhere 
 present, however, renders it very probable, that, while there will be a general 
 
 312, 813. TTJSTICATA. 
 
 312. Pasceolus Halli (Billings). 
 313. Ischadites Canadensis (Billings). 
 
 regularity in the parallelism of the escarpments, any deeply worn water 
 courses that may be transverse to the strike, will produce considerable 
 indentations in the lines of outcrop. 
 
 There are evidences of the existence of the Anticosti group on the south The group in 
 side of the Shickshock mountains, on the Chatte and Matanne Rivers, Gasp6 ' 
 and, farther to the westward, on the Metapedia and Great Metis Rivers; 
 but it has not yet been found practicable to determine its southern limit, 
 and to separate it from the newer rocks in that direction. The corrugated 
 condition of the rocks of the Gaspe Peninsula, and the difficulties of explo- 
 ration, arising from the uninhabited state of the interior, have prevented 
 that accumulation of facts, which is required to establish a detailed 
 classification of its rocks. It is therefore for the present found necessary 
 to arrange them in larger divisions than in Western Canada. What is 
 known of the Anticosti group on the south side of the St. Lawrence, will 
 
310 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XII. 
 
 be stated in describing that region in another chapter. For the present, 
 we shall follow out the distribution of the same group in Western Canada, 
 and shall then describe the Guelph formation, which succeeds it in that 
 part of the province. 
 
 ANTICOSTI GROUP IN WESTERN CANADA. 
 
 THE MEDINA AND CLINTON FOKMATIONS. 
 
 Medina in 
 New York. 
 
 Oneida 
 conglomerate. 
 
 In Ulster county, New York, according to the state geologists, the Hud- 
 son River formation is followed by a quartzose conglomerate, constituting 
 the Shawangunk Mountain ; which sometimes attains a thickness of 500 
 feet ; and in Oneida and Oswego counties, becomes a grey, fine grained, hard, 
 even-bedded sandstone. This is often spotted with red stains, from peroxyd 
 of iron ; and contains thin interposed layers of greenish shale, similar to 
 the underlying Hudson River shales ; the two formations showing a gradual 
 passage from the one to the other. At Oswego, the mass is about a hun- 
 dred feet thick, and some few fragments of undetermined fossils have 
 been met with in it. In the two counties last named, the Oswego sand- 
 stone runs from New Hartford to Oswego, a distance of about eighty-five 
 miles ; and to the westward, sinks beneath the waters of Lake Ontario. 
 
 In going upwards, this grey sandstone passes into the red sandstone of 
 the Medina formation ; the two differing lithologically , near the junc- 
 tion, in little more than in color. A gradual passage is thus established, 
 in New York, between the Hudson River and the Medina formations. 
 The latter, at Rochester, consists of a great mass of red marls, and red 
 marly or shaly sandstones, banded and spotted with green, and surmounted 
 by about ten feet of grey or whitish sandstone ; to which succeed about 
 twenty feet of red shales and sandstones, as before ; with Arthrophycus Ear. 
 lam. The series is terminated by seven feet of grey sandstone, known as 
 the Grey band ; and the whole volume of the formation may be somewhat 
 under 600 feet. In Oneida county, this sandstone is often a conglom- 
 erate, with quartz pebbles rarely exceeding three quarters of an inch in 
 diameter ; from which it has been designated the Oneida conglomerate. 
 In some places, it attains the thickness of twenty-five feet; and it is 
 supposed by Prof. Hall to be the equivalent of the conglomerate of the 
 Shawangunk Mountain. To the eastward of Oswego, the Medina forma- 
 tion, like the sandstone beneath it, dies out ; and in the southern part of 
 Herkimer county, the Clinton formation, about to be described, is only 
 separated from the Hudson River shales, by a small thickness of the 
 Oneida conglomerate. This, in its turn, also disappears, still farther to 
 
CHAP. XIL] 
 
 MEDINA AND CLINTON FORMATIONS. 
 
 311 
 
 the east ; and at the base of the Helderberg hills, the whole Middle Silu- 
 rian series is represented by only a few feet of strata. (Hall's Palaeontol- 
 ogy, Vol. II, p. 1.) 
 
 On the Genesee River, the Grey band is succeeded by twenty-three 
 feet of green shale, supporting a bed of oolitic fossiliferous peroxyd of iron New York - 
 of fourteen inches. Above this are fourteen feet of a limestone, described 
 as silieious, but more probably magnesian ; characterized, among other fossils, 
 by Stenopora fibrosa, Strophomena Clintonensis, Atrypa hemispherica, A* 
 congesta, and more particularly by Pentamerus oblongus. This is followed 
 by twenty-four feet of green shale, succeeded by eighteen feet of a limestone 
 
 316 a 
 
 314-317. BRACHIOPODA. 
 
 314 
 
 315 a 
 
 314. Strophomena rhomboidalis (Wahlenberg). 
 
 315. S. pecten (Linnaeus) ; a, ventral ; 6, hinge view. 
 
 316. S.' Leda (Billings) ; a, ventral valve ; b, portion 
 
 of the area of ventral valve, magnified to show the stri- 
 ated teeth ; c, ventral valve of a specimen without ears, 
 supposed to be the same species. 
 
 317. S. Philomela (Billings) ; a, and 6, two specimens 
 
 of different forms. 
 
 like the last ; containing the characteristic species, Spirifera radiata and 
 BeyricMa lata. These beds constitute the Clinton formation ; which has here 
 a thickness of about eighty feet. On the Oswego River, it appears from the 
 geological map of the State Survey, to have a greater breadth, but its 
 thickness is not stated ; it gradually thins down however, to the eastward, 
 and disappears in Montgomery county. 
 
 ; To the westward, the Medina and Clinton formations run in two parallel 
 zones along the south side of Lake Ontario, and cross the Niagara River 
 
312 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XII. 
 
 Medina in into Canada; the Medina increasing, and the Clinton diminishing in 
 volume. On the south side of Lake Ontario, the base of the Medina is 
 concealed under the waters of the lake ; but it is exposed on the north 
 side, to the eastward of Oakville, near the line between the counties of 
 Halton and Peel ; where it succeeds to the Hudson River formation, without 
 the intervention of the grey sandstone of Oswego. At the base, it consists 
 of red and green striped slaty sandstones and shales, with a few obscure 
 fucoids. At Wellington Square, one of its members, about 400 feet from 
 the base, crops out as a thick red coarse grained sandstone ; which yields 
 to the influence of the weather, on exposure, and is therefore unfit for 
 building purposes. The remainder of the series of beds, up to the lower 
 band of grey sandstone, is made up of red shales or marls, with green spots 
 and stripes; interstratified with thin bands of red sandstone. The upper 
 
 -BKACHIOPODA. 
 
 a 319 
 
 318 
 
 320 
 
 318. Orthis Davidsoni (DeVerneuil) ; a, dorsal ; b, side view. 
 
 319. 0. porcata (McCoy) ; a, dorsal view ; b, side view. 
 
 320. 0. elegantula (Dalman). 
 
 part of the formation is well displayed on the north side of Burlington Bay ; 
 and from Hamilton to the Niagara River, sections of it may be seen in 
 almost every brook that has worn a channel from the ridge to the lake. 
 The best development of this part occurs on the Niagara River, where there 
 is exposed a section, including the Grey band, of more than 200 feet. These 
 strata can be traced, dipping up the river, on both sides, from Queenston and 
 Lewisville, to within a quarter of a mile of the cataract ; the direct dis- 
 tance being about four miles. The total thickness of the formation at 
 the western end of Lake Ontario, is computed to be 614 feet. The only 
 organic remains which have been obtained from it, are Arthropliycu* 
 Harlani, near the top of the red portion at St. Catherines ; with an 
 undescribed fucoid, and lAngula euneata, from the forty-ninth lot of the 
 township of Niagara. 
 
 In Canada, for reasons which will be stated in describing the Niagara 
 formation, it is found convenient to limit the Clinton to the strata beneath 
 the Pentamerus band, and to include this band in the Niagara formation. 
 On the Niagara River, the Clinton is thus limited to a few feet, but it 
 gradually augments in thickness to the northward. 
 
CHAP. XII.] MEDINA AND CLINTON FORMATIONS. 
 
 In the cutting of the Welland Canal at Thorold, about seven miles to 
 the west, the Grey band is a white fine-grained sandstone, somewhat irreg- 
 ularly deposited; the beds thinning out, and occasionally coming to wedge- 
 shaped terminations. When of sufficient thickness, they afford excellent 
 material for the purposes of construction, and altogether constitute a mass of 
 about ten feet. Immediately above this band, the Clinton appears, con- 
 sisting of four feet of bluish and greenish argillaceous shale, presenting 
 fucoids on the surfaces of the beds : among these are fine examples of 
 Arthrophycus Harlani, especially near to the underlying sandstone. The 
 shales here show no indication of the fossiliferous iron ore beds. 
 
 At Mr. Goodenow's quarry, about a mile and a half west from the village 
 of Thorold, and immediately above the Grey band, which is there ten feet 
 thick, there occur the following Clinton strata, in ascending order : 
 
 Ft. in. 
 
 Bluish-green argillaceous shale, 4 
 
 Bluish-grey limestone, abounding in iron pyrites for an inch on the top, 2 9 
 Bluish-drab argillaceous limestone, yielding a hydraulic cement, .... 3 1 
 
 9 10 
 
 In the neighborhood of Hamilton, the Grey band is about twelve feet 
 thick, and the Clinton strata which succeed are 
 
 Ft. in. 
 
 Blue thin-bedded limestone, with thin partings of bituminous shale, . 9 
 Bluish thin-bedded limestone, somewhat slaty in the lower part, ... 36 
 
 Green shale, with thin irregular beds of limestone, 19 
 
 Measures concealed, but supposed to be similar shales, 18 
 
 49 6 
 
 On the Sydenham road, on the sixteenth and seventeenth lots of 
 the first range of Fiamborough West, near Dundas, the whole formation 
 appears to be still thicker. The following are the details of the section 
 in ascending order ; 
 
 Whitish and grey sandstone with ferruginous spots, in two beds, Ft. in. Ft. in. 
 constituting the Grey band, 8 6 
 
 Grey thin shaly sandstones, weathering yellowish, and divided by 
 partings of bluish-grey shales ; containing, in addition to fucoids, 
 Mrypa plano-convexa, Modiolopsis ortkonota, a new species of 
 Cyrtodonta, and Murchisonia subulata, 11 
 
 Grey compact calcareous sandstone in two beds, with a thin parting 
 of pyritiferoug shale ; small nodules of iron pyrites, with fucoids 
 and other fossils, stand out on exposed surfaces. Among them 
 are Stenopora fibrosa, Zaphrentis Stokesi, crinoidal columns, 
 Heliopora fragilis, Ptilodictya crassa, Ph&nipora ensiformis } 
 Strophomena rhomboidalis t Orthis elegantula, Rhynchonella ne- 
 glecta, Athyris naviformis, Jltrypa plano-convexa, and Tentaculite* 
 distant, , 1 9 
 
314 GEOLOGY OF CANADA. [CHAP. XII. 
 
 Ft. in. 
 
 Dark bluish-grey limestone, sometimes of a purple tinge, and weath- 
 ering to a pale red ; in beds separated by partings of bluish-grey 
 shale, passing into black and sometimes buff; containing, among 
 other fossils, Stenopora fibrosa, Zaphrentis Stokesi, Heliopora 
 fragilis, Ptilodictya crassa, Phcenipora ensiformis, Rhinopora ver- 
 rucosa, Fenestella prisca, Strophomena rhomboidalis, S. pecten, 
 Orthis lynx, 0. elegantula, Rhynchondla neglecta, Athyris navi- 
 formis, Atrypa reticularis, A. plano-convexa, Spirifera radiata, 
 Modiolopsis orthonota, a new species of Cyrtodonta, Murchiso- 
 nia, subulata, Orthoceras, Calymene Blumenbachii, and Encrinurus 
 
 punctatus, 7 
 
 Bluish-grey argillaceous shales, with green layers, and thin bands of 
 impure limestone, which hold fossils similar to the last. The 
 
 lower beds are marked with small green spots, 8 
 
 Buff shales, with thin bands of limestone holding Stenopora fibrosa, 
 an undetermined Petraia, Heliopora fragilis, Rhinopora verru- 
 cosa, Strophomena rhomboidalis, Orthis lynx, Atrypa reticularis, 
 A. plano-convexa, and Athyris cylindrica. The disintegrated 
 shales of this and the previous division are used as fire-clay,.. . . 12 
 
 Measures concealed, T 4 
 
 Bluish-grey calcareo-arenaceous shale, with argillaceous bands, ... 11 
 Green and grey calcareo-argillaceous and arenaceous shale, with 
 calcareous sandstones towards the top. The beds hold a few 
 fossils ; among which are Heliopora fragilis, Ptilodictya expla- 
 nata, and two or three undetermined species of Ctenodonta,. ... 10 8 
 
 Red calcareous sandstone in thin beds, 1 
 
 Green argillo-arenaceous shale, 2 
 
 Red marly shale, 4 
 
 Red ferruginous calcareo-arenaceous rock, being a very earthy 
 haematite, holding various fossils. Among them, in addition to 
 fucoids, are Stenopora fibrosa, Heliopora fragilis, an undetermined 
 Rhynchonella, Avicula emacerata, A. rhomboidea, an undetermined 
 Orthonota, and Dalmanites trisulcatus. In the equivalent of the 
 same stratum, on the eleventh lot of the first range of the town- 
 ship, besides most of the previous species, there are met with 
 Rhinopora verrucosa, Ptilodictya explanata, Strophomena rhom- 
 boidalis, Rhynchonella neglecta, Avicula alata, with undetermined 
 species of Cyrtodonta, Ctenodonta, Murchisonia, and Orthoceras. 
 
 This probably represents the iron ore bed of Rochester, 1 
 
 Red ferruginous calcareo-arenaceous rock, of the same character as 
 before, becoming reddish-brown at the top ; with partings of red 
 marly shale. Corals and bivalve shells occur in some abundance 
 
 in the bed, 1 8 
 
 Red argillaceous shale, with green stripes and patches, and with thin 
 
 bands of red and green limestone, 5 
 
 Pale green argillaceous shale, with three bands of lirnqstone, 50 
 
 Greenish calcareo-argillaceous and arenaceous shale, with thin divi- 
 sions of a more decidedly green shale, 1 3 
 
 Pale bluish-green calcareous sandstone, with nodules of iron pyrites 
 and ferruginous spots and stripes. Obscure fucoids, corals, and 
 shells occur in the bed, 1 9 
 
CHAP. XII.] MEDINA AND CLINTON FORMATIONS. 315 
 
 Ft. in. Ft. in. 
 
 Pale bluish-green calcareous sandstone, with partings of bluish-green 
 shale, marked by nodules of iron pyrites and by ferruginous 
 stains. Corals, encrinites, and broken shells occur in great abun- 
 dance at the top, 3 10 
 
 Bluish-green argillaceous shale, 1 3 
 
 92 5 
 
 100 11 
 
 The strata of this section are limited by a bold escarpment, composed of 
 the rocks of the Niagara formation, which succeeds. By this escarp- 
 ment, they are easily traceable from Flamborough West, in a north-easterly 
 direction, through Flamborough East into South Nelson. On entering the Collingwood. 
 latter township, they take a sweeping turn northward, and maintain a 
 general course somewhat westward of north, for seventy-five miles, from 
 South Nelson to Collingwood. The inclination of the measures being very 
 
 321-225. BKACHIOPODA. 
 
 323 
 
 321. Rhynchonella rugosa (Hall). 
 
 322. .R. camura (Hall). 
 
 323. R. cuneata (Hall). 
 
 324. R. brevirostris (Hall). 
 
 325. fl. neglecta (Hall). 
 
 small, probably not exceeding thirty feet in a mile, the outcrop of the 
 series, particularly at the summit, presents a very indented outline, 
 running into deep bays in the valleys of the principal streams; where 
 bold ravines are worn in the rock above. Two of the main indenta- 
 tions are on the Credit in Caledon, and on the Nottawasaga in Mono; 
 between which, the limit of the series spreads out considerably to the 
 eastward in Adjala and Albion. Several minor indentations occur north 
 of this, in Mono and Mulmur, and deeper ones on the Noisy and Mad 
 Rivers in Nottawasaga. From Collingwood, the general outcrop turns to 
 the north-west ; but it presents a very deep sinus, southward, up the valley 
 of the Beaver River, reaching nearly to the centre of the township of 
 Artemisia ; and another up the valley of the Bighead, in St. Vincent, 
 Sydenham, and Holland. A third indentation carries the outcrop a few 
 miles up the Sydenham River ; which flows through the town of Owen 
 Sound into the bight of the bay. 
 
 Though the Clinton strata are thus easily traced, by the conspicuous 
 escarpment which rises precipitously above them, they themselves are but 
 
316 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XII. 
 
 seldom seen, being for the most part concealed by a talus of debris. The 
 base of the series, however, is nearly as well marked as the summit, by the 
 sandstone of the Grey band ; which crops out from below them, and forms 
 a low but distinct terrace. 
 
 Grey band. Q^ ne (} re y band is seen at intervals, all the way from Flamborough West 
 to the township of Mono ; varying in thickness from ten to twenty feet, but 
 preserving a pretty uniform lithological character. It is exposed also in 
 many places in Nottawasaga and Mulmur. On the twenty-fourth lot of the 
 tenth range of the former, it attains the thickness of thirty-five feet ; above 
 which, the Clinton strata present a volume of ninety-two feet. The Grey 
 
 326-827. BRACHIOPODA. 
 
 326. Pentamcrus oblongus (Somerley). 
 
 327. P. Barrandi (Billings); a, dorsal view; 6, 
 
 side view. 
 
 band has not yet, however, been observed in any of the townships west of 
 Nottawasaga and Collingwood. In several places in the township of 
 Sydenham, the thin bedded limestones of the Clinton formation are seen to 
 rest upon the red and green shales of the Medina ; thus proving the absence 
 of the Grey band to the westward, unless perhaps in isolated portions. 
 This sandstone, wherever it has been examined between Queenston and 
 Collingwood, is of a whitish or pale grey color, sometimes striped and 
 spotted with ferruginous stains. It is always well adapted for building 
 purposes, and is, in many instances, a very beautiful and easily wrought 
 material. It has been extensively quarried near Hamilton and Dundas, at 
 'Waterdown in the township of Flamborough East, as well as near 
 Georgetown in Esquesing ; and it is equally fit for use nearly all 
 .the way along its outcrop, to the township of Nottawasaga. In many 
 
CHAP. XII.] 
 
 MEDINA AND CLINTON FORMATIONS. 
 
 317 
 
 places towards the north, it is sufficiently free and uniform to yield 
 very good grindstones ; for the manufacture of which it is used from 
 Orangeville to the vicinity of Bowmore, in Nottawasaga. These various 
 applications render the Grey band of considerable economic importance in 
 the district. 
 
 The upper parts of the Medina formation are seen beneath the Grey Owen sound, 
 band, in several places along their outcrop northward ; but the lower parts 
 being much covered with drift, it is not easy to trace the limits of the 
 base. The thickness of the series greatly diminishes in that direction ; 
 
 828-334. BRACHIOPODA. 
 
 328. Spirifera radiata (Sowerby) ; a, side view ; 6, dorsal view. 
 
 329. Sf. Niagarensis (Conrad). 
 
 330. Athyris naviformis (Hall). 
 
 331. A. umbonata (Billings) ; a, dorsal view; 6, side view. 
 
 332. A. crassirostra (Hall). 
 
 333. v. cylindrical (Hall). 
 
 334. 4. nitida (Hall). 
 
 and on the twenty-fourth lot of the tenth range of Nottawasaga, it scarcely 
 attains 200 feet. With this diminished volume, however, it appears 
 to be spread out, more extensively than elsewhere, in the townships of 
 Collingwood, Euphrasia, St. Vincent, and Sydenham. Over a considerable 
 part of these townships, the red marls, in a disintegrated state, form an 
 excellent surface soil ; and in many places in this area, they are seen in 
 place, where the ground is broken by ditches, the channels of brooks, and 
 road cuttings. In these townships, the Clinton formation also spreads out 
 somewhat wider than usual ; and the red ferruginous band which marks the 
 upper part of it, is met with in several exposures; though nowhere 
 
318 GEOLOGY OF CANADA. [CHAP. XII. 
 
 sufficiently charged with iron to constitute a workable ore. In the second 
 lot of the fourth and fifth ranges of St. Vincent, in a bed of bluish shale, 
 near the summit of the formation, crystals of gypsum are disseminated 
 in some abundance. 
 
 Owen sound. At Owen Sound, the Medina rocks are limited above by about 
 twenty feet of dolomite, which here constitutes the base of the Clinton 
 formation. This dolomite, which is of a yellowish-color and weathers yel- 
 lowish-brown, contains, in great numbers, a few species of silicified fossils ; 
 among which are an undetermined Petraia, Strophomena rhomboidalis, and 
 an undescribed Orthis, resembling 0. testudinaria. Between it and the base 
 of the massive limestones, which are classed with the Niagara series, the 
 
 335-337. BRACHIOPODA. 
 
 337 
 
 335. Atrypa reticularis (Linnaeus) ; a, dorsal ; 6, side, and c, ventral view. 
 
 336. A. plano-convexa (Hall) ; a, dorsal, 6, side, and c, ventral view. 
 
 337. A.hem.ispherica (Sowerby) ; a, dorsal, and 6, side view. 
 
 surface is covered with red clay. The strata from which this is derived, 
 no doubt represent the iron ore bed, and are seen in several places within a 
 circuit of three miles. From the bight of Owen Sound, the Medina and 
 Clinton formations are traceable along nearly the whole lake front of the 
 township of Keppel ; and in the vicinity of Cape Commodore, their entire 
 thickness can be determined by actual measurement. Strata of the 
 Hudson River formation here constitute the base of a cliff; above which the 
 red and green Medina shales present a volume of 109 feet. Besting upon 
 these, the Clinton formation shows about thirty-six feet of thin bedded 
 magnesian limestone ; between which and the abrupt overlying escarpment 
 of the Niagara series, there is a thickness of about 150 feet. In 
 this, the strata are partially concealed; but a considerable portion of 
 them appears to be red shales. The base of the Clinton appears to cross 
 Colpoy's Bay, at about three and a half miles, and the summit, at about two 
 
CHAP. XII.] 
 
 MEDINA AND CLINTON FORMATIONS. 
 
 319 
 
 and a quarter miles, from its western extremity ; leaving a mile and a 
 quarter for the breadth occupied by the formation. From this, it would 
 appear that the slope of the strata in this part, is about 120 feet in a mile. 
 The same two formations occupy the lake front of the townships of 
 Albemarle and Eastnor, with the exception of the peninsula terminating 
 in Cape Crocker. This consists of Hudson River strata ; and is overlooked 
 from the westward by a bold escarpment, in the lower part of which 
 the two formations occur. The summit of the Medina series disappears 
 beneath the water at Cape Dundas ; while the Clinton continues along the 
 
 ). CRUSTACEA. 
 
 338. Bumastes Barriensis (Murchison). 
 339. Homalonotus delphinocephalus (Green). 
 
 water line, as far north as Cape Chin, rising at Cape Gun and Point 
 Hungcliff to about the height of a hundred feet. 
 
 At Cabot's Head, the very summit of the Medina formation is seen at Cabot's Head, 
 the water's edge ; and there rest upon it about twenty-six feet of a dolomite, 
 similar in its color and its weathering to that of Owen Sound ; which it 
 also resembles in holding silicified fossils. Here the species are Stenopora 
 fibrosa, Favosites Gothlandica, an undescribed species of DipJiypJiyllum^ 
 Stromatopora concentrica, Strophomena rliomboidalis, S. pecten, Orthis 
 Davidsoni, Atrypa plano-convexa, with undetermined species of Murchi- 
 wnia and Pleurotomaria. On the dolomite, repose 103 feet of red marly 
 sandstones, partially striped and spotted with green, and interstratified 
 
320 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XII. 
 
 with beds of red and green argillaceous shale ; none of which exceed six 
 or eight inches in thickness. The green argillaceous beds appear to be 
 quite free from calcareous matter, and the stone is carved by the Indians 
 into tobacco pipes. These red and green strata are succeeded by about 
 fifty-five feet of green calcareo-argillaceous shales and thin bedded lime- 
 stones, and terminated by the massive limestones of the Niagara series. 
 
 At the base of a cliff composed of the red strata, loose fragments are 
 met with, which strongly resemble the earthy hsematitic iron ore of 
 Rochester. They are marked by Heliopora fragilis and Ptilodictya 
 explanata; which characterize the ore bed elsewhere. It would appear 
 that the red strata of Cabot's Head, are only an expansion of the ferruginous 
 beds which underlie the Pentamerus band at Flamborough West. 
 
 Proceeding north-westward, these red beds are found in place on the 
 north-eastern point of Horse or Fitzwilliam Island ; and the subjacent 
 dolomites, on a small island about a couple of miles northward. 
 
 340. CRUSTACEA . 
 
 340. Dalmanites limulurus (Green). 
 
 Manitouiin From this, the dolomitic strata, striking into the Great Manitoulin 
 Island, reach Manitoulin Gulf; near the upper end of which they are 
 exposed on the east side, composing a cliff of about forty feet in height ; 
 on the beds of which, at the summit, a great many silicified fossils are 
 weathered into relief. They here consist chiefly of the species Stenopora 
 fibrosa, an undetermined Petraia, Strophomena rhomboidalis, S. pecten, 
 an undetermined species of Orthis, 0. lynx, and 0. Davidsoni, with 
 Atrypa plicatula. The red strata of the Clinton above, and those of the 
 Medina below these dolomites, are here covered up; but about thirteen 
 miles to the westward, on Tecumseh Lake, a red marly clay, probably 
 derived from the Clinton formation, is washed up from the base of the 
 Niagara limestones. 
 
 It is probable that the Clinton formation extends through the length of 
 the Grand Manitoulin Island, as well as that of Cockburn and Drummond 
 Islands, striking across the various deep bays, which indent all these islands 
 
CHAP. XII.] NIAGARA FORMATION. 321 
 
 on the north side. Its position in these bays must be somewhat north of 
 their most southern parts ; and in crossing the largest bay of the Grand 
 Manitoulin, its strike would seem to carry it under the water, not far south 
 of Barrie Island. The probability of the continuance either of this or of the 
 Medina formation, is supported by the reported occurrence of red strata 
 on the Sucker River, on the Michigan side of St. Mary River, nearly 
 opposite to the southern extremity of St. Joseph Island: this would be 
 in the strike of the Clinton. From Tecumseh Lake westward, however, 
 it is only by the position of the Niagara strata above, and those of the 
 Hudson River below, that its course, and that of the Medina, can be 
 inferred; no exposures belonging to these formations having yet been 
 observed in Canada, in that direction. 
 
 THE NIAGARA FORMATION. 
 
 The rocks of this formation in the state of New York do not extend far- New York, 
 ther eastward than the township of Litchfield in Herkimer county ; falling 
 short of the termination of the Clinton deposits, in that direction, by about 
 forty miles. The formation first appears in that part of the state as an 
 unimportant mass of dark bluish impure concretionary limestone, enclosed 
 in shales of the same color. The concretionary layers, which do not exceed 
 a few feet in thickness, present a mammillated surface ; the elevations vary- 
 ing in diameter from three inches to three feet. 
 
 As the formation extends westward, its volume gradually increases ; and 
 at Rochester it attains a thickness of about 180 feet, consisting of about 
 a hundred feet of very fossiliferous blackish-blue calcareo-argillaceous 
 shale, supporting eighty feet of limestone. This is composed, at the base, 
 of bluish-grey silicious limestone fit for hydraulic purposes ; followed by 
 bluish-grey sub-crystalline thin bedded limestone, with partings of black 
 shale ; to which succeeds a lighter grey sub-crystalline contorted and concre- 
 tionary limestone. On this rests a dark bluish-grey thick bedded bituminous 
 limestone with irregular cavities and with masses of chert; followed by a 
 brownish-grey bituminous thin bedded limestone, holding occasional nodules 
 of the same mineral. 
 
 At Lockport and Niagara, the thickness of the shale, as given by Mr. 
 Hall, is eighty feet, and that of the limestone 164 feet. The shale includes, 
 at the top, a few beds of argillaceous limestone, yielding a good water 
 cement, and constituting a passage to the calcareous rock above. The 
 lower part of this consists of a grey cemented mass of broken encrinal 
 columns, often beautifully variegated with red. To this succeeds a thick 
 bedded grey sparry limestone, followed by beds of a darker color, upon 
 which rest a brownish bituminous limestone, sparry below, and marked by 
 
 v 
 
322 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XII. 
 
 Base of Ni- 
 agara series. 
 
 Thorold sec- 
 tion. 
 
 the presence of the sulphurets of zinc and of lead above. The whole is 
 crowned by a series of dark grey slaty calcareous beds, with mammillated 
 surfaces, separated by thin laminae of bituminous shale. A large proportion 
 of these limestones has been ascertained to be magnesian. In the slope 
 and precipice over which the rapids and the cataract of Niagara fall, the 
 whole thickness of these limestones is exposed ; so that to this series, with 
 the shales below, the geologists of New York have given the name of 
 the Niagara group. 
 
 The bluish-black shales which in the state of New York afford a well 
 marked division between the Clinton and Niagara formations, are avail- 
 able for this purpose but for 'a short distance in Canada. To the north- 
 ward, these shales thin out and disappear; and it is for the present very 
 difficult to distinguish them in that direction. We therefore propose to 
 include in the Niagara series, the two bands of limestone which underlie 
 the shales, and which, in New York, constitute the upper part of the 
 Clinton formation. So far as they have been examined in Canada, these 
 two limestone bands contain no Clinton fossils, but such as pass upwards 
 into the Niagara ; and the upper band here possesses one or two species, 
 which, in New York, are considered to belong to the latter group only. 
 There would thus appear, at present, to be no palaeontological reason why 
 these limestones may not be considered the base of the Niagara formation ; 
 while geographically they present a very marked feature for a considerable 
 distance, and afford a convenient means of describing the distribution of 
 the two formations. 
 
 Including these limestones, the Niagara strata seen in the cutting of 
 the Welland Canal, near Thorold, in immediate succession to the Clinton 
 formation, are as follows, in ascending order : 
 
 1. Bluish-grey magnesian limestone, with partings of bluish calca- Ft. in. 
 
 reous shale. Concentric rings of discoloration are observable 
 around small cavities lined with calcspar, which occur generally 
 at the surface of vertical joints, cutting the strata at right angles. 
 The circles are usually so large as to cross the divisional planes 
 of several beds. Pentamerus oblongus and Stricklandia Canadensis 
 occur in abundance, 10 
 
 2. Grey coarse grained sub-crystalline limestone, with disseminated 
 
 iron and copper pyrites ; the bed abounds with fossils, among 
 which, on the canal, are JLtrypa reticularis, Rhynchonella cuneata, 
 
 and Jlthyris cylindrica, ; 10 
 
 In the upper five feet of this bed, in Mr. Goodenow's quarry, a 
 mile and a half to the westward, there are fragments of an unde- 
 termined species of Rhodocrinus, of Eucalyptocrinus decorus, and 
 Cyathocrinus ornatus ; the latter two species are given as char- 
 acteristic of the Niagara series of New York. 
 
 3. Bluish-black bituminous shale, with thin bands of impure limestone, 
 
 holding trilobites and a few shells. Among the trilobites, Dalman- 
 ites caudatus is frequent. In some places, thin bands of gypsum 
 
CHAP. XII.] NIAGARA FORMATION. 323 
 
 Ft. in. 
 
 occur, giving a riband-like aspect to the shale. Small nodules of Gypeum. 
 
 gypsum are also sometimes met with, as well as crystals of 
 iron pyrites. This shale constitutes the base of the Niagara 
 group of New York, 55 
 
 4. Bluish-grey argillaceous limestone,yielding excellent water cement, Water lime. 
 
 which was much used in building the locks of the Welland Canal, 8 
 
 5, Dark bluish bituminous limestone, in some places yielding material 
 
 fitted for purposes of construction, as at Mr. Reefer's quarry at Tho- 
 .rold. The upper and under surfaces of adjacent beds are often 
 united by suture-like joints ; the parts interfiling being sometimes 
 two inches in depth, with vertical columnar sides, usually glazed 
 with a thin pellicle of argillaceous matter. Crystals of galena 
 are frequently met with in these beds, which contain many fossils. 
 Among these, where the rock is cut through by the Welland rail- 
 way, about 200 yards on the strike from the canal, are Stenopora 
 fibrosa, Favosites Gotklandica, F. Hisingeri, Heliolites interstincta, 
 Halysites catenulalus, JLlveolites repens, Petraia calicula, Zaphren- 
 tis Stokesi, Z. Marcoui, an undetermined Diphyphyllum, Stepha- 
 nocrinus angulatus, Eucalyptocrinus decorus, Caryocrinus ornatus, 
 Stromatopora concmtrica, an undetermined Fenestella, Lept&na 
 transversaliSj Strophomena rhomboidalis, S. pecten, S.profunda? 
 Orthis elegantula, 0. hybrida, Spirifera crispa, S. radiata, S. Nia- 
 garensis, Jitrypa, reticularis, Rhynchonella neglecta, R. cuneata, 
 Jlthyris nitida, A. crassirostra, Cyrtena pyramidalis, Avicula sub- 
 plana, Platyostoma Niagarensis, P. hemispherica, dcroculia Nia>- 
 garensiSjCalymene Blumenbachii, Encrinurus punciatus, Dalmanites 
 caudatus, Homalonotus delphinocephalus, and Bumastes Barriensis, 8 
 
 6. Light and dark grey magnesian limestone, in beds varying from 
 
 six to ten feet in thickness, constituting a building stone of the 
 best description. It is a cemented mass of broken encrinites, with 
 a few additional fossils, and in some parts holds geodes filled with 
 snow-white gypsum, 26 
 
 7. Bluish bituminous limestone well suited for purposes of construc- 
 
 tion, though inferior to the preceding mass. It holds many fossils, 
 principally corals, 7 
 
 124 
 
 This section represents all the beds of the series which are crossed on the Hamilton 
 canal, up to the highest part of the ridge, near Thorold ; but it does not 8e 
 reach the summit of the series by probably ninety feet. Proceeding west- 
 ward, the volume of the black shales diminishes, while that of the lime- 
 stones beneath them augments ; and in the neighborhood of Hamilton and 
 Ancaster, we have the following succession, in ascending order: 
 
 Ft. in. Ft. in. 
 1. Light grey magnesian limestone, weathering yellowish, and 
 
 holding Pentamerus oblongus in great abundance, 1 6 
 
 Grey magnesian limestone, with geodes of calcspar in the lower, 
 and broken encrinites in the upper part, 9 3 10 9 
 
324 GEOLOGY OF CANADA. [CHAP. XII. 
 
 Ft. in. Ft. in. 
 
 2. Bluish argillaceous and arenaceous shale, with thin bands of 
 
 sandstone, 5 
 
 Grey arenaceous limestone, 3 5 
 
 Bluish shale, 1 
 
 Bluish-grey argillaceous limestone, with geodes of calcspar ; 
 
 this is probably fit for water cement, 5 7 15 
 
 3. Whitish limestone, with geodes of calcspar, containing nodules 
 
 and patches of chert in considerable abundance, 16 6 
 
 4. Bluish-black bituminous shale with thin bands of limestone 
 
 holding fossils ; the shale, which is in very thin laminae, pre- 
 sents surfaces covered with bituminous matter, and nodules 
 of chert are sometimes met with in the limestone, 60 
 
 5. Grey strongly bituminous limestone, very unevenly deposited, 5 
 Reddish-grey, drab-weathering, bituminous, magnesian lime- 
 stone, moderately thin bedded ; with partings of bituminous 
 shale. The limestone holds disseminated crystals of galena 
 
 | associated with pearl-spar. This is equivalent to the bluish- 
 black shale, 3, of the previous section, 5 100 
 
 6. Grey compact tough magnesian limestone, 3 
 
 Bluish magnesian limestone, weathering into small pits on the 
 
 surface, and containing small nodules of a carbonaceous 
 
 matter, resembling coal, 3 
 
 Blue and grey compact magnesian limestones, 3 
 
 Grey compact magnesian limestone, 3 
 
 Bluish magnesian limestone, weathering into irregular pits on 
 the surfaces of the beds. The rock holds small masses of car- 
 bonaceous matter as above, 3 
 
 Bluish-grey compact magnesian limestone, presenting under 
 the influence of the weather a rough pitted surface, 5 200 
 
 78 3 
 
 Blende and T^ e limestones, 5, which overlie the black shales, 4, form the upper part 
 galena. O f the ridge which extends between the falls of Niagara and the village of 
 Ancaster. They are highly bituminous, and for the most part magnesian for 
 the whole distance ; and they abound in fine cabinet specimens of selenite, 
 celestine, pearl-spar, blende, and galena. Crystals of the latter mineral exist 
 in greater or less quantity, in nearly all the limestones from the Pentamerus 
 band to the summit of the upper beds ; but they are in the greatest abun- 
 dance in the latter, especially in the township of Clinton, near the village of 
 Beamsville, where an unsuccessful attempt was made by Mr. Lee to estab- 
 lish a lead mine upon what was supposed to be a lode, on a lot of the eighth 
 range of the township, which is the property of Mr. R. Comfort. The 
 supposed lode, however, appears to be rather one of the open joints or 
 fissures, running E. and W.,by which these rocks are intersected in many 
 places. In the locality in question, the fissure, which is filled up with drift, 
 is crossed by small cracks, the walls of which are invested with crystals 
 
CHAP. XII.] NIAGARA FORMATION. 
 
 of pearl-spar and galena. The ore is also seen on each side of the 
 main fissure, and is moreover disseminated throughout the limestone, 
 near the fissure. 
 
 Northward from this, the black shale, 4, maintains for a few miles the 
 thickness which it presents in the last section, and it is recognized above 
 the beds already described as composing the Clinton formation, on the 
 sixteenth and seventeenth lots of the first range of Flamborough West, 
 near Pundas (p. 313). In ascending order, these succeeding beds are West - 
 
 Ft. in. Ft. in. 
 
 1. Grey magnesian limestone, with Pentamerus oblongus in abun- 
 
 dance, and a few other fossils, chiefly fucoids ; besides a Fen- 
 estella, and an undetermined trilobite, 1 
 
 2. Blue magnesian limestone, in very even and regular beds, of 
 
 which the thickest are from sixteen to eighteen inches; sepa- 
 rated by partings of bluish-grey shale. The limestone is used 
 for building purposes ; it is fossiliferous, and shows fucoids, 
 crinoidal joints with Favosites Gothlandica, and undetermined 
 species of Fenestella, Orthis, and Rhynchonella, 7 
 
 3. Light grey magnesian limestone in one bed ; this is used for 
 " building purposes and is known by masons and quarrymen 
 
 as the five-feet band. It holds fossils, among which are 
 crinoidal columns, Fenestella tenuis, Strophomena pecten, 
 Orthis elegantula, Rhynchonella neglecta, Jlthyris naviformis, 
 Jltrypa reticularis, and Spirifera radiata, 5 6 13 6 
 
 4. Bluish-grey calcareo-arenaceous shale, passing into black ; it is Black ehalee 
 
 hard and solid in the bed, but disintegrates and crumbles into 
 a clay, when exposed to the atmosphere ; with the exception 
 of thin interstratified beds, which resist the weather. Among 
 its fossils are fucoids, Stenoporafibrosa, fragments of crinoids, 
 Ptilodictya crassa, Rhincopora verrucosa, Retepora angulata, 
 Fenestella prisca, Strophomena rhomboidalis, S. pecten, Orthis 
 elegantula, Rhynchonella robusta, R. neglecta, Jlthyris navifor- 
 mis, Atrypa reticularis, Spirifera radiata, and Cyclonema 
 obsoleta. In the same bed, on the eleventh lot of the first 
 range of the township, are Fenestella tenuis, Rhynchonella 
 cuneata, and an undetermined Platyostoma, 60 
 
 5. Bluish-grey magnesian limestone, composed chiefly of broken 
 
 encrinites. The beds are from three to four feet thick, and are 
 separated by very thin layers of buff colored argillaceous 
 shale. This limestone forms an excellent building stone, for 
 which it is used, as well as for burning. It holds fossils, 
 among which are fucoids, Stenopora fibrosa, Favosites Goth- 
 landica, Zaphrentis Stokesi, Eucalyptocrinus decorus, and 
 fragments of other crinoids, Strophomena rhomboidalis, S. 
 pecten, Rhynchonella neglecta, Jlthyris naviformis, Jltrypa reti- 
 
 cularis, Ji. plano-convex a, Spirifera radiata, S. ? Ortho- 
 
 ceras undulatum, and Calymene Blumenbachii, 19 3 
 
 6. Dark bluish-grey argillaceous shale ; this is a well marked 
 
 band, and may be traced for some distance on the strike,. . . 1 20 3 
 
326 GEOLOGY OF CANADA. [CHAP. XII. 
 
 Ft. in. Ft. in. 
 
 7. Blue and grey limestone, including bands of white, buff, and 
 
 grey chert, and thickly studded with chert nodules. Besides 
 fucoids, it holds Favosites Gothlandica, crinoidal fragments, 
 Ptilodictya crassa, P. ensiformis, Rhynchonella neglecta, and 
 Dal man-ties caudatus, 20 
 
 8. Brownish bituminous magnesian limestone, with small dissem- 
 
 inated crystals of galena, and a few fossils, 10 
 
 9. Grey bituminous magnesian limestone in rough irregular beds, 5 
 
 10. Measures concealed, 5 
 
 11. Black bituminous magnesian limestone in thin irregular layers, 2 
 
 12. Black bituminous shale, 1 
 
 " 13. Dark brown very bituminous magnesian limestone, in thin beds 
 
 with rough irregular surfaces, 2 
 
 14. Dark brown bituminous magnesian limestone, holding dissem- 
 
 inated crystals of galena, 5 
 
 15. Black fissile shale, 2 
 
 The beds, from 8 to 15 inclusive, are fossil iferous, and con- 
 tain, among other species, in addition to fucoids and crinoidal 
 columns, Strophomena rhomboidalis, S. pecten, Rhynchonella 
 neglecta, a new species of Athyris, Atrypa reticularis, an 
 undetermined species of Cyrtodonta, Encrinurus punctatus, 
 and Conularia Niagarensis. The equivalents of these beds 
 at the Peak, on the north-west side of Dundas, contain, in 
 addition to these, Favosites Gothlandica, Orthis hybrida, an 
 undetermined Lingula, JLthyris nitida, Spirifera bicostata, S. 
 radiata, Pentamerus oblongus, Murchisonia subulata, and Caly- 
 mene Slumenbachii. 
 
 16. Dark very bituminous magnesian limestone with black shale at 
 
 the top, and with numerous fossils, 3 
 
 17. Dark brown bituminous magnesian limestone, 2 
 
 18. Black bituminous shaly limestone, 1 
 
 19. Measures concealed, 2 
 
 20. Black bituminous magnesian limestone with obscure fossils in 
 
 the lower part, 8 
 
 21. Dark grey slaty limestone in thin layers, with an occasional 
 
 band of six inches, 4 6 
 
 22. Dark brown bitumino-arenaceous shale, with fossils, 6 
 
 23. Brownish bituminous limestone with partings and thin bands 
 
 of dark brown bituminous shale, 15 88 
 
 In the beds, from 16 to 23 inclusive, the fossils, in addition 
 to fucoids and crinoidal columns, are, among others, Stroph- 
 omena rhomboidalis, Rhynchonella neglecta, a new species of 
 dthyris, Atrypa reticularis, an undetermined Cyrtodonta, and 
 Encrinurus punctatus. 
 
 In this section, the black shale of the Niagara Falls is supposed to be 
 represented by the bed, 4, underlying the massive encrinal limestones, 5 ; 
 but it produces no marked feature in the form of the surface. 
 
 The rocks of the section in the neighborhood of Dundas, however, 
 form two separate and distinct terraces. The lower and more marked 
 
CHAP. XIL] NIAGARA FORMATION. 327 
 
 escarpment presents the strata beneath the band of cherty limestone, 7, Dundas. 
 which caps the precipice at Flamborough West. The upper escarpment, 
 composed of the dark colored bituminous magnesian limestones and their 
 accompanying beds, rises more gradually, in a succession of steps ; termi- 
 nating at the summit in a wide extent of table-land. 
 
 Northward from Flamborough East, the massive beds of encrinal lime- 
 stone, 5, which pass below the cherty band, form the crest of the lower 
 escarpment, and appear to gradually increase in thickness in that 
 direction. At Mr. McNaughton's farm, on the seventh lot of the seventh Nassagaweya. 
 range of Nassagaweya, there is a vertical precipice, in some places a hun- 
 dred feet in height. It is capped by the encrinal band, while the 
 Pentamerus bed is probably at the base ; but though the stratigraphies! 
 place of the black shale would thus be in the cliff, it has not yet been 
 detected. Nearly the whole mass of rock appears to be a light 
 grey drab-weathering limestone ; usually presenting a black surface in the 
 cliff, from the presence of minute lichens. Much of it appears to be 
 magnesian, and it for the most part abounds in encrinites. It is well 
 adapted for building purposes, but it seems too porous to be made avauV 
 able as a marble. Some of the beds are well adapted for burning to 
 quick-lime, and these probably contain a smaller proportion of magnesia. 
 Though the very base of the limestone is concealed by a talus of debris, 
 its near proximity is indicated by the copious streams of water which 
 flow along its whole outcrop, from the more argillaceous beds beneath, 
 and issue from among the debris ; depositing in their course, large quanti- 
 ties of calcareous tufa. 
 
 In a cutting for the Grand Trunk Railway at Limehouse, on a tributary 
 of the Credit, on the twenty-first lot of the sixth range of Esquesing, the base 
 of the Niagara limestone is seen resting on the beds of the Clinton forma- 
 tion. This has there*a thickness of only thirty-four feet ; not much more 
 than one third of what it presents in Flamborough West. It consists of 
 ten feet of a bluish shale, resting on the Grey band as a base, and over- 
 laid by seven feet of red shale, which represents the iron ore bed. To 
 this succeeds eight feet of bluish shales, followed by nine feet of water-lime. 
 This bed of water-lime rests on a thin bed of arenaceous shale, with a thin 
 seam of reddish sandy clay holding crystals of iron pyrites, and supports a 
 light grey partially magnesian limestone, belonging to the Niagara series ; 
 of which only twenty-seven feet are exposed in the cutting. The charac- 
 teristic Pentamerus oblongm has not been seen here. The species observed 
 are Strophomena peeten, an Ischadites allied to I. Koenigi (the first 
 instance of the genus on this continent) , and Calymene Blumenbachii. 
 
 The river Credit, in Caledon, is flanked on both sides by the cliffs of the 
 Niagara limestone, in some places a hundred feet high ; these, in ascending 
 the valley, meet on the ninth lot of the fourth range of the township, near 
 
328 GEOLOGY OF CANADA. [CHAP. XII. 
 
 Kiver Credit. Bellefontaine, and form a crescent-shaped precipice ; over which the river 
 falls in a cascade. In the valley of the Nottawa, similar cliffs prevail ; 
 and at Orangeville, some of the rock, of a yellowish-white, would take a 
 sufficient polish to constitute a very useful marble. The cliffs continue 
 through Mulmur and Nottawasaga; and on the twenty-fourth lot of the twelfth 
 range of the latter township, the whole mass of this limestone, to the highest 
 part of the escarpment, has been ascertained by measurement to be about 
 160 feet thick. As far as seen, its color appears to be greyish at the 
 base, gradually passing upwards into buff or yellowish-white ; most of the 
 beds being banded with the two colors. The rock, which is magnesian? 
 is harder in the lower than the upper part, and appears to be encrinal 
 for mostjDf the thickness; the encrinites abounding towards the top. It 
 maintains the same colors and characters along what is called the Blue 
 Mountain ridge, through Collingwood, to the point where the ridge 
 approaches nearest to Lake Huron ; and it is probable that the formation 
 thus far does not diminish in volume. 
 
 Artemisia. In the valley of the Beaver River, in Euphrasia and Artemisia, the 
 same limestone has a thickness of at least 120 feet. At the head of the 
 valley, on the twenty-sixth lot of the tenth range of Artemisia, the stream 
 falls over a precipice of seventy feet of this magnesian limestone. Flow- 
 ing thence rather to the east of north, it is flanked on both sides by bold 
 escarpments of the rock, which gradually separate from one another; 
 leaving between them a beautiful and fertile valley, which in a distance of 
 about eight miles, attains a breadth of three miles. In several places the 
 escarpment becomes perpendicular ; and in a precipice on the right side 
 of the valley, about the tenth lot of the third range of Euphrasia, forty- 
 seven feet of the rock appear to constitute a single massive bed, without 
 divisional planes. The color of the rock is, as before, a pale buff or yellowish- 
 white, and the weathered parts display obscure encrkiites and corals. 
 
 The escarpment on the left side of the valley continues northward into 
 St. Vincent ; and then makes a sharp turn to the westward, running for 
 ten miles in that direction on the right or southern side of the valley of 
 Big Head River; which is supplied from it with several tributaries. On 
 
 sydenham. * ne left side of this stream, and between it and Owen Sound, the limestone 
 spreads out into a high flat-topped hill, situated chiefly in Sydenham, 
 and presenting to the north-east a vertical escarpment. The encrinal por- 
 tion of the limestone is well displayed at the summit, while the character- 
 istic Pentamerus ollongus occurs on both sides, at the base, in the first 
 range of South Sydenham. 
 
 The two streams which flow into the bight of Owen Sound, the Pota- 
 watamie from the south-west, and the Sydenham from the south, fall over 
 precipices of twenty and fifty feet respectively, of the lower part of the 
 same limestone ; the bottom of which is from twenty to thirty feet beneath 
 
CHAP. XII.] NIAGARA FORMATION. 
 
 the cascades. On the thirteenth lot of the second range of Derby, the 
 escarpment which runs between these two falls, presents a height of sixty 
 feet; at the base of which, there occurs a bed abounding in corals. 
 Among the species are JFavosites G-othlandica, Heliolites interstincta, 
 Syringopora reteformis, S. Lyelli, Halysites catenulatus, and Zaphrentis 
 Stokesi; in addition to which, there is found Pentamerus oUongm. 
 
 The rock of the escarpment in this neighborhood abounds in excellent Owen sound, 
 material for the purposes of construction. About two miles south by east 
 from the town of Owen Sound, there are unworked strata of a white or pale 
 grey color ; of which the upper beds are from two to four feet thick, and the 
 lower ones occasionally over twelve feet. The upper bed might be quarried 
 to an almost boundless extent, and would give a very fine and lasting stone. 
 The lower beds are likewise fit for building purposes ; but being at the base 
 of an abrupt precipice, they cannot be so conveniently quarried. Large 
 loose blocks, however, skirt the escarpment, and these would furnish a 
 supply for a great length of time. About a mile and a half up the Sydenham 
 River, there has lately been quarried from the lower beds of the escarpment, 
 some fine stone for the light-house constructed on Griffith's Island. The 
 road south from Owen Sound, on the line between Sydenham and Derby, 
 crosses the base of the limestone, about a mile and a half from the town. 
 After a rather sharp ascent over the lower part of the escarpment, it 
 gradually rises for some distance, and reaches what is considered the 
 summit of the formation, on the sixth lot ; the total thickness being about 
 150 feet. 
 
 Across the whole of the western peninsula, the summit of the Niagara 
 formation is so much covered with drift, that it would be very difficult to 
 trace it with any degree of precision ; or to connect in an intelligible manner 
 the scattered exposures of Niagara strata to the westward, with the rock 
 of the lower escarpment, were it not for the aid afforded by the out- 
 crop of the succeeding rock. Above the east end of the Niagara and 
 Hamilton ridge, the upper limit of the formation probably reaches the 
 lower part of the Chippawa Creek ; and passing by Port Robinson on the 
 Welland Canal, it may cross the road between Hamilton and Port Dover, 
 within two or three miles of the former place. It is not, however, certain Dunda* aati- 
 where it folds over the Dundas anticlinal, there being no exposures clina1 ' 
 whatever upon the axis. The most western appearance of the upper part of 
 the formation, on the south side of the anticlinal, occurs in the vicinity of 
 Ancaster ; the most western on the opposite side, about two miles north of 
 Ancaster, on the third lot of the first range of Flamborough West. It may 
 be inferred from the trend of the formation on each side, and from the general 
 shape of the country, that its summit woujd fold over the axis of the 
 anticlinal, on the line between the townships of Ancaster and Beverley, at 
 about the thirty-fourth lot. 
 
330 GEOLOGY OF CANADA. [CHAP. XII. 
 
 Proceeding northward, the upper escarpment of the Flamborough West 
 section is found to merge into the plain above, and disappear. Black shales 
 and limestones, such as occur in it, are however met with in the sixth range 
 of Nassagaweya, on the Grand Trunk Railway, between three and four miles 
 back from the edge of the lower or main escarpment. It is probable that 
 the whole formation is carried westward, in a narrow spur, on the axis of 
 Rockwood. a small anticlinal. The effects of this are visible in the neighborhood 
 of Rockwood, on the Eramosa, a branch of the Speed, in the fourth 
 lot of the fourth range of Eramosa, where there is a considerable display 
 of the upper part of the formation. On the one side of the undulation, 
 the strata incline nearly north, at an angle of ten degrees ; and on the 
 other, nearly south, at an angle of twelve degrees. The axis of the 
 undulation would thus run about west, which would be nearly at right 
 angles to the general trend of the strata through this part of the country. 
 The undulation thus appears to be a small ridge running down the general 
 slope of the strata, and producing but little effect on the distribution. 
 Exposures of the rock occupy both sides of the stream, in vertical cliffs. 
 The lower part consists of nearly eighty feet of light grey dolomite, in 
 which divisional planes of stratification appear to be absent. Corals and 
 broken encrinites abound in it, associated with other fossils. Among the 
 species are Favosites Groihlandica, Halysites catenulatus, crinoidal col- 
 umns, Khynchonella cuneata. It. camura, Spin/era Niagarensis, with 
 undetermined species of Fenestella, Avicula, Bellerophon, Orthoceras, 
 and Cyrtoceras. On this mass, there rest about twenty feet of buff 
 or drab colored dolomite, holding nodules and patches of chert ; these 
 are succeeded by about five feet of alternating black bitumino-calca- 
 reous shale, and dark brown very bituminous limestone. Corals are 
 observed in some of these limestones, and crystals of galena are of com- 
 mon occurrence, both in the limestone and in the shale. In quarrying 
 the dolomite beneath the shales at this locality, there was found a 
 string or small vein of galena, which was followed for a distance of 
 fifteen or twenty feet in one of the beds, to which the ore appeared to 
 be confined. It was accompanied with smaller strings holding the same 
 mineral, which branched from the main one at irregular distances; but 
 the whole vein was quarried out without any appearance of a farther 
 quantity of the ore. 
 
 Quarries have been opened both in the lower and upper masses of this 
 encrinal magnesian limestone, which has been used in constructing the 
 viaduct over the Eramosa, for the Grand Trunk Railway. That from the 
 upper portion appears to be less porous than the lower, and of a better 
 color for architectural purposes ; but both are of excellent quality, and 
 will probably be found durable. Caverns occur in the base of the lower 
 mass. One of them extends about a hundred feet under the cliff, with a 
 
CHAP. XII.] NIAGARA FORMATION. 331 
 
 breadth of about forty feet. The roof, which is eighteen feet high at the 
 entrance, slopes irregularly downwards, and meets the floor at the distance 
 just mentioned; leaving however a passage at either corner. One of 
 these is said to lead to a large space beyond ; from which other passages 
 proceed. The roof is studded with small stalactitic incrustations. 
 
 From Rockwood westward, the surface of the country falls at about the Gueiph. 
 same rate as the supposed slope of the strata ; so that, on arriving at Gueiph, 
 we should still have near to the surface, the beds of Rockwood, or strata 
 not far removed from them. Exposures occur about five miles south-west- 
 ward from Rockwood, at McFarlane's tavern, on the second lot of the 
 third range, division C, of Gueiph. They consist of about six feet of 
 black bituminous shales and limestones, similar to the highest beds at 
 Rockwood ; succeeded, in ascending order, by the following section, of 
 which the last three feet belong to the Gueiph formation : 
 
 Ft. in. 
 
 Dark brown strongly bituminous limestone, probably magnesian, in 
 
 beds of about one foot each, 4 
 
 Dark brown bituminous limestone, hard, brittle, and nearly compact, 
 
 in several beds ; the color is a shade lighter than the previous beds, 2 
 
 Dark brown bituminous granular magnesian limestone, 6 6 
 
 Pale buff or yellowish- white magnesian limestone ; it holds Holy sites 
 catenulatus, an undetermined Zaphrentis, and imperfect impres- 
 sions of a few undetermined shells, , 3 o 
 
 15 6 
 
 On the north side of the anticlinal, the summit of the Niagara series 
 appears to run from Rockwood, towards the east side of the township 
 of Erin ; between which and Mulmur, it is only by the outcrop of the 
 overlying formation that its western limit can be determined. It is chiefly 
 by the same mark that it can be traced between Mulmur and Owen 
 Sound ; but in this part, the depth of the drift is less, and the upper strata 
 of the series are more frequently exposed. 
 
 The bold escarpment formed by the Niagara limestone in Derby, appears shore of 
 about two miles west of the town of Owen Sound ; and between this posi- Lake Huron - 
 tion and Colpoy's Bay, it sweeps round towards the heights above Cape 
 Commodore, in a line conforming in some degree to the shape of the 
 coast, but presenting a less salient curve. The base of the limestone comes 
 upon Colpoy's Bay, and crosses it, probably, about two miles and a quarter 
 from its bight. Thence it keeps rather close upon the north side of the 
 bay ; while the escarpment gradually rises, according to Bayfield's chart, to 
 a height of 350 feet above the level of Lake Huron in the bluff which 
 faces Hay Island ; to 300 feet in the next bluff north ; and to 200 feet 
 in Cape Paulet. The Clinton formation occupies perhaps a hundred feet 
 at the base of the most southern bluff, and is seen in the second ; but the 
 summit of the formation comes to the level of the water at the extremity 
 
332 GEOLOGY OP CANADA. [CHAP. XIL 
 
 of Cape Paulet. The cliffs along the coast, from this to Cape Chin, are 
 altogether occupied by the Niagara escarpment, and vary in height from 
 130 to 150 feet, being often nearly vertical. The limestone of which they 
 are composed approaches to white in color ; the beds are massive, and 
 a majority of them appear to be magnesian. These cliffs would supply 
 an unlimited amount of a superior material for the purposes of construc- 
 tion. The limestone abounds in corals. Masses which have fallen from the 
 cliff in Isthmus Bay, contain Favosites favosa, Holy sites catenulatus, 
 Syringopora reteformis, and undetermined species of Diphypliyllum and 
 Strophomena, with Pentamerus oblongus. The last named species appears 
 also in place, in beds at the level of the lake. 
 
 Cabot's Head. The summit of the cliff at Cabot's Head, is, by measurement, 324 
 feet above the lake ; 184 feet of this, at the base, are occupied by the 
 Clinton formation; leaving only 140 feet of the Niagara formation in 
 the escarpment. In the transverse section presented by the coast between 
 Cabot's Head and Cape Hurd, higher portions of the series are however 
 met with. The coast intersects the strata obliquely ; but from the posi- 
 tion where the base of the limestone comes to the lake, the distance to 
 the strata of Cape Hurd would be, at right angles to the strike, about 
 twelve or thirteen miles. The slope of the strata, as ascertained by a 
 measurement of two miles and a half, being about thirty-seven feet in a 
 mile, the whole thickness of the limestone, provided the dip is constant, 
 would thus be about 450 feet. It is probable, however, that the slope 
 diminishes towards the main body of the lake : this may considerably reduce 
 the thickness, and some part of the strata may belong to the succeeding 
 formation. The rock is of a pale buff or yellowish white, and weathers'to a 
 drab. It is divided into massive beds, many of them being nine and ten 
 feet thick ; they are cut into rhomboidal forms by two sets of parallel 
 joints, one running N. 85 E. and the other S. 29 E. Some of the thick- 
 est beds appear to be a mass of corals, and most of them present a very 
 rough and irregular exterior. Great blocks of the rock, some of them 
 fifty tons in weight, have fallen from the cliffs, and are scattered along the 
 cape Hnrd. shore. Among the fossils which they contain are Favosites Grothlandica, 
 an undetermined Diphyphyllum, Pentamerus ollongus, with undeter- 
 mined species of Pleurotomaria, Murchisonia, and Orthoceras; while hi 
 the beds in place, near Cape Hurd, there are found, Stromatopora concen- 
 trica and Pentamerus oUongus. 
 
 It seems probable that the coast, from Chiefs Point to Cape Hurd, a 
 distance of fifty miles, runs very nearly on the strike ; but it has still to be 
 ascertained whether the coast may not include some part of the suc- 
 ceeding formation. The rock, all the way, is a whitish sub-crystalline 
 magnesian limestone ; presenting at Tobermorey Harbor, Lyell Island, the 
 mouth of the Riviere aux Sables near Chief's Point, and other places, Pen- 
 
CHAP. XII.] NIAGARA FORMATION. 333 
 
 tamerus oblongus, several undetermined species of Rhynchonella, Murchi- 
 sonia, and Pleurotomaria, P. Huronensis, undetermined species of Gyrto- 
 ceras and Orthoceras, besides 0. undulatum. The Rankin River, falling 
 into the Riviere aux Sables (north), discharges the waters of a chain of 
 lakes, which, with the river first named, occupy a valley running parallel 
 with Lake Huron, for ten miles ; at a distance of two miles from it. A 
 low escarpment occupies the west side of the valley ; but we have not yet 
 been able to ascertain whether this may give clearer evidence of the true 
 summit of the Niagara rocks than is afforded by the coast. 
 
 Strata similar in almost every respect to the Niagara limestone of the 
 peninsula which ends in Cabot's Head and Cape Kurd, run through the 
 whole of the Manitoulin Islands in succession ; of which, with the excep- 
 tion of St. Joseph Island, they compose by far the larger part. These 
 limestones come up to the south front of the Grand Manitoulin, Cockburn, 
 and Drummond Islands ; and form the Huron coast of the northern peninsula 
 of Michigan, as far as Martin Bay. The greatest breadth of the formation 
 is on the Grand Manitoulin, where it measures about eighteen miles. The 
 limestone in this part of its course presents, as in other places, a bold escarp- 
 ment at its base. On the coast, as in the fifty miles from Chief's Point to 
 Cape Hurd, it forms a rugged rocky shore, with shallow water extending 
 out to a considerable distance, in consequence of the smallness of the dip ; 
 rendering the navigation somewhat dangerous. The fossils along this range of 
 islands appear to consist chiefly of corals, and there is little difference be- 
 tween them and those already mentioned on the mainland. On the south 
 side and west end of Drummond Island, there are met with Favosites Q-oth- 
 landiea, F. Hisingeri, Halysites catenulatus, an undetermined Alveolites, 
 Stromatopora concentrica, Zaphrentis Stokesi, Atrypa reticularis. Pen- 
 tamerus ollongus, with undetermined species of Orthis, Pleurotomaria, 
 and Orthoceras. 
 
 Fitzroy or Horse Island, the Isle of Coves, Flower-Pot Island, and 
 several others between the Grand Manitoulin and Cape Hurd, belong to 
 the Niagara formation. In the Isle of Coves, the rocks are worn into 
 various fantastic shapes ; while Flower-Pot Island derives its name from 
 two slender vertical pillars, wider at the top than at the base, which rise 
 up from the water near it ; their shapes being produced by the wearing 
 action of the water, aided probably by the effect of ice. 
 
 The whole of the massive limestones of the Niagara formation are caver- Tecmnseh 
 nous ; worn fissures receive the waters of the surface, and in some places Lake - 
 copious streams burst out at the foot of the escarpment. Tecumseh Lake 
 on the Grand Manitoulin, in the vicinity of Manitouwaning, has an area of 
 about fifty-five square miles, with a height above the level of Lake Huron 
 of 155 feet. While its only visible supply of water is derived from one 
 small stream, this lake furnishes sufficient water for three large brooks,; 
 
334 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XII. 
 
 Springs and 
 caverns. 
 
 which fall from it to the south, the west, and the north. The first of 
 these discharges itself into Lake Huron near Michael Bay on the south 
 side of the island; the second, which leaves Tecumseh Lake at its 
 western extremity, feeds a succession of small lakes, and falls into Beau- 
 fort Bay ; while the third, flowing to the north, supplies two small lakes, 
 and eventually terminates in Shequenandod Bay. Another large lake 
 is said to occupy a portion of the island between Beaufort Bay and Bay- 
 field Sound ; but no examination of it having yet been made, the height 
 and size of this lake cannot be stated. It appears probable that these 
 two lakes may be connected by a subterranean channel, and thus the 
 waters of Tecumseh Lake may result from the drainage of a considerable 
 part of the island. 
 
 On the twelfth lot of the second range of Derby, a spring bursts out 
 from the base of the limestone escarpment, yielding water enough to drive 
 a mill, which is situated within fifty yards of the face of the rock. There 
 is another such spring on the eleventh lot of the first range of the same 
 township, and a water-worn cavern occurs on the twelfth lot of the 
 second range of Mono. Here a branch of the Nottawa River falls for 
 nearly sixty feet, in successive leaps over the edges of massive nearly 
 horizontal beds of a pale buff limestone, which is filled with obscure encri- 
 nites ; and makes a final fall of twelve feet over a less fossiliferous rock. 
 Just below the latter fall, this rock is worn into a cavern, which pre- 
 sents a length of about fifty feet, with a roof ten or twelve feet high at 
 the entrance, gradually sloping down to the floor, in a breadth of twenty- 
 five feet. Stalactites of two feet in length and six inches in diameter, 
 hang from the roof, and corresponding masses rest on the floor. 
 
 Northern 
 basin. 
 
 Absence of 
 Lower Silu- 
 rian. 
 
 THE NIAGARA FORMATION ON LAKE TEMISCAMANGK 
 
 About 150 miles to the north-west of the nearest part of the Niagara 
 formation as described above, rocks, apparently of the same age, are met 
 with on Lake Temiscamang. These properly belong to the great northern 
 fossiliferous trough, connected with Hudson's Bay, of which they are prob- 
 ably an outlier. Being however the only portion of the fossiliferous strata 
 on the northern side of the Laurentian mountains, which has come under 
 our examination, they are for the present noticed in connection with the 
 Niagara series of the southern basin. On Lake Temiscamang, they lie 
 unconformably on the slate conglomerates and sandstones of the Huronian 
 series. The absence of all Lower Silurian strata in place, not only on 
 this lake, but wherever the fossiliferous strata of the northern trough have 
 been observed, corroborates the testimony already furnished by the Pots- 
 dam formation, that during the Lower Silurian period, the Laurentian 
 
CHAP. XII.] NIAGARA FORMATION. 335 
 
 and Huronian rocks on the north were above the sea. It must be re- 
 marked, however, that at Lake Temiscamang, there are found lying 
 on the Niagara limestone, loose angular fragments of dolomite, resembling 
 that of the Birdseye and Black River formation of Lacloche and Lake 
 Nipissing, and holding Strophomena altemata, species of Maclurea like 
 M. magnet, and M. Atlantica, Orthoceras anceps, and 0. proteiforme. 
 The source of these fragments has not yet been ascertained. 
 
 In this northern part of its distribution, the lower portion of the Niagara Base of N* 
 formation is generally arenaceous, and very often a conglomerate; con- J^ ra fonna " 
 taming large pebbles, fragments, and frequently huge boulders of the sub- 
 jacent rocks. On the west side of the lake, about fourteen miles from the 
 head, the base of the deposit consists of vast boulders and fragments of 
 the underlying sandstone, in a calcareo-arenaceous fossiliferous matrix ; 
 some of the enclosed masses being nine feet in diameter. Near by, are seen 
 the Huronian sandstone strata, great cracks and worn fissures in which 
 are filled with the fossiliferous cement. These lower conglomerate beds 
 are in fact a collection of great blocks of sandstone ; which were lying 
 directly upon the strata from which they were derived, when they became 
 enveloped by the sediments of the Niagara formation. It is evident, that 
 the immersion at this period, must have been sudden. 
 
 Higher up in the series, the rock is a buff or light grey limestone, weather- 
 ing white. The beds vary in thickness from a few inches to two or three feet, 
 and are in some parts interstratified with green calcareous shales. Some 
 of the harder beds abound in chert; many of them are very fossiliferous, and 
 the organic remains are frequently replaced by silica. Among the fossils 
 are Favosites G-othlandica, F. favosa. Holy sites catenulatus, Syringopora 
 verticittata, an undetermined Cystiphyllum, Stromatopora concentrica, 
 crinoidal columns in abundance, an undetermined species of Orthis, great 
 numbers of Pentamerus oblongus, Atrypa reticularis, two undetermined 
 species of Pleurotomaria, and Discosorus ( Orthoceras) conoides. 
 
 The thickness of these strata exposed in any one observed section, does 
 not exceed a hundred feet ; but it is probable that the total amount of the 
 Niagara formation is here not less than 300 feet, and may attain 500 feet. 
 The limestones constitute the two large islands north of the Hudson Bay 
 Company's post; the two smaller ones between them, besides the island 
 already mentioned at the entrance of the eastern bay, and a very small one 
 on the west coast ; as well as the promontory which separates the east from 
 the west bay. The strata lie in the form of a shallow trough, resting some- 
 times on the sandstones and sometimes on the slates ; occupying the breadth 
 of the lake, which is from five to six miles, and extending from the south 
 side of the southern great island to some unknown distance northward. 
 
 Ascending Lake Temiscamang, the Huronian slates come in upon the 
 Laurentian gneiss, about three miles below the mouths of the Montreal and 
 
336 GEOLOGY OF CANADA. [CHAP. XII. 
 
 Huronian Metabechuan Rivers, on the west bank ; and about three miles above them 
 on the east. They thence occupy both sides of the lake, to within two and 
 a half miles of the Hudson Bay Company's post. In this distance they 
 may have a direct breadth of about seven miles ; in which they are affected 
 by one or more undulations, and rise into hills of about 400 feet. 
 
 The slates are followed by the sandstones, which cross the lake with 
 a strike N. 70 E., dipping northward at a very small angle. After 
 forming a range of about the same elevation as the slate hills, they reach 
 the Company's post about eighteen miles from the upper end of the lake. 
 Here they are nearly flat, and are overlaid by a hill of gravel, 130 feet in 
 height. On the other side of this, they continue to a distance of about half 
 a mile above the post, and then become interrupted on both sides of the 
 lake, by a mass of syenite ; composed of reddish orthoclase feldspar and 
 white colorless quartz, with a sparing quantity of green hornblende. 
 
 The breadth of this syenite band is pretty nearly three miles, on both 
 sides of the lake. On the west, it is succeeded by the sandstones ; which 
 strike along the coast for a distance of four miles, dipping towards the 
 water at a small angle. These are followed by the slates ; which come from 
 behind them, and continue in a straight line for nine miles, to the western 
 bay at the head of the lake ; forming high perpendicular cliffs for part of 
 the distance, and rounded hills for the remainder. On the east side of the 
 lake, the syenite is succeeded by the slates ; the sandstones come upon 
 these on the south side of the southern large island, and the main land 
 near, dipping N. 20 W. at an angle of three degrees. The sandstones 
 and the slates, with their associated conglomerates, make their appear- 
 ance wherever they are denuded of the overlying limestone ; the basset 
 edge of which thinly covers them, as far as the island at the entrance of 
 the eastern or Moose River Bay. Beyond this, the sandstones are seen 
 gently dipping south, in a projecting point to the east of the island. The 
 slates are met with at the mouth, and at the first, second, and third port- 
 ages of the Riviere des Quinze, or Moose River ; and the conglomerates, hi 
 the bay to the west of the Blanche. For other details of these Huronian 
 rocks of Temiscamang, see page 50. 
 
 THE GUELPH FORMATION. 
 
 In Canada, the Niagara rocks are succeeded by a series of strata, which 
 appear to be wanting in the state of New York. They are largely 
 developed in the neighborhood of Guelph and Gait, and we have desig- 
 nated the series as the Guelph formation. 
 
 The town of Guelph, in the township of the same name, is situated on 
 the river Speed, about eight miles south-west from Rockwood. Here, 
 
CHAP. XII.] GUELPH FORMATION. 337 
 
 in the bed of the stream, under the bridge on the Brock road, there are Gueiph. 
 exposed several feet of dark brown very bituminous dolomite ; succeeded 
 a little way up, on the left bank, by a mass of whitish coralline dolomite, 
 which appears on the side of the road. About half a mile above Gueiph, 
 near the right bank of the Speed, there is a quarry in a whitish sub-crys- 
 talline dolomite, the strata of which are altogether about twelve feet thick. 
 All of the beds contain obscure casts of fossils ; chiefly of corals and bivalve 
 shells. Among them are, Favosites G-othlandica, Halysites catenulatus, a 
 
 new species of Columnaria, Obolus ? Megalomus Canadensis, 
 
 with undetermined species of Pleurotomaria and Orikoceras. The strata 
 
 841 . BKACHIOPOD A. 
 
 341. Pentamerus occidentalis (Hall) ; a, ventral valve ; b, cast of the interior 
 of the umbo of the ventral valve ; c, side view. 
 
 are probably a little higher in the series than those of the same color at 
 the bridge. Similar beds are extensively wrought a little below the town, 
 and yield an excellent building stone. Some of the beds are burned for 
 lime. 
 
 Nearly five miles below Gueiph, where a bridge crosses the Speed, 
 on the town line between the fifth and sixth ranges of the Gore of Puslinch, 
 there is a section, consisting, at the base, of fifteen feet of black hard 
 compact bituminous dolomite, without observed fossils ; followed by seven 
 feet of brown bituminous strata. On these, rest seven feet of buff or pale 
 drab dolomites, holding obscure fossils. These exposures on the Speed are 
 nearly in the strike of the strata. The light colored dolomites, which are 
 here seen to rest upon dark colored bituminous strata, are regarded as the 
 base of the Gueiph formation. See farther, the section at McFarlane's 
 tavern, given on page 331. 
 
 The fall from the base of the formation, at Gueiph, on the Speed, to the 
 bed of the Grand River, at Breslau, as deduced from the levels on the 
 
 w 
 
338 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XII. 
 
 Breslau. 
 
 Dolomites. 
 
 Dumfries. 
 
 Grand Trunk Railway, is eighty-two feet. The distance across the strike 
 of the measures, between Guelph and Breslau, is about nine miles ; so that 
 if the dip of the strata be taken at twenty feet in a mile, which is perhaps 
 near the truth, the base of the formation would be one hundred feet beneath 
 the bed of the Grand River. The rocks of the Guelph formation are not 
 seen at Breslau ; but at points both to the north and to the south, which 
 would include this place in their strike, strata are met with at a level of 
 about sixty feet above the Grand River. This would give for the Guelph 
 dolomites, about 160 feet; which we may assume as the approximate thick, 
 ness of the formation. 
 
 The strata of this formation appear, so far as examined, to be magnesian 
 limestone, having the composition of true dolomites, and are frequently 
 made up of brilliant crystalline strongly coherent grains. The rock is very 
 
 342. LAMELLIBRANCHIATA. 
 
 342. Megalomus Canadensis (Hall) ; cast of the interior. 
 
 often porous, and has small drusy cavities ; besides which, are those form- 
 ing the moulds of fossils. In many cases, the shell appears to have been 
 simply enveloped in the rock ; and having been afterwards removed by 
 solution, it has left a corresponding cavity. At other times, the interior of 
 the shell was also filled with the dolomite, so that the mould corresponds 
 only to the thickness of the shell ; the markings of both the interior and 
 exterior of which are thus preserved. More rarely, the cavities have 
 been subsequently filled up by calcareous matter ; so that the substance 
 of the shell appears to have been either replaced or preserved. 
 
 The most southern exposure of the summit of the formation, on the Grand 
 River, occurs just above Middleton bridge, on the twenty-first or twenty- 
 second lot of the sixth range of Dumfries. The rock is a light grey dolo- 
 mite, weathering to a pale drab : it holds fossils of the genera Zaplirentis 
 Murchisonia, and Pleurotomaria, but they are too obscure to be specifically 
 determined. Similar beds, with others of a pale buff color, continue up to 
 
CHAP. XII.] 
 
 GUELPH FORMATION. 
 
 839 
 
 the north end of the fourteenth lot of the sixth range of Dumfries, with 
 a very gentle dip to the south-west ; the distance across the measures being 
 probably two miles. In one of the buff colored beds on the lot just named, 
 in addition to the previous genera, there occurs Megalomus Canadensis;> 
 being the largest bivalve shell of the formation, and its most characteristic 
 fossil. The rocks of the Guelph formation are again met with, farther up 
 the Grand River, in the vicinity of Gait. 
 
 The highest strata here appear to be the same as those above Mid- 
 dleton bridge. The exposures are chiefly on the right bank of the river, 
 but occasionally on both banks; and they extend for some distance, both 
 
 343. Murchisonia bivittata (Hall). 
 344. If. macrospira (Hall). 
 
 345. Murchisonia Soydii (Hall). 
 346. Subulites ventricosus (Hall). 
 
 below the town and above it, where quarries are wrought in the rock. 
 The greatest vertical section in any of these is thirty-four feet ; but expo- Gait, 
 sures of both higher and lower strata would make the whole thickness 
 upwards of sixty feet. At the top of the formation, in this neighborhood, 
 there are about eighteen feet of hard thin bedded bluish dolomite, beneath 
 which are thirteen feet of pale buff or white dolomite; succeeded by- 
 twenty feet of yellowish-white and greyish-white crystalline thick bedded 
 dolomite, in overlapping lenticular masses. The whole mass holds fossils ; 
 but these, in the immediate vicinity of Gait, are most abundant in the 
 twenty feet of pale buff thin-bedded dolomite in the middle of the section. 
 The species met with are "Favosites G-othlandica, Pentamerus occiden- 
 talis, Obolus f Megalomus Canadensis, Pleurotomaria $ 
 
340 GEOLOGY OF CANADA. [CHAP. XIL 
 
 P. G-altensis, P. Mora, P. solaroides, Murchisonia Boydii, M. Logani, 
 M. longispira, M. Uvittata, M. turritiformis, M. Tullia, Cyclonema 
 G-altensis, 0. Thy she, 0. Psyche, Bellerophon angustata, Orthoceras Dar- 
 t wini, Cyrtoceras arcticameratum, C. Jonesi, Phragmoceras Hector, and 
 Calymene Blumenbachii. 
 
 The exposures continue all the way to Preston, which is still higher up 
 on the river. Here the banks exhibit a section of from fifteen to twenty 
 feet of coralline magnesian limestone; probably equivalent to the thin 
 bedded pale buff dolomite of Gait, but not so fossiliferous. Exposures con- 
 
 Hespeier. tinue up the Speed ; and at Hespeler, strata occur that are lower in the 
 series than those at Gait ; their stratigraphical place being probably near 
 the middle of the formation. A cutting at Hespeler, on the Great Western 
 Railway, exhibits fifteen or twenty feet of pale greyish-white strata ; which 
 are not so massive as some of those at Gait, but more fossiliferous. The 
 species observed are Favosites G-othlandica, F. polymorpha, Columnaria 
 G-altensis, Halysites catenulatus, Diphyphyllum irregulare, Amplexus 
 
 laxatus, Obolus ? undetermined species of Rhynchonella and 
 
 Athyris, Megalomus Canadensis, Murchisonia Logani, M. Uvittata, an 
 undetermined Pleurotomaria, Cyclonema depressa, O. Thysle, Orthoceras 
 Darwini, and Cyrtoceras arcticameratum. Both at Gait and Hespeler, 
 quarries are worked in these magnesian limestones ; which yield excellent 
 building stones, easily dressed and probably durable. Some of the beds 
 are burned for lime, which is often rather dark in color, but makes a strong 
 mortar. 
 
 Eiora. About fourteen miles north from Breslau, in Pilkington and Nichol, on 
 the banks of the Irvine and Grand Rivers, near their junction, at Elora, 
 perpendicular cliffs of these dolomites occur; varying in height from 
 seventy-five to eighty or eighty-two feet. The upper portion of these strata 
 is probably near the top of the Guelph formation. The beds in descending 
 order are as follows : 
 
 Ft. in. 
 
 1. Light drab or reddish compact magnesian limestone, in beds of from 
 
 three to six inches, with small cavities (probably once holding 
 fossils), and cracks lined with calcspar. The fossils are Hal- 
 ysites catenulatus, Obolus ? Pentamerus occidentalis, Mega- 
 lomus Canadensis, and Murchisonia Logani ; with several undeter- 
 mined species of Pleurotomaria and Orthoceras, 12 
 
 2. Buff colored coralline magnesian limestone, with a stratum of about 
 
 three feet, near the middle, filled with Megalomus Canadensis; the 
 corals observed are Favosites Gothlandica, F. polymorphaj and 
 Stromatopora concentrica, 14 
 
 3. Pale buff or yellowish-white compact magnesian limestone with a 
 
 conchoidal fracture, in massive beds holding fossils. Among 
 these are Favosites Gothlandica, Pentamerus occidentalis, with 
 undetermined species of Rhynchonella, Murchisonia, &n&0rthoceras, 56 
 
 82 
 
CHAP. XII.] 
 
 GUELPH FORMATION. 
 
 341 
 
 At Fergus, which is on the Grand River, at such a distance above the Fergus, 
 mouth of the Irvine as would give three miles across the measures, a 
 section occurs near Mr. Webster's mill, displaying about twenty feet of 
 strata, which would underlie the preceding. About sixteen feet of these 
 
 347. GASTEROPODA. 
 
 347. Pleurotomaria solaroides (Hall) ; a, side view ; 6, view of the under side. 
 
 are a pale buff magnesian limestone, with casts and impressions of fossils ; 
 among which are Favosites G-othlandica, Megalomm Canadensis, and 
 MureUsonia Logani. The remaining four feet consist of a grey hard 
 magnesian limestone ; which rests upon a mass of the same color, but some- 
 
842 GEOLOGY OF CANADA. [CHAP. XII, 
 
 what closer grained, forming the bed of the stream. About a mile farther 
 up the stream, on the land of Mr. James Webster, there are beds of pale 
 yellowish-grey magnesian limestone, weathering to a light buff. These 
 would be still somewhat lower than the beds at Fergus ; and contain Favo- 
 sites Grothlandica, F. polymorpha, Pentamerus occidentals, Megalomus 
 Canadensis, MurcTiisonia Logani, M. longispira, and Pleurotomaria 
 Huronensis. Some of the Fergus beds yield good lime : they range from 
 two inches to two feet in thickness, but are for the greater part thin and 
 irregular, and, although some of them are used for rough buildings, the 
 stone for facing is brought to Fergus from Gruelph. 
 
 Exposures of these dolomites are again met with, on the Rocky 
 Saugeen River, upwards of forty miles N. N. W. from Fergus. One of 
 them occurs about three miles beyond Durham, where the Garafraxa and 
 Owen Sound road crosses the river. Here the rock has been quarried 
 for building stone, and for burning into lime. The lower part is a light 
 greenish-grey sub-crystalline magnesian limestone, divided into beds of 
 from eight to ten inches thick, with very obscure fossils ; while the upper 
 part is a greyish-white coralline mass, seven feet thick, in several beds, 
 of which the thickest is three feet. Among its fossils are Favosites 
 
 Crothlandica, Amplexus laxatus, Obolus ? and Megalomus 
 
 Oanadensis. Another of these exposures is at the junction of the Rocky 
 Saugeen with the main stream, in the rear of the sixty-second lot of the 
 Bentinck. third range of Bentinck ; where about twenty -five feet of the rock are 
 seen on the right bank. The upper twelve feet consist of a rough irreg- 
 ular bed of greyish-white dolomite ; underlaid by a buff colored compact 
 stratum, divided into layers of from three to four inches. The fossils 
 found here are Favosites Grothlandica, Pentamerus occidentalis, Obolus 
 
 ? Megalomus Canadensis, with undetermined species of 
 
 Murchisonia and Pleurotomaria. 
 
 The exposures which have been mentioned between Puslinch and Ben- 
 tinck, belong to the upper part of the formation, and indicate the strike of 
 its summit northward, as far as the Rocky Saugeen. In this region, with 
 the exception of the space occupied by the westward spur of the Niagara 
 series on the Rockwood anticlinal, the Guelph formation presents a breadth 
 of about twenty-five miles, opposite to Puslinch ; which gradually increases 
 to thirty-five miles, opposite to Bentinck. This great breadth is probably 
 due in part to the fact that the country rises with the general slope of the 
 strata, to the edge of the eastern escarpment, though at a somewhat smaller 
 angle ; and in part also to a series of north and south undulations, which 
 appear to exist in this region. 
 
 Between Rockwood and Erin, the base of the formation forms a small 
 sinus up the Speed, to Everton ; while to the southward, it forms another 
 sinus running down the same stream, to Eden. These two turns in the 
 
CHAP. XII.] 
 
 GUELPH FORMATION. 
 
 343 
 
 distribution of the rock, are occasioned by an undulation transverse to Anticiinais. 
 the Rockwood anticlinal. Its axis, with a bearing a little east of north, 
 would pass under Eden, Rockwood, and Everton, and thence to Orange- 
 ville. The sinus which terminates there may owe its origin to the same 
 anticlinal ; and it is probable that some of the other deep southward in- 
 
 348-351. GASTEROPODA. 
 
 3S.Pleurotomaria Elora (Billings). 
 
 349. P. Galtensis (Billings). 
 
 350. Cyclonema sulcata (Hall) ; a and b, two views of the same specimen. 
 | 351. Holopea Guelphensis (Billings). 
 
 dentations in the outcrop of the formations between Orangeville and Owen 
 Sound, may be due to undulations parallel to this one. The strata over 
 this region are so nearly horizontal, that the dips can scarcely be appealed 
 to as proofs of undulations in the strata ; yet we are inclined to believe 
 that the indentations in the outcrops, on the Noisy and Beaver Rivers, 
 and on Owen Sound, are connected with anticlinals. These north and 
 south undulations appear to be related to those already mentioned as 
 affecting the outcrop of the Trenton group, between Kingston and Lake 
 Simcoe. The bearings of the undulations in the latter region, seem to 
 accord with those of the Laurentian folds, as far as these have been 
 ascertained ; and the undulations of the Silurian strata may be connected 
 with the inequalities of the surface of the Laurentian rocks, upon which 
 they repose. The thick masses of Silurian sediment accumulated in the 
 ancient Laurentian valleys, would, by their contraction during solidification, 
 undergo a vertical subsidence ; which would cause them to dip away 
 from the thinner deposits that covered the Laurentian hills. 
 
 From Bentinck, northward, the strike of the summit of the formation 
 appears to continue in the same bearing as between Puslinch and Ben- 
 tinck, for about twenty-five miles, to the RiviSre aux Sables (north). The 
 
344 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XII. 
 
 chiefs Point 
 toCapeHurd. 
 
 base, however, folding successively over the supposed anticlinals of the 
 Beaver River and Owen Sound, the breadth of the formation becomes 
 reduced, between the latter place and the Riviere aux Sables (north), to 
 ten miles; which is about the same as that which it appears to have 
 between Guelph and Breslau. 
 
 It has already been stated that the strata seen near the mouth of the 
 Ri v j re aux g a bl e s, at Chief's Point, probably strike along the coast, 
 by Lyell Island, to Cape Hurd ; and belong in part to the Niagara forma- 
 tion, whose characteristic fossils are met with in several localities along the 
 shore. These strata, however, have for the most part the lithological 
 
 852. GASTEROPODA. 
 
 B52.Bellerophon angustata (Hall) ; a, dorsal, and b, side view. 
 
 characters of the Guelph formation, and some of their undescribed species 
 of Murchisonia have a strong resemblance to others found in this series. 
 The Pleurotomaria Huronensis, which belongs to the Guelph rocks, occurs 
 on Lyell Island associated with Pentamerus ollongus, and other charac- 
 teristic Niagara species ; so that it is not impossible that some of the strata 
 along this coast may constitute a passage between the Niagara and Guelph 
 formation. 
 
 The Guelph formation appears to be absent from the state of New York, 
 and in Canada it probably has the form of a great lenticular mass, the 
 limit of which between Niagara and Guelph is uncertain; though it 
 appears to extend beyond Ancaster. In the other direction, it seems 
 to thin out in Lake Huron, before reaching the northern peninsula of 
 Michigan. 
 
CHAP. XIII.] GEOLOGY OF CANADA. 345 
 
 CHAPTER XIII. 
 
 THE ONONDAGA FORMATION AND THE LOWER HELDERBERG GROUP. 
 
 UPPER SILURIAN SERIES. ONONDAGA FORMATION; CONTAINS SALT AND GYPSUM. IMPRESSIONS 
 OF CRYSTALS; EP8OMITES. DISTRIBUTION OF THE FORMATION IN CANADA; GYPSUM OF 
 THE GRAND RIVER; STRUCTURE AND ARRANGEMENT OF THE GYPSUM BEDS. LOWER 
 HELDERBERG GROUP; ITS DIVISIONS. UPPER PORTIONS WANTING IN WESTERN CANADA; 
 WATER-LIME GROUP; EURYPTERUS BEDS. OUTLIERS NEAR MONTREAL; MAGNESIAN CON- 
 GLOMERATES; ST. HELEN'S ISLAND. EVIDENCES OF DENUDATION DURING THE PALAEOZOIC 
 PERIOD. 
 
 The Middle Silurian formations, which have been described in the last salt and 
 chapter, are followed by a series of rocks, noted, in some parts of their syP 80111 - 
 distribution, for their deposits of gypsum and for salt springs. The latter 
 are extensively wrought in Onondaga county, New York, and the name of 
 the Onondaga Salt group has hence been given, by the state geologists, to 
 this series of rocks ; for which we preserve the name of the Onondaga 
 formation. Succeeding these, is a group of strata, which, from their posi- 
 tion in the Helderberg hills, in New York, have received the name of the 
 Lower Helderberg group, and which are regarded as forming the summit 
 of the Silurian system. These two groups, whose position in Canada we upper suu- 
 propose to describe in the present chapter, constitute the Upper Silurian rian ' 
 division. 
 
 In the state of New York, the Guelph formation is wanting, and the Onondaga 
 Onondaga series rests directly upon the Niagara Limestones. It is there formation - 
 described as consisting, at the base, of red shales, occasionally marked by 
 green bands and spots. This first division is overlaid by greenish shales 
 and marls, with occasional bands of red shale and of shaly limestone. These 
 strata abound in small veins and nodules of gypsum, and readily disinte- 
 grate when exposed to the air. The third division, which is the true gyp- 
 sum-bearing portion, consists of grey or drab-colored magnesian limestones, 
 with greyish and greenish shales ; including two ranges of interstratified 
 masses of gypsum, sometimes with native sulphur. With these is a band impressions 
 of shaly limestone, marked by hopper-shaped cavities, which are supposed of crystajs - 
 to have contained crystals of common salt. Two bands of what was called 
 by Eaton, vermicular limerock, also occur in this division : it is described 
 as a solid drab-colored limestone, with vesicular cavities, of varying sizes, 
 
346 GEOLOGY OF CANADA. [CHAP. XIII. 
 
 up to half an inch in diameter. The fourth or upper division of the Onon- 
 daga formation, is a limestone, with columnar markings on the surface of 
 the beds ; which were supposed by Mr. Yanuxem to be impressions formed 
 bj crystals of sulphate of magnesia, or Epsom salt, during the deposition 
 of the sediments ; and were in consequence called by him epsomites. (Geol- 
 Epsomites. ogy of New York, Vol. Ill, p. 108.) These peculiar impressions have 
 already been described hi the Marmora lithographic stone of the Trenton 
 group (p. 182), and in the Niagara formation (p. 323); they are also 
 met with in the Corniferous limestone formation. Their origin may be 
 conceived if we suppose large prismatic crystals of sulphate of magnesia 
 to be implanted vertically, and near to each other, hi a soft bed of sediment, 
 ancl to be afterwards removed by solution, leaving moulds which are filled 
 by the next deposited layer ; a thin film of black argillaceous mud, which 
 generally divides the beds, covering also the moulds of the crystals. In 
 some of the cherty portions of the Corniferous, we find these columnar 
 markings between layers of chert and limestone. In the dolomites of the 
 Onondaga formation, in Canada, there are also beds containing great num- 
 bers of thin lenticular crystals of translucent calcspar, whose greater diam- 
 eters lie for the most part in the plane of deposit. These, being dissolved 
 out from the weathered surface of the dolomite, give to its surface a 
 curiously fissured appearance, which was noticed by Vanuxem; who did 
 not however explain its origin. The cavities in the vermicular limerock, 
 which is a similar dolomite, are due in like manner to the solubility of car- 
 bonate of lime ; the cavities, in fresh fractures of the rock, being filled with 
 this mineral in a pulverulent form. Mr. Vanuxem also noticed two other 
 classes of markings on the beds of this formation ; the one being cuneiform 
 figures, and the other lines branching off from a stem, at an angle of 
 about thirty-five degrees : these he also ascribed to crystallization. Similar 
 traces are found impressed on some of the thin bedded dolomites of the 
 gypsiferous rocks, on the Grand River ; and it may be remarked that all of 
 these, not less than the gypsum, and the hopper-shaped moulds of salt 
 crystals found in New York, show that these rocks were deposited from 
 waters concentrated by evaporation. This condition may account for the 
 absence of organic remains from the Onondaga formation. 
 
 the form f "^ n ^ eastern part of New York, the Onondaga formation, like the 
 tk>n. Middle Silurian series, is but little developed. Commencing as a thin 
 
 band, at Shannon, in Montgomery county, it attains its greatest thickness, 
 which is about 700 feet, in Wayne county. Running parallel with the 
 shore of Lake Ontario, it diminishes considerably to the westward, until it 
 crosses the Niagara River, and enters Canada, with a thickness which is 
 estimated at between 200 and 300 feet. The salt-bearing strata of this 
 formation, do not appear to extend to the westward of central New York. 
 
CHAP. XIII.] ONONDAGA FORMATION. 347 
 
 Commencing at the Niagara River, the upper beds of the series are seen Distribution, 
 near the village of Waterloo ; and are traceable to the westward, from the 
 eighth lot of the seventh, to the twenty-third lot of the second range of 
 Bertie. Sweeping round towards the shore of Lake Erie, behind Cape 
 Abino, through the influence of an undulation, they are again traceable, 
 from the fifteenth lot of the third range of Humberstone to the Welland 
 Canal, on the twenty-sixth lot of the second range of the same township. 
 Between this outcrop and the Chippawa, the whole of the country is cov- 
 ered by clay. It is probable, however, that the lowest beds occur some- 
 where near to Chippawa village ; as the clay for a considerable extent in that 
 neighborhood, has a red color, such as might be expected from the disin- 
 tegration of the red shales, which occur at the base of the formation in 
 New York. The same red color also prevails on the Welland Canal, hi 
 the vicinity of Port Robinson ; though no red shales have yet been seen in 
 place, either there or for upwards of a hundred miles beyond. 
 
 The exposures of the Onondaga formation in Canada, so far as yet 
 examined, appear to belong chiefly to the upper portions, from the sum- 
 mit to a little below the gypsum-bearing beds. These portions consist of 
 dolomites and soft crumbling shales, which are greenish, and sometimes 
 dark brown or bluish in color, and are often dolomitic. The dolomites are 
 mostly of a yellowish-brown or drab color, and are in beds which seldom 
 exceed a foot in thickness. They often exhibit the vesicular or the lenticular 
 cavities just described. Some beds of a bluish dolomite are also met water ce- 
 with ; and many of the strata, both above and below the gypsum, contain ment> 
 such a proportion of clay as makes them fit for hydraulic cement. 
 
 The beds of gypsum are never continuous for long distances, but appear Gypsum, 
 as detached lenticular or dome-like masses ; the strata above them being 
 arched over and often broken, while those below constitute an even undis- 
 .turbed floor. The gypsum is interstratified with the dolomite, and often 
 separated by beds of it. The layers of gypsum may sometimes extend 
 for a quarter of a mile ; but they have always been found, on working, to be 
 lenticular in form, and to gradually thin out, until the strata above and 
 below the masses, come in contact. This peculiar structure gives rise to 
 mounds on the surface ; which are regarded by the inhabitants, as indica- 
 tive of the presence of gypsum beneath. 
 
 Between the Niagara and the Grand River, the workable masses of 
 gypsum, if any are present, are concealed by the drift ; but on the Grand 
 River, they are seen, twelve or fourteen miles above its mouth, in the third 
 range of North Cayuga, and thence are traced to Paris. Their strike cayuga. 
 appears to coincide with the general course of the river. A large 
 deposit of gypsum, which has been extensively wrought, occurs on the 
 land of Mr. Brown, about three miles below the village of Cayuga, on the 
 left bank of the Grand River. It is supposed to extend over at least sixty 
 
348 GEOLOGY OP CANADA. [CHAP. XIII. 
 
 acres, and is generally covered only by drift. In some parts, however, 
 portions of thin dolomitic beds are found, resting upon the gypsum; which 
 is five feet in thickness, and very pure. The lower portion includes some 
 thin interrupted layers of dolomite, which are vesicular when weathered. 
 In a well sunk upon this bed, near the proprietor's house, there were found, 
 beneath the gypsum, about twenty feet of dolomite, containing small por- 
 tions of gypsum ; beneath which, at the bottom of the well, were three or 
 four feet of unmixed dolomite, fit for water cement. The dip of the bed, 
 which is about S. 20 W. < 2, would carry it under the level of the 
 river ; and the position of the summit of the formation, which is seen at a 
 little distance on the other side of the river, would apparently give a thick- 
 ness of about ninety or one hundred feet above the gypsum. This upper 
 portion of the formation, as seen in Jones's tract, consists of a dark ferrugi- 
 nous shale, with nodules of yellowish-grey chert ; interstratified with green- 
 ish marl, containing harder layers. The thickness of these beds is about 
 thirteen feet, and they are surmounted by about five feet of yellowish shale 
 and tufaceous dolomite, with vesicular bands. 
 
 About five miles above Brown's plaster bed, gypsum occurs in Indiana, 
 
 on the left bank of the river ; and about four miles farther, near to York, 
 
 oneida. on both sides. The following is a descending section of the strata observed 
 
 in the latter vicinity, near Mount Healy, at the plaster bed of Mr. Taylor : 
 
 Ft. in. 
 
 Drab-colored dolomite, with some blue layers, in beds of about five inches, ... 23 
 
 Greenish shales, 3 
 
 Drab-colored vesicular dolomite, yielding good lime, 1 6 
 
 Blue thin bedded hard limestone, said to be fit for hydraulic purposes, ....... 1 7 
 
 Pure white gypsum, with bluish bands, 3 6 
 
 Blue schistose argillaceous dolomite, some of it fit for water cement, 5 
 
 Grey dolomite, with joints at right angles to the beds, which are thicker at 
 
 the bottom than at the top, and separated by partings of shale, 6 
 
 22 10 
 
 In the bed of the river at York is a stratum of solid limestone, which 
 would underlie the above section: it holds small quantities of galena. 
 The dip of the measures in this part, judging by the strike of the summit 
 of the formation, is, like that of Cayuga, about S. 20 W. ; but it is not 
 easy to determine the slope. If we assume the thickness of the overlying 
 portion to be the same as before, the distance of the summit, which is 
 nearly five miles, would give a slope of about twenty feet in a mile. 
 
 Three adits have been opened in this plaster bed at Mount Healy, and 
 afford good opportunities of studying the gypsiferous rocks. One of the 
 most remarkable characteristics is the irregular nature of the bedding. 
 Some of the layers of dolomite immediately below .the gypsum, to the east 
 of it, are seen to augment and to then diminish considerably in thickness in 
 
CHAP. XIII.] ONONDAGA FORMATION. 349 
 
 the distance of a few feet ; giving thus, at first sight, the appearance of Mount 
 undulations, while the beds beneath are completely horizontal. In the Healy> 
 central opening, a layer of dolomite, not seen in the others, is interstrati- 
 fied with the gypsum ; and in one of the adits, the gypsum bed is observed 
 to thin out, the strata from above bending downwards, and conforming to 
 it. It results from these irregularities in the beds, that sections in different 
 portions are by no means concordant. In one part, three or four feet of 
 dolomite overlie the gypsum bed ; the upper part being vesicular, and a 
 portion of it filled with crystalline carbonate of lime. Here, immediately 
 resting upon the gypsum, is a reddish ferruginous layer, followed by two 
 inches of green shale. In another opening, this thin layer of shale is 
 succeeded by a few inches of plastic calcareous clay ; to which succeed 
 very thin bedded vesicular dolomites, whose surfaces are marked with 
 the branching lines already described. Farther on, this layer of shale 
 becomes a foot or two in thickness ; and it includes portions of travertine, 
 which is sometimes compact like alabaster, and forms considerable masses 
 in the fissures of the overlying beds. At about three feet above the prin- 
 cipal mass of gypsum, a second interrupted layer is met with, which is 
 very pure. It is generally only a few inches thick ; but it swells to a 
 foot or two in some places, and in others is wanting. 
 
 At Aikman's plaster bed, a mile and a half above York, on the left bank York, 
 of the Grand River, the mass of gypsum is seven feet in thickness, but is 
 divided into six layers by interstratified bands of dolomite, of from two to 
 six inches ; the same band varying in short distances. The upper portion 
 of gypsum is two feet thick, and is pure and white ; the lower portions are 
 mixed with dolomite and are less pure. Immediately above the gypsum 
 is a sandy ferruginous layer of from two to six inches ; then, after some 
 layers of dolomite, occur eighteen inches of greenish shale ; followed by four 
 feet of yellowish vesicular dolomite. For the next two miles, as far as Seneca. 
 Seneca, the gypsum appears occasionally, in thick rounded masses, envel- 
 oped and underlaid by green shales ; the lower portions of which some- 
 times include small interrupted layers of the mineral. 
 
 About two and a quarter miles across the measures, in a direction nearly 
 S. "VV. from Seneca, there is an exposure at McKenzie's mills, of about 
 twelve feet of beds belonging to this formation, which may be fifty or sixty 
 feet higher in the series than the gypsum. The section consists of drab- 
 colored dolomites, sometimes vesicular, interstratified with hard blue slaty 
 layers, and with green shales ; which sometimes include thin dark colored 
 laminae. The same strata are met with again at Barton Creek, about a 
 mile south from McKenzie's mills. Some of the beds at both places yield 
 good lime, but others are unfit for burning. 
 
 About twenty miles above Seneca, gypsum is met with in Brantford, on Brantford. 
 the seventeenth lot of the third range, the sixteenth lot of the second, and 
 
350 GEOLOGY OF' CANADA. [CHAP. XIII. 
 
 the fifteenth lot of the first range. In the first of these lots, it occurs on 
 the right, and in the other two, on the left bank of the river. In the last 
 of these, the gypsum has been mined by Mr. Tennant, and forms a bed of 
 Paris, three feet, underlaid by and imbedded in green shale. Above this, on the 
 river, gypsum is quarried in many places in the vicinity of Paris. At Mr. 
 Coy's,, about a mile and a quarter below this town, on the left bank of the 
 river, there appear, as at Mount Healy, to be two ranges of gypsum ; the 
 upper of five, and the lower of four feet. These are separated by a layer of 
 four feet of shale, which is also found both above and below them. A short 
 distance above this, on the same side of the river, is a hill, into which an 
 adit has been driven upwards of 250 yards, at right angles to the river ; 
 along a gypsiferous bed, different in some respects from those already de- 
 scribed. The underlying rock is green shale, upon which rests a layer of 
 three feet of green shale, occasionally mingled with dolomite, and enclos- 
 ing rounded masses of gypsum, from a few inches to four feet in diameter ; 
 around which the enclosing strata are always bent conformably. A thin 
 layer of dolomite covers this bed ; but at the end of the adit, it is wanting, 
 and a conical mass of the gypsum is found protruding into the overlying 
 drift clay, which rises to the height of eighty feet above the river. At 
 Paris, on the east bank of the river, between the Great Western Railway 
 viaduct and Mr. Wright's plaster bed, the strata of this part of the forma- 
 tion are very well exposed. Here we have eight or ten feet of tender, 
 brittle greenish argillaceous dolomitic rock, often red-weathering, and 
 passing into a shale. This is overlaid by three feet of dove-colored dolo- 
 mite, vesicular below, with thin eroded cellular beds; followed by a bed 
 of one foot, compact above, but cellular below, and succeeded by a foot or 
 more of vesicular beds. These are overlaid by about a foot of conglomerate, 
 apparently of vesicular dolomite, with fragments of green shale ; the upper 
 part very ferruginous, and decomposing. The whole is overlaid by green 
 shales, more tender and crumbling than those below. These strata are 
 slightly undulating ; and as they are concealed near the gypsum quarry, it 
 is not easy to give the exact horizon of this. The upper part of the gyp- 
 sum bed is intercalated with much dolomite, and for two feet seems made 
 up of alternating lenticular masses of gypsum and dolomite, the latter pre- 
 vailing at the top, and succeeded by thin bedded cellular dolomites ; one 
 portion of which seems to have been broken and re'-cemented. Examples 
 of this are seen on the other side of the river just below the viaduct ; 
 where the green shales are overlaid by masses of similar dolomite, often 
 stained red, and having apparently been broken^ and re-cemented into a 
 kind of breccia. 
 
 Exposures of strata belonging to the Onondaga formation, are met with 
 at several places on the Grand River, for a distance of about fifteen miles ; 
 from Doon, six miles above Gait, to about two miles below Glen Morris. 
 
CHAP. XIII.] ONONflAGA FORMATION. 
 
 Between Gait and Preston, on the west side of the river, on a lot adjoin- 
 ing one where the Guelph formation is exposed, there are seen about five 
 feet of brownish shale, interstratified with thin beds of dolomite ; in one 
 of which is found an obscure bivalve shell. Similar strata are said to occur 
 two miles below Glen Morris ; beyond which the rocks of the formation are 
 concealed beneath a great thickness of drift. In the townships of Mary- 
 borough and Peel, on the Canestoga, a branch of the Grand River, how- 
 ever, abundant fragments of the gypsiferous rocks mark the proximity of 
 the outcrop of this formation. 
 
 In the township of Normanby, sections, apparently belonging to the Normanby. 
 lower portions of the formation, occur at Ayton and at Neustadt-; both on 
 the banks of a tributary of the Saugeen, known as the South Saugeen 
 River. Near the latter village, are seen about ten feet of thin bedded 
 dolomites, some of which are water-lime. To these succeed six feet of 
 greenish crumbling shales, overlaid by rusty brown, dark red, and green 
 shales ; which probably have a thickness of forty feet. At Ayton, there 
 are seen forty-three feet of bluish and drab-colored dolomitic shales, with 
 some harder bands. At Walkerton, in the township of Brant, on the right Brant, 
 bank of the Saugeen, there occur, at the base of a section, two feet of 
 greenish dolomite ; followed by forty-four feet of a bluish argillaceous rock, 
 with red bands. It contains numerous vesicular cavities, stained red 
 within, and disintegrates on exposure to the weather. This is overlaid 
 by eight feet of drab dolomite ; while near by, and apparently overlying 
 this, are thirty or forty feet of drab-colored dolomites. The lower part, 
 compact, and apparently fit for/ lithography, is interstratified with bands of 
 dark shale. The upper portion is whiter, softer, and filled with small 
 lenticular crystals of calcite ; it also holds, in some parts, geodes of the 
 same mineral. Farther down on the Saugeen, ^at the commencement of a 
 great bend called the Ox-bow, occur vesicular drab colored dolomites, over- 
 laid by a bed of black shale ; which is followed by thin bedded buff colored 
 bituminous dolomites, with lenticular crystals of calcite. In less than half s 
 a mile across the measures, to the south-west, we come upon the strike of 
 a rock belonging to a higher formation ; so that the strata at the Ox-bow 
 probably belong to the higher portion of the Onondaga series ; while the 
 red and green shales in the previous section, seem to indicate the base of 
 the formation. 
 
 Exposures of thin bedded dolomites are met with, at several points, Eidereiie. 
 nearly to the mouth of the Saugeen. About a mile below the village of 
 Paisley, in the township of Elderslie, strata of this kind are seen, contain- 
 ing small lenticular crystals of calcite. Tfte lithological characters of many 
 beds at the summit of this formation, are, however, so much like those of 
 the overlying Water-lime group, that it is not easy to draw a line of 
 division between them. 
 
352 GEOLOGY OF CANADA. [CHAP. XIIL 
 
 To the northward of the Saugeen, no further exposures of the Onondaga 
 formation are known in Canada. Gypsum has been said to occur in the 
 largest of the Duck Islands, in front of the Great Manitoulin ; but the 
 island proves, on examination, to be covered with drift. The formation is, 
 however, apparently continued, through Lake Huron, to the straits of Mack- 
 inaw ; where it forms the island of that name, and the points of the main- 
 land on either side. 
 
 Acid springs. No brine springs have as yet been observed in this formation in Canada, 
 though feebly saline and sulphurous waters are inet with. The springs of 
 Tuscarora and Chippawa, which issue from the Onondaga formation, are 
 remarkable for containing three or four thousandths of free sulphuric acid. 
 A similar spring occurs in the same formation at Byron in New York ; and 
 two others, at Niagara and St. Davids, rise from the Medina sandstones. 
 The action of the waters upon the calcareous strata through which they 
 pass, must give rise to sulphate of lime ; which might be deposited in 
 lenticular or dome-shaped masses, such as have been described above. 
 
 Masses of Conditions of the surrounding strata, similar to those which we have de- 
 scribed, are observed in the gypsiferous formations of other regions, and 
 have been explained by supposing a partial removal of a bed of gyp- 
 sum, through solution by infiltrating waters ; leaving only isolated masses, 
 around which the unsupported superior strata have fallen. Certain 
 appearances of disturbance in the gypseous rocks of the Alps have been 
 explained by supposing that the sulphate of lime was at one time in the 
 form of anhydrite ; which, by absorbing water, was converted into gypsum, 
 with a large increase of volume, uplifting the strata around. The beds of 
 gypsum which have been examined in the Onondaga formation in Canada, 
 seem however to have been in all cases contemporaneous with the shales 
 and dolomites in which they are interstratified, and to have no connection 
 with the acid springs of the present time. 
 
 If we suppose the gypsum to have been deposited in its present form, in 
 basins, we may conceive, that, when the surrounding and overlying strata 
 were subsequently consolidated by pressure, which would reduce then* 
 thickness much more than that of the solid crystalline gypsum, they would 
 conform to the masses of the latter, and appear to dip down on every side ; 
 precisely as we now see them in the gypsum quarries which have been 
 described. The hillocks in which the gypsum occurs, appear to be due to 
 the fact that the masses of gypsum, or the hard beds immediately overlying 
 them, have resisted denudation to a greater extent than the softer argilla- 
 ceous strata; which appear elsewhere to make up a great portion of the 
 formation. 
 
CHAP. XIII.] LOWER HELDERBERG GROUP. 353 
 
 THE LOWER HELDERBERG GROUP. 
 
 The rocks of the Lower Helderberg group, which in New York are found 
 overlying the Onondaga formation, appear, with the exception perhaps of 
 their lowest division, to be wanting hi Western Canada. Strata of this 
 group are however met with in the vicinity of Montreal ; and it is very 
 largely developed in the eastern portion of the province, where it includes 
 a part of the Gaspe* limestones. The description of these, for reasons 
 already stated, is reserved for a future chapter. 
 
 In the state of New York, the Lower Helderberg group was, by Mr. 
 Vanuxem, separated into the following five divisions, in ascending order : 
 1, Water-lime group, or Tentaculite limestone ; 2, Pentamerus limestone ; 
 3, Delthyris shaly limestone; 4, Encrinal limestone; 5, Upper Penta- 
 merus limestone. 
 
 1. Water-lime group, or Tentaculite limestone. In the central part of water-lime 
 New York, this division is described by Vanuxem as consisting of from group - 
 thirty to one hundred feet of limestone, chiefly dark blue in color, and fit 
 for ordinary lime ; with two drab colored layers, which yield a hydraulic 
 cement, and give the name of Water-lime to the series. The limestone is 
 often marked by colored bands of sedimentation ; and in some parts, it holds 
 nodules of chert, and geodes of celestine, gypsum, and fluor-spar. The 
 beds are often from three to five feet thick, and sometimes exhibit at their 
 surfaces the columnar markings which have been called epsomites. Some 
 of the drab colored beds, which are dolomites, also exhibit the lenticular 
 crystals of calcite, already described. The strata of this division, in their 
 lithological characters, closely resemble the upper portions of the preceding 
 gypsiferous series, with which they were in part confounded by Yanuxem ; 
 who classed the beds containing Eurypterus, with the Onondaga formation. Eurypterus 
 According to Mr. Hall, the drab colored strata characterized by this beds> 
 remarkable crustacean, are seen, in Oneida county, to underlie the dark 
 blue or black limestone ; which abounds in tentaculites and other fossils, 
 and constitutes, in his view, the true base of the Lower Helderberg group. 
 This group, as thus defined, is not seen farther west than the centre of 
 the state ; while the drab colored dolomitic beds, which contain scarcely 
 any other fossils than Eurypterus, and allied crustaceans, extend through- 
 out western New York, and have been identified through a portion of 
 Western Canada. They rest directly upon the Onondaga formation, and 
 constitute, throughout that region, the summit of the Silurian series. 
 
 The Water-lime series, as thus defined, enters Canada opposite to Buf- 
 falo, and can be traced pretty continuously,, in a band varying from twenty 
 
 x 
 
354 GEOLOGY OF CANADA. [CHAP. XIII. 
 
 Bertie. to .forty-five feet in thickness. This series has been found to exhibit its 
 characteristic fossils, in three localities, in Canada.* One of these is on 
 the fifth lot of the tenth range of Bertie, where the following ascending 
 section occurs : 
 
 Ft. in. 
 
 Dark bluish-grey shaly dolomite, 1 
 
 Light bluish-drab dolomite (water-lime), in beds of from one inch to 
 
 one foot ; containing Eurypterus remipes, 3 6 
 
 Grey dolomite in beds of from one to eight inches, 10 
 
 Measures concealed in an escarpment which rises from the previous 
 bed, but supposed, from fragments by which they are covered, to 
 be of the same character as before, . . 6 
 
 20 6 
 
 Jones's tract. The second locality is on Jones's tract, where, in continuation of the beds 
 already given as constituting the summit of the Onondaga formation, we 
 have the following ascending series : 
 
 Ft. in. 
 
 Lavender-grey compact dolomite, of a lighter color on the weathered 
 surfaces ; it is brittle, with a conchoidal fracture, and presents' 
 beds of from two to three inches in thickness, 7 
 
 Brownish-grey shaly dolomite, 5 
 
 Greyish-drab dolomite (water-lime), containing remains of Eurypterus 
 
 remipes, and fragments of an undetermined Cemtiocarus, 2 6 
 
 Grey hard slaty dolomite, weathering brown, 1 
 
 Brownish-grey porous crystalline dolomite, in beds of from one to 
 
 three feet thick, 5 
 
 Grey conglomerate or breccia, composed of a light grey calcareous 
 paste, holding small angular masses of a darker grey and more 
 compact dolomite, with a brownish tint. The whole mass weath- 
 ers yellowish, and is divided into beds varying from four to twelve 
 inches in thickness, 4 
 
 Grey porous dolomite, interlaminated with very thin bluish leaves, 
 which in section appear to run irregularly and interruptedly, as 
 if the bed had been broken and re-cemented. The rock, which is 
 lighter colored on weathered surfaces, is divided into beds of from 
 two to ten inches in thickness, and is interstratified with thin 
 beds of fine grained dolomite. It holds nodules of light yellowish 
 chert, weathering almost opaque white, and leaves of dark brown- 
 ish bituminous shale, 20 6 
 
 45 
 
 The third locality is at Rattlesnake Falls, on a small tributary of the 
 Grand River, on the thirty-fifth and thirty-sixth lots of the first range 
 
 * Figures of the Eurypterus, and of some Helderberg group, will be given in the 
 of the characteristic fossils of the Lower Appendix to this volume. 
 
CHAP. XIII.] LOWER HELDERBERG GROUP. 355 
 
 south of the Talbot road, in Cayuga ; where a series of beds occurs, very cayuga. 
 much resembling those of Jones's tract, but showing not more than half the 
 thickness. Fragments of Ceratiocarm are seen in a two-feet bed, about 
 six feet from the base, and Leperditia alta occurs six feet above. 
 
 2. Pentamerus limestone. In the eastern part of New York, this is a 
 dark grey concretionary limestone in irregular layers ; associated with a 
 small amount of black shale, and holding fossils, of which the most char- 
 acteristic is Pentamerus galeatus. It extends from Ulster to Onondaga 
 county, and attains its greatest thickness at Cherry Valley, where it is 
 about thirty feet. It is not recognized in the western part of New York. 
 
 3. Deltkyris shaly limestone. This division, like the last, occurs only in 
 the eastern part of the state, extending from Ulster to Madison county, 
 and is a mixture of blue drab-weathering calcareous shale and blue lime- 
 stone. It is very fossiliferous, and takes its name from the frequent occur- 
 rence of two species of Spirifera (formerly called Delthyris), S. macro- 
 pleura and S. pacJwptera. It appears to attain its greatest thickness in 
 Albany county, where it is stated to be sixty or seventy feet. 
 
 4. Encrinal limestone. This is a mass of light-grey limestone, holding a 
 large quantity of broken encrinites ; the peculiar crystalline structure of 
 these remains giving a crystalline character to the rock. It contains in 
 great abundance a shield-like pelvis of a crinoid, from which it is some- 
 times called the Scutella limestone. Its greatest thickness is about twenty- 
 five feet, and it extends, along with the previous division from Ulster to 
 Schoharie county. 
 
 5. Upper Pentamerus limestone. This division, which is still more 
 restricted than the preceding ones, is characterized by the Pentamerus 
 pseudo galeatus, and by several species of Rhynchonella. These local sub- 
 divisions however, according to Hall, cannot be recognized at any great 
 distance from the Helderberg mountains ; although this group, as a whole, 
 has a wide geographical distribution. 
 
 As already stated, none of the members of this group, with the exception 
 of the Water-lime series, are recognized in the- western part of New York, 
 or in Western Canada. In Eastern Canada, besides the Gaspe* limestones, 
 which belong to the great eastern palaeozoic basin, there are evidences of 
 the existence of the Lower Helderberg group in two or three small outliers 
 in the great western basin, near to Montreal ; and at a distance of about 
 two hundred miles from the nearest position of the group in New York. 
 Of these, the most important is on the island of St. Helen's, opposite 
 to Montreal. 
 
 This outlier appears to repose on the Utica formation ; the shales of Lower Hei- 
 which, with some of their characteristic fossils, are visible at the upper ^J berg out " 
 extremity of the island. The deposit consists principally of a conglomerate, 
 the enclosed masses in which are sometimes rounded, but chiefly angular. 
 
356 GEOLOGY OF CANADA. [CHAP. XIII. 
 
 They consist of fragments of Laurentian gneiss ; of white quartzose sandstone 
 resembling that of the Potsdam formation ; of dark grey limestone, in some 
 cases holding Trenton fossils ; of black shale resembling that of the Utica 
 formations ; and of red sandstone and red shale similar to those of the 
 Medina. With these fragments are associated others of igneous rocks. 
 All of these, varying in size from a quarter of an inch to five and six 
 inches in diameter, are enclosed in a paste of a light-grey dolomite, which 
 weathers to a reddish-yellow. 
 
 st. Helen's The island has a north and south length of about 1200 yards, with a 
 island. k rea( jth of between 600 and 700, and the conglomerate rises into two 
 small hills, separated by a narrow ravine crossing the island obliquely ; the 
 southern hill having a height of about 125 feet. In neither of these hills 
 have there been observed any divisional planes clearly referable to strati- 
 fication ; but there are many parallel vertical joints, running in the bearings 
 S. 30 E., S. 35 E., and S. 60 E. About two thirds of the distance down 
 the east side of the island, nearly opposite to one end of the ravine, there 
 occur two masses of dark grey fossiliferous limestone, weathering to a light 
 grey ; which are not magnesian. These are included in a length of about 
 forty yards, and are limited on the east side by the water of the river; they 
 have a breadth of scarcely more than ten feet, and appear to run under the 
 dolomitic conglomerate on the west side. They present, in section, the 
 appearance of two small arches of about four feet in height, separated from 
 one another by a few feet of the conglomerate, and sinking under the same 
 rock on the north and south. Two parallel dolerite dykes, running N. 
 75 W., cut both the limestone and the conglomerate, their position being 
 partially intermediate between the two fossiliferous masses ; which seem 
 to be related to an anticlinal fold, with a dislocation running along 
 the axis. The dolomite and the limestone seem to pass into one another for 
 a few inches, and show no tendency to separate at the junction. The 
 fossils observed in the limestone are Favosites Grothlandica, iStrophomena 
 rhomboidalis, S. punctulifera, Orthis oblata, an undetermined species of 
 Khynchonella with R. Wilsoni ; Athyris bella, Atrypa reticularis, and two 
 undetermined species of Spirifera. 
 
 As none of this limestone comes from beneath the conglomerate, where 
 this reposes upon the Utica formation, it is supposed to belong to a 
 small disturbed lenticular portion, lying in or under the conglomerate. 
 Smaller patches of the same limestone, a few feet in diameter, are seen 
 in the forty yards north of the two chief masses ; and the whole may be 
 connected beneath. There are other masses of similar limestone, only a 
 few inches in diameter, which are completely enveloped in the conglom- 
 erate. It would seem therefore that this magnesian rock is younger than 
 the fossiliferous limestone, upon which it is deposited, inasmuch as frag- 
 
CHAP. XIIL] LOWER HELDERBERG GROUP. 357 
 
 ments of the latter are mingled with those of older rocks in the paste of 
 the conglomerate. 
 
 Round Island, which is a little north of St. Helen's, is composed of the Bound island, 
 same dolomitic conglomerate ; and there is no doubt that the channel be- 
 tween the two islands is floored with the same rock. The area occupied by 
 the deposit, including both islands, and making some allowance for what 
 may be concealed by the water on each side, very probably does not 
 exceed half a square mile. The surface of Round Island is not in any 
 part more than ten or fifteen feet above the St. Lawrence, and there does 
 not appear to be any special difference in the composition of the con- 
 glomerate in the two islands. The only mass observed in the conglom- 
 erate of Round Island, which resembled the newer limestones of St. 
 Helen's, was one of eight or ten inches in diameter, holding an unde- 
 termined species of HeliopJiyllum. 
 
 On the north-west side of Isle Bizard, not far from the outcrop of the i s i e Bizard. 
 Chazy formation, but resting on the Calciferous, there occurs an exposure 
 of dolomitic conglomerate so similar to that of St. Helen's, with the 
 exception of the associated masses of Lower Helderberg limestone, that 
 it is most probably of the same age. This outlier has an area of about 
 a hundred paces in length, by about fifty in breadth, and rises to a height 
 of fifty-five feet ; forming a bold hillock on a flat country: The paste of 
 the conglomerate has a greyish or slightly greenish color, and weathers to 
 an orange-brown. Many of the enclosed fragments are composed of a 
 sandstone resembling that of the Potsdam formation, and some are of a 
 fine grained dark grey hard silicious slate. The fragments vary in size 
 from a quarter of an inch to five or six inches in diameter. 
 
 On the right bank of the Riviere des Prairies at the White Horse Rapids, 
 about four and a half miles east of the mass on Isle Bizard, there is 
 another of the same description, occupying a somewhat larger area ; while 
 about six miles to the west of that on Isle Bizard, there is still another, on 
 the road between St. Eustache and the Indian Mission of the Lake of 
 Two Mountains. It is on the north side of the most eastern of the Lau- 
 rentian hills of that vicinity, and lies, partly on the Potsdam sandstone, and 
 partly on the Laurentian gneiss ; of which latter rock the fragments 
 enclosed in the dolomitic paste are in part composed. 
 
 In one of the cuttings for the Grand Trunk Railway, between Point ste. Anne. 
 Claire and Ste. Anne, there occurs a strip of a similar dolomitic conglomer- 
 ate, filling a worn fissure in Trenton limestone. It is about a foot in width 
 and some ten or twelve feet in length, but none of it appears on the 
 surface of the limestone on either side. A fissure crossing the promon- 
 tory on the west side of Shelburne Bay, near Burlington in Vermont, is 
 described by Mr. C. H. Hitchcock as being filled with a conglomerate 
 dyke. Specimens of this have a remarkable resemblance to the con- 
 
358 GEOLOGY OF CANADA. [CHAP. XIII. 
 
 glomerate of St. Helen's Island, and very probably belong to a contempo- 
 raneous deposit. 
 
 From these scattered outlying patches, it would appear that a consider- 
 able area in the Champlain and St. Lawrence valleys was once continu- 
 ously covered with rocks of the Lower Helderberg group ; while from 
 the unconformable relation of these to the formations on which they repose, 
 it is evident that, prior to the Lower Helderberg period, the older fossiliferous 
 strata had suffered a great amount of denudation. The horizontal surface 
 of the region around these outlying masses, farther shows, that, since the 
 deposition of these newer rocks, denuding agencies cannot have greatly 
 affected the older strata ; but that their action has been confined to the 
 Lower Helderberg or to more recent sediments, which have disappeared ; 
 and that consequently the geographical distribution of the Lower Silurian 
 rocks in this vicinity, is now essentially the same as it was at the com- 
 mencement of the Lower Helderberg period. 
 
 Besides the two dolerite dykes which have been mentioned, several 
 others of a similar character intersect the dolomitic conglomerate of St. 
 Helen's Island. These strongly resemble a certain set of dykes which .cut 
 alike the Utica, Trenton, and Chazy formations at Montreal, and the Lau- 
 rentian series in Grenville, and are described in their proper place. 
 
CHAP. XIV.] GEOLOGY OF CANADA 359 
 
 CHAPTER XIV. 
 
 THE ORISKANY AND CORNIFEROUS FORMATIONS. 
 
 BASE OF THE DEVONIAN SERIES. ORISKANY SANDSTONE. CAUDA-GALLI GRIT AND SCHOHAEIB 
 GRIT OF NEW YORK. ORISKANT FORMATION IN CANADA. THE UPPER HELDERBERG GROUP 
 CORNIFEROUS FORMATION; ITS DISTRIBUTION IN CANADA. Two AREAS IN THE WESTERN 
 PENINSULA. CINCINNATI ANTICLINAL. THE FORMATION ON LAKE HURON; ON THE DE- 
 TROIT RIVER. BITUMINOUS BEDS; PETROLEUM SPRINGS. UNDULATIONS OF THE FORMATION. 
 
 The calcareous rocks of the Lower Helderberg series are followed in 
 New York by an arenaceous group, divided in ascending order as follows : 
 1, Oriskany sandstone ; 2, Cauda-galli grit ; 3, Schoharie grit. These 
 divisions there appear to be characterized by distinctive fossils; but in 
 Canada, several of the most characteristic species belonging to the lowest 
 division, ascend into the Corniferous formation, which overlies them all. Devonian 
 They are therefore to be looked upon only as local subdivisions of a sand- series - 
 stone formation, which is regarded as the base of the Devonian series. 
 
 The Oriskany sandstone is traceable in New York, from the valley of Sandstones, 
 the Hudson in Ulster county, to the neighborhood of Buffalo on Lake 
 Erie, as a band of white or yellowish rather coarse and sharp grained 
 slightly calcareous sandstone, varying in thickness from an inch to thirty 
 feet. It abounds in characteristic organic remains; of which many of 
 the species are of large size, and usually occur as casts and impressions. 
 Remains of plants, described as fossil wood, are said by Mr. Emmons to 
 have been met with hi this band, at New Scotland in Albany county. 
 The top of the band is in some places marked by a fucoid, which resem- 
 bles a cock's tail, and gives its name to the next division. 
 
 The Cauda-galli grit, which succeeds, is a crumbling argillaceous sand- 
 stone, approaching to an arenaceous shale ; passing from bluish-drab below to 
 brownish above. Its usual thickness is not given, but it sometimes attains 
 seventy feet ; and it abounds with the peculiar fucoid already mentioned, 
 which covers the surfaces of successive beds of the deposit. The band 
 ranges from Ulster to Herkimer county, but is not known farther west. 
 
 The Schoharie grit rests upon the previous bed in Albany county, to 
 which it appears to be confined, and is a brownish decomposing calcareous 
 
360 GEOLOGY OF CANADA. [CHAP. XIV. 
 
 sandstone, with a thickness of about four feet. It abounds in fossils, -which 
 in New York are different from those in the strata above and below. 
 
 It appears to be the lowest only of these bands which enters Canada at 
 Waterloo, on the Niagara River. In its lithological characters, it does not 
 seem to differ materially from the same rock in New York. The lower 
 beds appear in several places to be composed of chert or hornstone, fre- 
 quently containing large quantities of iron pyrites, and occasionally beau- 
 
 chert. tiful specimens of purple fluor-spar. This chert is sometimes found to 
 
 descend continuously, into small vertical fissures in the rock beneath, and, 
 sending out parallel horizontal seams for short distances, to enclose small 
 flat portions of the strata, as if these had been partially broken up before 
 the deposit of the chert. Resting on these beds, there is a sandstone, 
 which is somewhat different in different localities. In the township of 
 Dunn, near Haldimand, it is frequently made up of large angular pieces of 
 hornstone ; which, with the numerous large corallines and other fossils 
 present, render it almost useless as a building stone. In the townships of 
 
 North Cayoga. Oneida and North Cayuga, particularly on the forty-sixth, forty-ninth, 
 and intermediate lots of the first range north of the Talbot road, m the 
 latter township and the corresponding lots in the former, there are large 
 exposures of the rock. It is composed of fine grains of white quartz, in 
 some parts so closely cemented as to assume the characters of a white 
 compact quartzite. In other parts, it is made up of coarser grains of 
 quartz, some of them being an eighth of an inch in diameter and pretty 
 well rounded. With these, there are occasionally grains of feldspar. 
 The rock in these cases, being sometimes slightly calcareous, disinte- 
 grates by exposure to the weather. The beds are massive, and from six 
 inches to six feet thick. They are in many places well adapted for building 
 purposes, and some of them have been applied to the manufacture of mill- 
 stones for grinding oats. The sandstone in some parts very much resem- 
 bles the white beds of the Potsdam formation ; but it passes from white to 
 light grey, and, in some places, through yellowish to brown. It is not 
 improbable that portions of it would be found sufficiently free from iron to 
 be used for glass-making. The greatest thickness of the mass may be 
 about twenty-five feet ; but though now and then attaining ten feet, it 
 seldom exceeds about six, and it is frequently wanting between the Water- 
 lime series and the overlying Corniferous formation. 
 
 The rock abounds in organic remains. The species met with in the 
 exposures in North Cayuga just mentioned, are JFavosites G-athlandica, 
 F. hemispherica 9 F. turbinata, Zaphrentis prolifica, Heliophyllum exiguum, 
 Cystiphyllum sulcatum, an undetermined Coscinium, Strophomena rhom- 
 boidalis, tS. incequistriata, 8. perplana, S. magnified, 8. magniventra, 
 8. ampla, Ohonetes hemispherica, Orthis musoulosa, Centronella glcms- 
 faga, StricUandia elongata, Renmlaeria ovalit, R, ovoides, Pentamerua 
 
CHAP. XIV.] CORNIFEROUS FORMATION. 361 
 
 aratus, Spirifera arenosa, /S. arrecta, Cyrtia rostrata, Atrypa 
 Conoeardium trigonale, Avicula arenosa, Platyostoma ventricosa^ 
 Platyceras nodosum, undetermined species of Turbo and Orthoceras, Caly- 
 mene Blumeribaeliii, Phillipsia crassimarginata, Dalmanites anehiops^ 
 with an undetermined species of fish.* The band being thin, it generally 
 appears in its distribution as a very narrow border to the succeeding for- 
 mation. The exposure in North Cayuga, which is the largest that haa 
 been seen in Canada, does not exceed 230 acres, and the Oriskany 
 formation is not yet known to extend beyond the township of Windham. 
 
 THE CORNIFEROUS FORMATION. 
 
 In New York and in Western Canada, the sandstone just described, 
 or, where this is wanting, the Water-lime series is followed by bitumi- 
 nous limestones, holding a large amount of chert or hornstone; from 
 which the name of Corniferous has been given to the formation. In 
 New York, it is divided into two masses, supposed to be distinguished 
 by characteristic fossils, and, in some degree, by lithological peculiar- 
 ities. The lower portion consists of beds of a light grey limestone, occa- Encnnai 
 sionally almost altogether composed of broken encrinal columns and corals, Umestone - 
 and having much the appearance of the beds at the base of the Niagara 
 limestone ; particularly when, as in this, the organic remains are of a 
 reddish tinge. It then yields a handsome variegated marble, and it 
 generally affords good stone for building and for lime-burning. The strata 
 are in many localities separated by thin layers of green shale ; nodules of 
 chert are common, and towards the top, in some places, beds of this 
 silicious mineral alternate with those of limestone, forming a passage to 
 the upper portion. This is a limestone of a compact texture, and varies in 
 color from drab and light grey, through different shades of blue, to black; 
 having, in this case, black shales associated with it. The hornstone which Hornstone 
 occurs in the lower division, is frequently very largely developed in this, or chert ' 
 and sometimes constitutes nearly the whole of the strata. The rock is 
 fossiliferous, but not so abundantly as the one below, and the corals are 
 in smaller proportion. The lower division attains, in New York, a thick- 
 ness of twenty feet, and has there been called the Onondaga limestone ; a 
 title not to be confounded with that of the underlying Onondaga formation, 
 or Salt group. The name of Corniferous limestone is, by the New York 
 
 * Figures of some of the characteristic fossils of this formation will be given in the 
 Appendix to this volume. 
 
362 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XIV. 
 
 Upper 
 Helderberg. 
 
 geologists, restricted to the upper division, which has in that state a 
 thickness of about seventy feet. These two portions, with the addition of 
 the local Schoharie grit, make up what they have described as the Upper 
 Helderberg group. 
 
 In Western Canada, we find that many of the fossils of the Corniferous 
 limestone pass up from the Oriskany sandstone ; and the intermediate 
 
 353-355. ZOOPHYTA. 
 b 
 
 354 
 
 353. Favosites basaltica (Goldfuss) ; club-shaped variety. 
 
 354. F. hemispherica (Yandell and Shumard) ; a, specimen showing 
 
 the variations in the size of the cells ; 6, specimen show- 
 ing the incomplete transverse diaphragms. 
 
 355. F. turbinata (Billings); a, portion of the surface enlarged, show- 
 ing the different appearances of the cells when closed ; 
 &, side view of a small imperfect specimen. 
 
 Onondaga limestone, with its encrinites, can no longer be recognized as a 
 distinct formation. We therefore unite the two limestones under the 
 name of the Corniferous formation. 
 
 The surface occupied by this formation in Western Canada is probably 
 between 6000 and 7000 square miles. A great part of this however is 
 deeply covered by drift, so that the exposures are comparatively few. 
 To the eastward, this formation is bounded by the outcrop already 
 assigned to the underlying strata ; the limits of which in many parts have 
 as yet been but imperfectly traced. The whole of the province to the 
 
CHAP. XIV.] 
 
 CORNIFEROUS FORMATION. 
 
 west and south of this line, belongs to the Corniferous formation ; with the 
 exception of a belt of higher Devonian rocks, which crosses the country 
 from Lake Huron to Lake Erie, and divides the region into two areas. 
 These newer strata occupy a saddle-shaped depression on the great Gin- synclinal, 
 cinnati anticlinal, which runs nearly east and west through the peninsula ; 
 while the course of this depression or synclinal is nearly north and south, 
 from Plympton on Lake Huron, to Oxford on Lake Erie. The belt of 
 higher rocks has a breadth of only about twenty-five miles on the anti- 
 
 356, 357. ZOOPHYTA. 
 
 356. Favosites cervicornis (De Blainviile). 
 
 357. p. polymorpha (Goldfuss) ; three specimens. 
 
 clinal, between the Thames and Sydenham Rivers ; but on either side, it 
 spreads to the north-east and to the south-west, along the shores of the 
 two lakes. 
 
 Outliers of the higher rocks may very probably yet be found within these 
 areas of the Corniferous formation ; and subordinate undulations may, in 
 some places, bring to the surface, domes or ridges of the Oriskany and 
 Onondaga formations. The only evidences as yet obtained of the probable 
 outcrop of these inferior rocks, within the areas in question, are found in 
 two localities on the shore of Lake Huron ; the one at Goderich, and the 
 other at Point Douglas. 
 
364 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XIV. 
 
 Thickness of 
 formation. 
 
 Distribution. 
 
 The generally small dip of the strata, and the frequent occurrence of 
 slight undulations, render it very difficult to find the succession of the 
 beds, or to determine with accuracy the whole thickness of the Cornif- 
 erous formation. The great extent occupied by it in Western Canada, 
 however, makes it probable that it must be much more considerable here 
 than in New York. In the townships of Woodhouse and Townsend, 
 where there are frequent exposures, the breadth at right angles to the 
 
 ). ZOOPHYTA. 
 
 358 
 
 358. Fistulipora Canadensis (Billings). 
 359. Michelinia convexa (D'Orbigny). 
 
 strike is upwards of ten miles. The fall of the surface, in that distance, is 
 estimated at 140 feet ; so that if the average slope does not exceed thirty 
 feet in a mile, there would here be a thickness of about 160 feet of the Cor- 
 niferous limestone. The strata, which in Michigan are considered as the 
 equivalents of this formation, have, according to Prof. Winchell, a thick- 
 ness of about 350 feet ; so that it would appear that the thickness gradu- 
 ally augments to the westward. 
 
 The formation enters Canada from New York, nearly opposite Buffalo, 
 and is traceable, in a narrow belt, along the shore of Lake Erie, resting on 
 the Oriskany sandstone ; or, where this is wanting, on the Water-lime series. 
 At Horn's quarry, in Bertie, two miles below Ridgway station, on the 
 
CHAP. XIV.] 
 
 CORNIFEROUS FORMATION. 
 
 365 
 
 railway, there is a section of nearly twenty-four feet ; and at various points Bertie, 
 on the lake, or at a short distance inland, sections of from ten to twenty 
 
 360-363. ZOOFHYTA. 
 
 360. Zaphrentis prolifica (Billings) ; a, side view ; b, view 
 
 of the cup. 
 
 361. Cystiphyllum aggregation (Billings). 
 362. Haimeophyllum ordinatum (Billings). 
 363. Phillipsastrea Verneuili (Edwards and Haime). 
 
 feet have been observed, as far as Woodhouse and Middleton. In many 
 parts, it is quarried for building purposes ; while some portions abound in 
 
GEOLOGY OF CANADA. 
 
 [CHAP. XIV. 
 
 Chert beds, chert, which forms beds of from one to four inches, or exists in nodules 
 like flints in the limestone. Many of the beds contain silicified organic 
 remains. These, in some localities, as in North Cayuga and at Port Col- 
 borne, are found weathered out and loose, in great abundance, at the 
 
 364. vtfwfopora cornuta (Billings) ; a, 6, c, three specimens. 
 
 365. A. umbellifera (Billings) ; a, b, two specimens. 
 
 366. Syringopora Maclurea (Billings). 
 
 367. S. , Hisingeri (Billings). 
 
 368.S. perelegans (Billings). 
 
 369. Eridophyllum Simcoense (Billings). 
 
 370. E. Verneuilanum (Edwards and Haime). 
 
 371. JLlveolites labiosa (Billings) ; a, &, two specimens. 
 372. A. cryptodens (Billings). 
 
 surface of the ground. Some of the beds are little more than an aggre- 
 gate of silicified organic remains ; with so little calcareous matter, that the 
 whole mass coheres, after the carbonate of lime has been dissolved out. 
 The Corniferous limestones, unlike the great mass of the Middle and 
 Upper Silurian strata, in Western Canada, effervesce freely with acids, 
 
CHAP. XIV.] 
 
 CORNIFEROUS FORMATION. 
 
 367 
 
 and are not dolomitic. Some of the beds are marked with epsomites, 
 as on the lake shore near Port Dover, where these impressions occur 
 
 373-377. BKACHIOPODA. 
 
 373 
 
 374 
 
 373. Slrophomena rhomboidalis (Wahlenberg). 
 
 374. 8. Patersoni (Hall). 
 
 375. 8. incequistriata (Conrad) ; a, ventral aspect ; 6, 
 
 longitudinal section. 
 
 376. S. ampla (Hall) j a, dorsal aspect ; 6, longitudi- 
 nal section ; c, view of the area. 
 
 377. S. demissa (Conrad) ; a, 6, c, d, different views of 
 
 two specimens. 
 
 between layers of limestone and chert ; the latter being apparently the 
 overlying bed. These strata are often highly bituminous : petroleum is 
 found in many places, filling the pores of the corals, and in one case a drusy 
 
368 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XIV. 
 
 Petroleum, cavity in a Pentamerus. Instances of oil-bearing coral beds are met 
 with at Horn's quarry in Bertie ; near Gravelly Bay in Wainfleet ; and 
 near the village of Jarvis. In other beds, however, the cells of the corals 
 are empty. In some parts along the lake shore, thin layers of bitumi- 
 nous shale are met with in the limestones. 
 
 378-381 . BBACHIOPODA. 
 
 378 
 
 378. Strophomena ampla (Hall). 
 
 379. Chonetes ? a and b, ventral valves of undeter- 
 mined species. 
 
 380. C. hemispherica (Hall) ; a, ventral aspect ; b, lon- 
 gitudinal section ; c, view of the hinge line, 
 showing the bases of the spine, and the striated 
 area. 
 
 381. Producta ? a small and undetermined species ; 
 
 a, side view ; 6, ventral view. 
 
 To the west of the Grand River, in the counties of Haldimand and 
 Norfolk, the Corniferous limestones are often seen resting on the Oriskany 
 formation, and forming small eminences ; which present escarpments, with 
 the sandstone at their base. These limestones are here of a drab color, and 
 abound in chert. The organic remains with which the strata abound, are 
 entirely silicified in many of the beds ; while in others, they have undergone 
 
CHAP. XIV.] 
 
 CORNIFEROUS FORMATION. 
 
 369 
 
 no such change. Among the species characterizing these and the immediately 
 succeeding beds, constituting probably about twenty feet of the formation, 
 are Fistulipora Canadensis, Favosites G-othlandica, F. hemispherica, F. 
 basaltica, F. turbinata, F. cervicornis, F. polymorpha, Michelinia convexa, 
 M. inter mittens, M. favosidea, Syringopora Maclurei, S. Hisingeri, S. 
 perelegans, Zaphrentis prolifica, Z. gigantea, Z. exiguum, Heliophyllum 
 Eriense, H. Cayugaense, H. Canadense, H. colligatum, Phillipsastrea 
 
 382-385. BBACHIOPODA. 
 
 a 382 6 
 
 382. Leptoccelia flabellites (Conrad) ; a, dorsal, and b, side view. 
 383. L. concava (Hall) ; a, 6, c, three views of the same 
 
 species. 
 384. Streptorhynchus Pandora (Billings); a, dorsal valve; &, 
 
 longitudinal section. 
 385. Orthis Lima (Billings) ; a, ventral, b, side, and c, dorsal 
 
 view. 
 
 gigas, Olisiopliyllum Oneidaeme, Blothrophyllum decorticatum, Urido- 
 pkyllum Verneuilanum, E. Simcoense, DipTiypTiyllum arundinaceum, D. 
 stramineum, Cystiphyllum sulcatum, 0. Senecaense, 0. grandis, Orthis 
 Livid, Streptorhynchus Pandora, StropJiomena rhomboidalis, S. ampla, $. 
 perplana, S. Pattersoni, S. incequiradiata, S. demissa, an undetermined 
 species of Chonetes with O. arcuata, KhyncTwnella Thalia, R. Tethys, Pen- 
 tamerus aratus, Stricklandia elongata, Centronella glam-faga, C. Hecate, 
 Leptoccelia flabellites, L. concava, Spirifera duodenaria, S. fimbriata. 
 
370 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XIV. 
 
 S. raricosta, with undetermined species of the same genus, Cyrtena 
 rostrata, Aihyris Clara, A. Clusia, Spirigera concentrica, Atrypa reticur 
 laris, Conocardium trigonale, Platyostoma ventricosa, two undetermined 
 species of Orthoceras, and one of Cyrtoceras, Phacops bufo, Phillipsia 
 
 386-389V-BBAOHIOPODA 
 
 386. Rhynchonella Thalia (Billings) ; a, 6, c, three views of a specimen. 
 
 38*7. R. Tethys (Billings) ; a, 6, side views of two specimens; 
 
 c, front view. 
 
 388. R. Medea (Billings) ; a, dorsal, and 6, side view. 
 
 389. Pentamerus aratus (Conrad) ; a, 6, ventral and dorsal views of a 
 
 small specimen; 
 large specimen. 
 
 c, d, dorsal and side views of a 
 
 crassimarginata, two undetermined species of Dalmanites, with remains 
 of fishes. 
 
 Higher in the series, along the same line of country, blue limestones, 
 sometimes to the amount of twenty feet, with grey beds in less volume, 
 
CHAP. XIV.] 
 
 CORNIFEROUS FORMATION. 
 
 371 
 
 are associated with cherty layers, and interstratified with bands of a drab- 
 oolored limestone. These strata are sometimes quarried, and yield stone 
 fit for building purposes. 
 
 An outcrop of the Corniferous limestone occurs near Woodstock, nearly Woodstock, 
 on the axis of the main east and west anticlinal of the peninsula. To the 
 north of this exposure, the western boundary of the formation is traced by 
 the abundant fossils, which are found loose on the surface, in Wallace and 
 Elma. Farther on, escarpments of twenty or thirty feet of the limestone, 
 run through the west half of Carrick, and are said to extend southward 
 into Ho wick ; while, to the north, the outcrop of the formation crosses the 
 
 390. BBACHIOPODA. 
 
 390. Stricklandia elongata (Vanuxem) ; a, 5, two specimens, showin g 
 the narrow and the broad forms. 
 
 south-west corner of Brant, and is seen upon the Teeswater, near the east 
 
 line of Greenock. The general trend of the strata would bring them upon Lake Huron. 
 
 Lake Huron, near the mouth of the Saugeen River. No exposures have ? 
 
 however, been observed at this point, nor for seven miles to the south-west, 
 
 along the coast. Beyond this, however, nearly horizontal buff-colored beds 
 
 appear, at about two feet above the edge of the lake ; holding numerous 
 
 organic remains, which are frequently replaced by chert. These beds 
 
 come out at intervals along the shore, the surface of the same stratum 
 
 being sometimes exposed for a considerable distance : they occupy altogether 
 
 a distance of four or five miles. Among the fossils found here, are Favo, 
 
 sites Grothlandica, Zaphrentis prolifica, Syringopora Hisingeri, Erido- 
 
372 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XIV. 
 
 phyllum Verneuilanum, Strophomena rhomboidalis, S. incequistriata, 8. 
 perplana, Orthis lowensis, Spirifera gregaria, S. Umesialis, Cyrtena 
 
 891-394 . BBACHIOPODA. 
 
 391. Spirifera gregaria (Hall) ; a, b, c, three views of the same specimen. 
 
 392. 8. raricosta (Conrad) ; a, dorsal, and &, side view ; c, ven- 
 tral view of a partially exfoliated specimen. 
 
 393. S. fimbriata (Conrad) ; a, 6, c, different views of the same 
 
 specimen. 
 
 394. S. duodenaria (Hall) ; a, dorsal view ; 6, view of the hinge 
 
 line ; c, dorsal view of another specimen. 
 
 rostrata, Aihyris Maia, Atrypa reticularis, Lucina elliptica, Conocardium 
 trigonale, and PJiacops bufo. 
 
 Beyond this, another interval of concealment occurs, to within three 
 miles of Point Douglas. Here, a yellowish calcareous sandstone skirts the 
 
CHAP. XIV.] 
 
 CORNIFEROUS FORMATION. 
 
 373 
 
 coast line ; and proceeding along the beach towards the point, the sand- Point 
 stone is found to be associated with calcareous beds, holding numerous Dou g la - 
 nodules of chert, with black bituminous shales, and blue and drab dolo- 
 mites; one bed among which is fit for hydraulic cement. The whole 
 of these strata appear to be devoid of fossils ; but they contain crystallized 
 celestine, quartz, and calcite, in geodes and fissures. A black band, 
 
 395-399. BBACHIOPODA. 
 
 395. Retzia Eugenia (Billings) ; a, dorsal, and 6, side view. 
 
 396. Athyris unisulcata (Conrad); a, dorsal, and b, ventral view; 
 
 c, view of the front margin. 
 
 397. A. Clara (Billings) ; a, dorsal, and 6, ventral view. 
 
 398. #. Mala (Billings) ; a, dorsal, and b, ventral view. 
 
 399. Spirigera concentrica (Von Buch) ; specimen with the front margin 
 
 truncated. 
 
 of a coarsely granular texture, overlies the sandstone, and appears to 
 be composed of an aggregate of imperfect crystals of calcite ; while 
 the color results from the presence of bituminous matter, which exists, 
 in greater or less proportion, in all of the beds. Ascending in the section, 
 which at Point Douglas displays a thickness of twelve feet, thin calcareous 
 beds of a dark color occur, separated by very thin layers of black bitumi- 
 
374 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XIV. 
 
 nous shale. Above them, the upper part of the cliff is occupied by thin 
 blue layers, with pale yellowish beds, sometimes more than a foot in thick- 
 ness, marked by small lenticular crystals of brownish calcite, and by 
 epsomites. Portions of these non-fossiliferous strata continue to occupy the 
 coast to the southward, with gentle undulations, to a point about half a 
 mile beyond Little Pine Brook. Here, fossiliferous cherty beds, similar to 
 
 400. Charionella Circe (Billings) ; a, dorsal view of a specimen which 
 shows some remains of spiral appendages ; 6, ventral, and 
 c, side view ; ?, portion of the interior of the dorsal valve, 
 showing the absence of a hinge plate ; e, fragment of the 
 ventral valve of C. Dons. 
 
 Doris ? (Hall) ; a, dorsal, and 6, side view. 
 
 ; a, 6, an undetermined species, perhaps a small 
 
 401. C. 
 
 402. C. 
 
 specimen of C. Doris. 
 4Q3.Centronella Hecate (Billings) ; a, specimen showing the loop ; b, c, 
 
 d t different views of another specimen. 
 
 404. C. tumida (Billings) ; a, b, c, three different views. 
 
 405. C. glans-faga (Hall) ; a, &, c, three different views. 
 
 those on the other side of Point Douglas, are seen, overlying the highest of 
 the strata already mentioned, in detached isolated portions, for upwards of 
 a mile ; beyond which, no rock is exposed for upwards of twenty-five miles. 
 Kincardine. Near the village of Kincardine, in the sixth and seventh lots of the 
 township of that name, is a quarry on the land of Mr. C. R. Barker, 
 where from fifteen to twenty feet of the formation are exposed, consisting 
 for the most part of thick bedded light and dark grey granular limestones; 
 which are quarried both for building stone and for burning, and yield a 
 
CHAP. XIV.] 
 
 CORNIFEROUS FORMATION. 
 
 375 
 
 very white lime. The lighter colored beds contain a few corals. No 
 chert was observed here, but the rocks are bituminous ; and towards the 
 top, are thinner beds, interstratified with layers of a dark brown inflam- 
 mable shaly limestone, some specimens of which contain a large proportion 
 of asphaltum. 
 
 Where the line between the townships of Ashfield and Colborne meets 
 the lake, a little south of Port Albert, on the Ashfield or Nine-mile River, Riyer 
 rocks come from beneath the high clay cliffs which face the water, and 
 
 406, 407. LAMELLIBRANCHIATA. 
 
 406 b 
 
 406. Conocardium trigonale (Conrad); a, side view; b, view of the ante- 
 rior extremity. 
 407. Vanuxemia Tomkinsi (Billings) ; a, side view ; 6, posterior view. 
 
 are seen at intervals along the shore, for about a mile. The greatest 
 section here exposed does not afford a vertical thickness of more than 
 six feet. The rocks resemble a part of those of Point Douglas : they are 
 destitute of fossils, and consist, in ascending order, of grey calcareous and 
 bituminous sandstones, cherty limestones, brown calcareous beds striped 
 with thin bituminous shales, and pale yellowish dolomitic layers, sometimes 
 three feet thick : marked by lenticular crystals of calcite, or by cavities 
 from which such crystals have disappeared. At the falls of the Ashfield 
 River, about a quarter of a mile above Port Albert, there is exposed a 
 
376 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. XIV. 
 
 series of thick bedded dark grey calcareous sandstones, with buff colored 
 silicious limestones, both holding organic remains, which are more numer- 
 ous in the latter ; the most abundant species being Spirifera bimesialis. 
 These fossiliferous beds, like those at Point Douglas, probably overlie the 
 unfossiliferous strata. 
 
 On the Maitland River, about four miles in a direct line from the shore 
 of Lake Huron, there occurs on the first lot of the first range of Col- 
 borne, an exposure of yellowish-drab limestone, holding among its fossils 
 Favosites G-oihlandica, F. polymorpha, Zaphrentis prolifica, Stropho- 
 
 408, 409. GASTEROPODA. 
 408 
 
 409 a 
 
 409 & 
 
 4Q8.Loxonema Cotterana (Billings). 
 4W.Euomphalus De Cewi (Billings) ; a, front viewi; & > 
 of the umbilicus. 
 
 mena rhomboidalis, 8. incequistriata, S. ampla, an undetermined species 
 of Orthis, Spirifera gregaria, S. bimesialis, Athyris Maia, Atrypa reti- 
 cularis, Avicula deeussata, iMcina elliptica, and PTiacops bufo. Beds 
 Godench. similar to those seen on the coast and the river near Port Albert, and 
 probably a continuation of them, occur in a cliff lower down on the Mait- 
 land, near Goderich. The following is a descending section of them : 
 
 Ft. in. Ft. in. 
 
 1. Dark grey thin bedded bituminous limestones, holding organic re- 
 mains ; with epsomites between two of the beds. Among the 
 fossils are Favosites Gothlandica, Zaphrentis prolifica, Stropho- 
 mena inequistriata, S. rhomboidalis, Spirifera gregaria, Jlthyris 
 Clara, Jltrypa reticularis, and Lucina elliptica, 
 
 24 
 
CHAP. XIV.] CORNIFEROUS FORMATION. 377 
 
 Ft. in. Ft. in. 
 
 2. Measures concealed by clay and debris, 12 
 
 3. Pale grey or drab fine grained sandstone, marked with ferruginous 
 
 spots and stripes, and mottled with blue and yellowish colors ; 
 
 no fossils appear, 2 
 
 4. Brownish calcspar, an aggregation of irregular crystals arranged 
 
 in a bed, 1 
 
 5. Dark brown fine grained sandstone, striped with bituminous layers ; 
 
 the rock is very soft and easily disintegrated, until after ex- 
 posure to the air, when it becomes hard, 2 6 
 
 16 7 
 
 40 7 
 
 At the bridge across the Maitland River, about half a mile from the 
 town of Goderich, and at a short distance below the place where the above 
 section was measured, the following unfossiliferous beds are found exposed 
 in a continuation of the same cliff. Four feet of dark grey bituminous and 
 gilicious limestone, followed by two feet of brecciated beds, are seen, which 
 probably correspond to a portion of the measures, 2, concealed above. 
 To these succeed 
 
 Ft. in. 
 
 3. Pale yellowish calcareous sandstone, with ferruginous stripes and spots, 1 10 
 
 4. Brownish calcspar, an aggregation of irregular crystals arranged in a 
 
 bed, 6 
 
 5. Yellowish sandstone, with bituminous and ferruginous spots, 3 
 
 6. Dark grey or brownish bituminous dolomite, with small lenticular crys- 
 
 tals of calcspar ; some beds contain a large quantity of chert, and 
 
 thin partings of bituminous shale, 4 
 
 There is little doubt that the fossiliferous beds in all these various 
 exposures, from Fort Douglas, belong to the Corniferous formation; while 
 the lower non-fossiliferous strata bear a strong resemblance, in their mineral 
 character and general aspect, to the Water-lime series. Their arrange- 
 ment shows that we have here one of the minor undulations, to which 
 allusion has been made. 
 
 In the south-western area, which includes the region between the lakes south-west- 
 Erie and St. Clair, the Corniferous limestones appear to become somewhat er 
 lighter in color, and more granular in texture, than they are to the east. 
 In this respect, they approach in character to the rocks of the same 
 formation in Ohio, and others of the western states of the American 
 Union. A section of about twelve feet of the formation is displayed st. Mary, 
 on the banks of the north branch of the Thames, at the village of 
 St. Mary, between the sixteenth and eighteenth ranges of Blanchard. 
 The rock is exposed for about a mile and a half above, and for the 
 same distance below the bridge, which here crosses the river. Its color 
 
378 GEOLOGY OF CANADA. [CHAP. XIV. 
 
 is a light drab, occasionally weathering to a greenish tinge ; it is very 
 bituminous, and holds numerous fossils. Among these are Favosites G-oth- 
 landica, F. hemispherica, F. polymorpha, Zaphrentis prolifica, Stroph- 
 omena rhomboidalis, S. demissa, S. incequistriata, S. ampla, an unde- 
 scribed species of Orthis, with two or three of Chonetes ; Spirifera bimesialis, 
 and fragments of a large undetermined species of this genus with very 
 numerous ribs ; Cyrtena rostrata, Athyris Maia, Atrypa reticularis, Lucina 
 elliptica, Vanuxemia Tomkinsi^ an undetermined species of Avicula, with 
 two or three others of lamellibranchiate shells, three or four undetermined 
 species of Orthoceras, Phacops bufo, and the remains of fish. 
 
 Maiden. At Maiden, near Amherstburg, which is upwards of a hundred miles to 
 
 the westward of St. Mary, the limestones of the formation are whitish- 
 grey and sometimes light buff, and some of the beds are granular. The 
 fossils which they contain are Favosites G-othlandica, F. hemispherica, 
 F. polymorpha, Syringopora Hisingeri, Michelinia convexa, Zaphrenti* 
 prolifica, Strophomena rhomboidalis, S. incequistriata, S. demissa, S. per- 
 plana, S. ampla, an undetermined Orthis, Spirifera fimbriata, S. vari- 
 cosa, Athyris Clara, Atrypa reticularis, iMcina elliptica, Oonocardium 
 trigonale, Phacops bufo, Phillipsia crassimarginata, with an undeter- 
 mined Orthoceras, and the remains of fish. These beds yield a very fine 
 building stone at Maiden, where they are extensively quarried : the beds 
 are from one to two feet in thickness, and nearly flat. For a consid- 
 erable space in the neighborhood, they are seldom covered by more than 
 two or three feet of soil, and in some parts are seen at the very surface. 
 At the base of some of the sections at Maiden, there is a compact layer 
 of a buff color, somewhat resembling lithographic stone in appearance ; but 
 for lithographic purposes it seems to be too brittle. All of these beds burn 
 to good lime. 
 
 on-bearing The limestones of this formation are all more or less bituminous, and 
 bitumen exists in many of them in a liquid form, as petroleum or rock oil, 
 filling the cells of the corals and other fossils. The corals often prevail 
 in distinct bands, some of which will be saturated with the oil, while 
 those above and below will have little or none. In working Mr. Horn's 
 quarry, which has already been mentioned, on the thirteenth lot of the 
 second range of Bertie, the oil is seen to impregnate particular beds, 
 which are in great part made up of the remains of a species of Heliophylr 
 lum. These corals, in various attitudes, are arranged in bands varying 
 in breadth from three to six inches ; and in their open cells, the petroleum 
 is lodged. The intermediate parts of the rock, which contain no oil, are 
 composed of a mass of broken organic remains, chiefly encrinites ; while in 
 the coral-bearing beds, these comminuted crinoids serve as a paste to fill up 
 the interstices among the corals. 
 
CHAP. XIV.] CORNIFEROUS FORMATION. 379 
 
 The petroleum springs which rise from this formation in Tilsonburgh, Petroleum 
 probably have their origin in such bituminous beds ; and other springs *?**& 
 of the same character, which issue in Enniskillen from strata above 
 the Corniferous, very probably ascend, through these newer rocks, from 
 the same formation. Some of thefce springs appear to be on the line of 
 the great anticlinal, which runs through the western peninsula ; and sub- 
 ordinate undulations of a similar character will be found connected with 
 others. The oil being lighter than water, and permeating with it the strata, 
 naturally rises to the highest part, which is the crown of the anticlinal ; 
 whence it escapes to the surface by some of those cracks which are usually 
 found in such positions. These petroleum springs, by the aid of wells 
 and artificial borings, have been found to yield a very large supply ; and the 
 uses of the oil having been greatly extended by recently discovered modes 
 of refining it, a new industry, to be noticed in a separate chapter, has 
 arisen in Western Canada and other places where petroleum springs occur. 
 
 It will be observed, that the positions of these anticlinal forms in Wes- undulations, 
 tern Canada thus become a matter of economic importance. The general 
 course of the main anticlinal can be readily traced by means of the 
 distribution of the formations. It would appear that the crown of the 
 arch runs in a gentle curve, from the western extremity of Lake Ontario, 
 by Woodstock ; in the neighborhood of which, the base of the Corniferous 
 formation folds over it. Proceeding thence by the Thames, in the general 
 bearing of the Great Western railway, it would reach the town of Chatham, 
 and then pass to Pigeon Bay on Lake Erie. The springs of Enniskillen 
 would appear to be north of this axis, and they may probably be on a subor- 
 dinate one parallel with it ; which may be connected with the undula- 
 tion that has already been mentioned as affecting the outcrop of the 
 Guelph formation at Rockwood. Small undulations in the Corniferous forma- 
 tion, are observable at several places in that part of its distribution which 
 borders on Lake Erie, from the Niagara River to the township of Windham. 
 Two of these are indicated by curves in the outcrop of the base ; one of 
 them, already alluded to, near Point Abino, and another obliquely crossing 
 the Welland Canal in the second range of Humberstone : the course of 
 both is probably about south-west. Opposite dips in some of the exposures of 
 the strata, indicate other undulations. One of these occurs on the thirteenth 
 lot of the first range of Rainham, where the direction of the undulation is 
 nearly north-west ; and another is shown in the large exposure of Oris- 
 kany sandstone on the town line between Oneida and North Cayuga, 
 where the axis of the undulation is about south-west. 
 
380 GEOLOGY OF CANADA. [CHAP. 
 
 CHAPTER XV. 
 
 THE HAMILTON FORMATION AND THE PORTAGE AND CHEMUNG GROUP. 
 
 UPPER DEVONIAN ROCKS IN NEW YORK. MARCELLUS SLATE. HAMILTON GROUP. TULLY 
 LIMESTONE. GENESEE SLATE. PORTAGE GROUP. CHEMUNG GROUP. HAMILTON FORMA- 
 TION IN WESTERN CANADA; ITS DISTRIBUTION. BLACK SHALES BELONGING TO THE BASE 
 OP THE PORTAGE GROUP; THEIR DISTRIBUTION IN WESTERN CANADA. DEVONIAN ROCKS 
 OF MICHIGAN AND NEW YORK. 
 
 In the state of New York, the Corniferous limestones are succeeded by 
 
 a series of shales, limestones, and sandstones, which are designated in 
 
 ascending order as follows: 1, Marcellus shales; 2, Hamilton group; 3, 
 
 Tully limestone ; 4, Genesee slates ; 5, Portage or Nunda group ; and 6, 
 
 Upper Devo- Chemung group. These together make up the Erie division of the New 
 
 nian strata. York geologists, which is regarded as the summit of the Devonian system ; 
 
 and are followed, in that state, by the Catskill group of sandstones, which 
 
 are considered as the base of the Carboniferous system. 
 
 The Marcellus shale is described as a black or brown bituminous shale 
 or pyroschist, often pyritiferous, and very much resembling that of the 
 Utica formation. The lower portion contains thin layers of dark colored 
 impure fossiliferous limestone, and concretionary calcareous masses, which 
 have the internal structure of septaria. In the upper part, the shales are 
 destitute of organic remains, and lighter in color ; becoming olive-grey, 
 and passing into the succeeding formation. The black color of these 
 lower shales formerly led to explorations for coal in this formation ; and 
 the borings then made, show that its greatest thickness, which is towards 
 the Hudson River, may be one hundred feet ; while to the westward, in 
 which direction it has been traced to Lake Erie, it does not exceed half 
 that volume. 
 
 Hamilton The Hamilton group in New York, consists of a series of olive-colored or 
 
 group. bluish calcareo-arenaceous and argillaceous shales, weathering to ash-grey 
 
 or brown. In its eastern distribution, some beds of sandstone occur, near 
 the middle of the series ; while to the westward, it becomes more argilla- 
 ceous, and includes a band of encrinal limestone, besides layers of septaria. 
 Towards the east, it is said to resemble the Hudson River formation, and 
 to have a thickness of from 300 to 700, and even 1000 feet ; while to the 
 
CHAP. XV.] HAMILTON FORMATION. 381 
 
 west, it presents the characters of the shales at the base of the Niagara 
 formation, and has a thickness of a little more than 200 feet. This, 
 according to Mr. Hall, consists, in ascending order, of- 
 
 Feet. 
 
 Olive shales, with Pterinea, Cypricardia, and Strophomena,* 80 
 
 Coarse grained shales, with numerous fucoids, and with a hard calcareous 
 
 s tratum at the top, 40 
 
 Bluish and greyish-blue very fissile shales, with large numbers of dtrypa, 
 
 Orthis, Spirifera, and Strophomena, 90 
 
 210 
 
 To this succeeds the Tully limestone; a blackish-blue concretionary 
 fossiliferous stratum, which has a thickness of twenty feet, in the eastern 
 part of New York, but thins out westward, and disappears before reaching 
 Lake Erie. 
 
 The Genesee slates consist of black bituminous shales, so like those of Genesee 
 the Marcellus division that it is difficult to distinguish them, without the 6l 
 aid of fossils. They exfoliate where their edges are exposed to the 
 weather; but retain their black color, except in those portions where 
 pyrites occurs. These shales are interstratified with occasional bands of 
 flagstones, and include septaria, some of which contain petroleum and a 
 white crystalline hydro-carbon, while others hold crystallized selenite, cal- 
 cite, and quartz. The upper part of these strata contains a few fossils. 
 The Genesee slates extend from Chenango county to Lake Erie. Towards 
 the east, they attain a thickness of from 100 to 150, and even, according 
 to Emmons, of 400 feet ; but to the westward, according to Mr. Hall, 
 their volume is reduced to about twenty-four feet. 
 
 The Portage group consists, in ascending order, of: 1, A shaly sand- Portage 
 stone, in the eastern and middle parts of the state ; becoming, to the west- group< 
 ward, a series of greenish crumbling shales ; within which, at eight feet 
 from the base, is included a band of black shale, like the Genesee slate. 
 From a thickness of one hundred and ten feet, hi the east, these strata are 
 reduced to thirty-three feet, on Lake Erie. 2, A series of beds, which, to 
 the eastward, are chiefly sandstones ; but, towards Lake Erie, present an 
 alternation of black and green sandy shales, with thin sandstone layers. 
 Farther west, they consist of a thick mass of black shales, followed by 
 several hundred feet of alternating green and black shales, without sand- 
 stones. 3, Soft thin bedded sandstones below, followed by thick massive 
 layers above. The total thickness of this group is estimated by Mr. Hall 
 at 1400 feet. Casts of shrinkage cracks, mud furrows, and lines of flow, 
 mark the surface of the sandstone beds ; and the structure called cone-in- 
 cone occurs in the argillaceous ones. Fucoids abound in the group, 
 Fucoides grapUca characterizing the lower, and F. verticalis, the upper 
 portion. In addition to these, fossils of the following genera occur: 
 
382 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XV. 
 
 Chemung 
 group. 
 
 CyathocrinuS) Orthis, Spirifera, Avicula, Ambonychia, Cardmm, As- 
 tarte, Lucina, Nucula, BeUerophon, Ungulina, Orihoceras, Clymenia, 
 and Croniatites. 
 
 The Chemung group consists at the base of olive shaly sandstones, fol- 
 lowed by black slaty shales, with septaria. To these succeed green shales, 
 with grey sandstones, supporting grey and olive shales and shaly sand- 
 stones ; the proportion of the softer and harder masses varying in different 
 places. The greatest thickness of the group is said to be about 1500 feet, 
 diminishing gradually from south-eastward to north-westward. It is well 
 characterized by its fossils, which are abundant, and consist chiefly of 
 brachiopoda and acephala. A few species of land plants occur in this 
 formation, belonging to the genera Sigillaria^ Stephanopteris, and 
 Plumalia. The other fossils belong to the genera Orthis, Rhynchonella, 
 Strophodonta (Strophomena) , Spirifera, Athyris, Atrypa, Avicula- 
 pecten, Pteronitis, and Phacops. 
 
 HamUton 
 formation. 
 
 Bosanquet. 
 
 THE HAMILTON FORMATION. 
 
 In the western part of Canada, we have not been able to distinguish 
 either the Marcellus shales, or the Tully limestones, from the Hamilton 
 group; and we shall therefore, in describing the rocks of that region, 
 include under the name of the Hamilton formation, all the strata between 
 the Corniferous limestones and the Genesee shales. This formation occu- 
 pies the lowest portion of the saddle-shaped depression, noticed in the pre- 
 vious chapter, as crossing the peninsula from Lake Erie to Lake Huron, 
 and separating the Corniferous formation into two areas. The space thus 
 occupied is very much covered by drift, and the contact between the 
 Corniferous and Hamilton formations, has not yet been seen ; so that it is 
 not easy to assign their precise stratigraphical place to the exposures 
 which are met with. 
 
 On the twenty-third, twenty-sixth, and intermediate lots of the third 
 range of Bosanquet, exposures of the rock are met with, on the banks of a 
 small tributary of the Riviere aux Sables (south) . The following section in 
 
 ascending order was measured on the twenty-fifth lot : 
 
 Ft. in. 
 Grey calcareous shale, imperfectly seen in a slope or talus on the stream,. . 25 
 
 Grey calcareous shale with Spirifera mucronala and other fossils, 4 
 
 Grey solid limestone composed of broken remains of encrinites, 2 
 
 Grey soft shales, thinly laminated next the limestone, and filled with fossils, 
 among which Cystiphyllwn Americanum is very abundant. The upper 
 
 part has the softness of clay, 20 
 
 Grey decomposing shale not well exposed, 80 
 
 Grey encrinal limestone, weathering into small lenticular fragments, and 
 
 holding bivalve shells, corals, and encrinites, 2 
 
 133 
 
CHAP. XV.] 
 
 HAMILTON FORMATION. 
 
 383 
 
 This section probably includes the strata of the neighboring exposures. 
 The fossils obtained from the whole of these are Favosites Grothlandica, F. 
 turbinata, F. polymorpha, Cystiphyllum Americanum, Pentremites Hoe- 
 meri, Strophomena ampla, /S. convexa, S. lepida, Orfhis Vanuxemi, 0. 
 perversa, Rhynchonella Laura, Spirifera mucronata, Cyrtia Hamilton- 
 ensis, Aihyris concentrica, Charionella rostrata, Retzia Chloe, Atrypa 
 
 410. Striatopora Linnceana (Billings). 
 
 411. Trachypora elegantula (Billings) ; fl, 6, portions of two corallites ; 
 
 longitudinal section; </, portion of a corallite enlarged. 
 412. Diphyphyllum Jlrchiacl (Billings). 
 413. Mveolites Fischeri (Billings). 
 GoMfussi (Billings). 
 
 reticularis I/ticina elliptica, Pleurotomaria 
 
 an undetermined 
 
 Orthoceras, and Phacops lufo ; with an undetermined Dalmanites. 
 
 At Jones's mill, on the third lot, upon the south boundary of Bosanquet, 
 on the bank of another small tributary of the Riviere aux Sables (south), 
 
 the following ascending section is exposed : 
 
 Ft.in. 
 Brownish grey-weathering shales, holding Spirifera mucronata in great 
 
 abundance, and a few other bivalves and corals, 25 
 
 Grey encrinal limestone, 2 
 
 Grey decomposing shale with Cystiphyllum Jlmericanum, 3 
 
 30 
 
384 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XV. 
 
 In addition to the fossils named, which are the most abundant, these 
 strata contain Favosites G-othlandica, Zaphrentis prolifica, Heliophyllum 
 i) Strophomena incequistriata, and an undetermined Chonetes. 
 
 415-418. BRAOHIOPODA. 
 
 415. Cyrtia Hamiltonensis (Hall) ; a, ventral, 6, side, and c, dorsal 
 
 view. 
 416. Jltrypa reticularis (Linnaeus) ; a, coarse-ribbed variety ; &, and c, 
 
 common form. 
 
 41 7. Orthis Vanuxemi (Billings) ; a, ventral, &, side, and c, dorsal view. 
 418. Rhynchonella? Laura (Billings); a, dorsal, 6, side, and c, ventral 
 
 view. 
 
 At Austin's mill on the fourth lot of the first range of the same town- 
 ship, on another small stream, there is a corresponding section, where the 
 grey encrinal limestone which forms the uppermost layer of the exposed 
 strata, is five feet thick. Below this band, the strata are characterized, as 
 
CHAP. XV.] 
 
 HAMILTON FORMATION. 
 
 385 
 
 before, by a great abundance of Spirifera mucronata; and in the bed of 
 the stream, at a level of probably fifty or sixty feet below the encrinal 
 limestone, there is a band of solid arenaceous limestone, about seven inches 
 thick. This is underlaid by black shales, holding Strophomena incequi- 
 striata, Atrypa reticularis, and an undetermined Chonetes. These black 
 shales may possibly indicate the passage, which occurs in New York, 
 between the Marcellus and the Hamilton shales. 
 
 A series of beds, which are probably higher than those in the third 
 range, is met with on the twenty-fifth lot of the fifth range of Bosanquet. 
 They consist chiefly of grey decomposing shales, and may have a thickness 
 of thirty feet. The fossils which they contain are Favosites G-othlandica, 
 F. turUnata, F. polymorpha, F. cervicornis, F. hemispherica, Alveolites 
 
 419-421. BRACHIOPODA. 
 
 419 
 
 419. Retzia ChloS (Billings) ; a, ventral, b, side, and e, dorsal view. 
 420. Charionella rostrata (Hall) ; a, side,, and b, dorsal view. 
 421. Spirigera concentrica (Von Buch) ; a, dorsal, fe, side, and c, ventral 
 view. 
 
 Eoemeri, A. Fischeri, A. G-oldfussi, Trachypora elegantula, T^ irregu- 
 laris, Striatopora Linnceana, Diphyphyllum Archiaci, Zaphrentis prolif- 
 ica, Heliophyllum Halli, H. tenuiseptatum, Cystiphyllum Americanum, 
 StropJiomena ampla, S. concava, S. lepida, Spirifera mucronata, Athyris 
 concentrica, and Phacops htfo. 
 
 In the same township, near the Widder station, a cutting on the Grand widder. 
 Trunk Kailway exposes about forty feet of this formation, in horizontal 
 beds. The strata here consist of a soft scarcely indurated marl or clay, 
 with occasional intercalated beds of limestone, a few inches in thickness. 
 The whole of these beds abound in fossils, the chief of which are Spirifera 
 mucronata, Atrypa reticularis, and Spirigera concentrica; with fragments 
 of Groniatites. It is not unlikely that these clays, instead of being the 
 
386 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XV. 
 
 result of a decomposition of the shales, are sediments which have never 
 ciay beds, been hardened. Portions of the Hudson Biver formation, at Point Rich, 
 
 and of the Clinton formation, at Dundas, are in a similar condition, and 
 
 might be confounded with recent clays. 
 EnnisMiien. The oil springs of Enniskillen, which are supposed to have their source 
 
 in the Corniferous limestones, rise through the Hamilton shales, in which 
 
 422-424. BKACHIOPOD A . 
 
 422 
 
 422. Spirifera Parry ana (Hall) ; a, dorsal, and b, side view. 
 
 423. S. sculptilis (Hall). 
 
 424. S. mucronata (Conrad) ; a, long- winged variety ; 6, c, 
 
 and d, different views of the short-winged form. 
 
 Oil weiis. numerous wells and borings have been sunk, to various depths. These, 
 meeting with fissures, connected probably with anticlinals, bring to the 
 surface large quantities of petroleum ; often accompanied by inflammable 
 gas and saline waters. Three of these wells have been sunk in the adja- 
 cent corners of the thirteenth and fourteenth lots of the tenth and eleventh 
 ranges of the township, and, after passing through fifty or sixty feet of 
 drift, reach the rock beneath. In one of the borings, according to the 
 account given, there were met with, thirty-eight feet of limestone or sand- 
 stone layers, alternating with soft shale or clay; succeeded by 162 feet of 
 
CHAP. XV.] PORTAGE AND CHEMUNG GROUP. 337 
 
 similar soft clays, beneath which was a limestone, which may belong to 
 the summit of the Corniferous formation. In two other borings, the soft 
 rock appears to have been met with immediately beneath the drift, and 
 was penetrated to depths of 182 and 190 feet, before reaching the 
 limestone. 
 
 A boring on the seventeenth lot of the third range, beneath sixty feet 
 of drift, passes through thirty-eight feet of alternating hard and soft 
 strata, and then 117 feet of soft shale. Below this, a harder bed was met 
 with, which was called by the workmen a sandstone, and may be some 
 arenaceous layer overlying the lower limestone. Another boring, on the 
 thirteenth lot of the sixth range, beneath sixty feet of drift, penetrates 
 224 feet of soft shale, without meeting with the limestone beneath. It xttai thickness, 
 thus appears that there is a great mass of soft shale in the lower part 
 of the Hamilton formation, reaching in some places a thickness of nearly 
 230 feet ; and it would perhaps be quite safe to estimate the whole volume 
 of the formation at about 300 feet. 
 
 THE PORTAGE AND CHEMUNG GROUP. 
 
 Of the higher members of the Devonian series of New York, the Gen- 
 esee slates are regarded by Mr. Hall, as forming a lower member of the 
 Portage group ; the sandstones of which, as we have already said, are 
 interstratified, at their base, with similar black shales. We may, for con- 
 venience, unite the Chemung sandstones with those of the Portage series 
 and their underlying black shales, under the name of the Portage and 
 Chemung group. The strata of this group are wanting in Western Can- 
 ada, with the exception of some portions of black bituminous shale, which 
 are supposed to represent the Genesee slates. These black shales are 
 met with at Cape Ipperwash, or Kettle Point, in Bosanquet, on Lake Kettle Point 
 Huron. Here, in a low cliff, on the west side of the cape, is a section of st 
 between twelve and fourteen feet of very fissile black bituminous shales, 
 weathering to a leaden-grey, and often stained brown by oxyd of iron. A 
 yellow earthy coating of oxalate of iron is sometimes found in the surfaces 
 of the shales, which also contain nodules and crystals of iron pyrites ; 
 besides peculiar spheroidal concretions, whose fancied resemblance to 
 inverted kettles has probably given its name to the point. They vary in size, 
 from three inches to as many feet in diameter, and are sometimes nearly 
 spherical, and at others somewhat flattened, generally on the under side. 
 Occasionally a smaller spheroidal mass is implanted on the top of a larger 
 one. These concretions are readily broken, and are then seen to be com- 
 posed of brown crystalline carbonate of lime ; which is confusedly aggre- 
 
388 GEOLOGY OF CANADA. [CHAP. XV. 
 
 gated in the centre, and sometimes contains blende. Around this, are 
 arranged slender prismatic crystals, which extend from the nucleus to the 
 circumference ; the whole having a radiated columnar structure, which, 
 not less than the terminations of the prisms, at the surface of the sphe- 
 roidal masses, gives them very much the aspect of fossil corals. 
 
 On the east side of the point, the upper beds of the section are con- 
 cealed ; but the lower ones come from beneath the bank, at a little above 
 the water's level, and cover an area of several acres ; the whole surface 
 being studded with these spheroidal concretions, which remain when the 
 softer shale around them has been partially worn away. 
 
 Fossil plants. This black shale is fossiliferous, and contains a fucoid resembling a 
 variety of the Fucoides cauda-galli of Vanuxem, which is very abundant 
 in the lower beds. Flattened stems of Oalamites inornatus (Dawson), 
 which are sometimes seven or eight feet long, and three inches wide, 
 occur about the middle of the section, and are occasionally converted into 
 coal. Besides these, according to Dr. Dawson, there occurs here a stem 
 which belongs to Sagenaria Veltheimiana (Goeppert). An undetermined 
 Lingula is found with these plants, together with numbers of what appear 
 to be microscopic orbicular shells. 
 
 These shales contain so much organic matter, as to take fire and 
 burn with flame, after which the color is changed to brick-red. This is 
 observed in the shingle of the beach, which has evidently been subjected 
 to fire ; and it is reported by the Indians, to have continued burning for 
 a long time. These black shales have also been observed on a branch 
 of Bear Creek, near Kingston Mills, on the seventh lot of the third range 
 of Warwick. There, as at Kettle Point, the spheroidal concretions of 
 carbonate of lime are met with, but the only fossils observed are some 
 rather obscure scales of fishes. It is probable that this outcrop may have 
 a connection with that on the lake shore ; but a third exposure of the 
 shales, with their characteristic concretions, which occurs at Branon's 
 mills, on the twentieth lot of the seventh range of Brooke, in the bed of 
 the east branch of Bear Creek, may perhaps belong to an outlying por- 
 tion. It is not improbable that another portion of these same shales may 
 underlie the drift, to the south side of the anticlinal, on the shore of Lake 
 Erie ; but no exposures of them have as yet been seen in that region. 
 
 The black color and inflammable properties of these black shales, as in 
 the case of the similar shales of the Utica formation, have suggested to 
 many persons the probability of beds of coal in their vicinity. Between 
 these highest shales, however, and the horizon of the true coal measures, 
 
 Devonian in in the southern peninsula of Michigan, where these measures are nearest, 
 there is wanting, in Western Canada, the remaining portion of the Portage 
 and Chemung group ; which, in Michigan, according to Prof. Winchell, 
 attains a thickness of 363 feet, and in some parts contains native copper. 
 
CHAP. XV.] PORTAGE AND CHEMUNG GROUP. 389 
 
 Following this, we have there what has been named the Napoleon group, 
 of 123 feet of sandstones, often saliferous ; to which succeeds the Mich- 
 igan Salt group, of 184 feet ; consisting, like the Onondaga formation, of 
 marls, dolomites, and beds of gypsum, and yielding brine springs of great 
 strength and purity. To this succeed 66 feet of Carboniferous limestone, 
 and 105 feet of sandstone ; making in all 840 feet, before attaining the 
 coal measures of Michigan, on the western side of Lake Huron.* (Report 
 on the Geology of Michigan, 1861.) 
 
 To the south of Lake Erie, in New York, the thickness of the strata, 
 from the Genesee slates to the coal measures of Pennsylvania, is vastly 
 greater. The Portage and Chemung sandstones have a thickness of 2000 
 feet; which increases to 3000, farther to the eastward. These are over- Devonian in 
 laid by the sandstones, shales, and conglomerates of the Catskill moun- NewYork - 
 tains ; which, on the west side of the Hudson River, rise to a height of 
 3800 feet, and correspond to at least 3000 feet of strata, overlying the 
 Devonian series. Above the coarse conglomerate which forms the sum- 
 mit of the Catskill group, we find, along the line of the Appalachians, 
 in Pennsylvania, a series of red shales, with calcareous bands, amount- 
 ing to 3000 feet more, and succeeded by another conglomerate ; which, 
 in that region, lies at the base of the coal measures, and is said to have a 
 thickness of 1400 feet. We have thus, above the Hamilton formation and 
 its overlying black shales, a thickness of more than 10,000 feet of silicious 
 and argillaceous rocks, before reaching the coal measures of the Appala- 
 chian field. This great thickness is, as we have seen, represented by 
 less than 800 feet in the Michigan coal field, where it includes 65 feet 
 of what is called the Carboniferous limestone. This calcareous formation 
 is wanting in Northern Pennsylvania, but it appears at the base of the 
 conglomerate farther south ; and gradually augmenting to the westward, 
 becomes the great Carboniferous limestone series of the Mississippi valley ; 
 where fossiliferous limestones, with occasional sandstones, appear to repre- 
 sent the 7400 feet of sediments, which, in New York and Pennsylvania, 
 overlie the Devonian series. (Hall's Palaeontology, Vol. III., Introduction.) 
 We find, in Gaspe*, a great series of sandstones and conglomerates, which 
 there succeed to the Upper Silurian limestones, and are supposed to repre- 
 sent the Devonian strata of the New York series. The succeeding Bona- 
 venture formation belongs to the base of the Carboniferous system. 
 
 * As a farther illustration of the thin- of the Trenton group, at only 2500 feet, 
 ning out of the palasozoic rocks to the The latter rests upon the Ste. Marie sand- 
 westward, so often alluded to, we may gtones. This, as we have shown, belongs to 
 mention that Winchell estimates the entire the Upper Copper-bearing series of Lake 
 thickness of the series in Michigan, from Superior, which corresponds to the Que- 
 the top of the coal formation to the base bee (or Calciferous) and Potsdam groups. 
 
390 GEOLOGY OF CANADA. [CHAP. XVI. 
 
 CHAPTER XVI. 
 
 THE GASPfi LIMESTONES AND SANDSTONES, AND THE BONA VENTURE 
 
 FORMATION. 
 
 THB GASPE LIMESTONES, OP MIDDLE AND UPPER SlLUXUAN AGE. THE GASPE SANDSTONES, 
 CHIEFLY DEVONIAN. THE BONA VENTURE SANDSTONES AND CONGLOMERATES, OF THE CAB- 
 SONIFEROUS SYSTEM. DISTRIBUTION OF THESE GROUPS IN GASPE. CHATTE AND CASCA- 
 PEDIA SECTION; MATANNE SECTION; MATAPEDIA SECTION; METIS AND PATAPEDIA SECTION; 
 LAKE TEMISCOUATA AND MADAWASKA SECTION; SECTION ON THE ST. JOHN, ST. FRANCIS, 
 AND BLACK EIVERS; CHAUDIERE SECTION; SECTION ON THE ST. FRANCIS AND SOME OF 
 
 ITS TRIBUTARIES. LAKES AYLMEH AND MEGANTIC ; LAKE MEMPHRAMAGOG. DEVONIAK 
 LIMESTONES. COAST SECTION OF THE BAY OF CHALEUR8. MIDDLE SILURIAN LIMESTONES. 
 
 BONA VENTURE FORMATION; ITS RELATION TO THE COAL OF NEW BRUNSWICK. 
 
 In describing the Anticosti and Lower Helderberg groups, we have 
 already alluded to their existence in Gaspe*, where they appear as a series 
 of limestones. Mention was also made, at the close of the last chapter, 
 of a great mass of Devonian and Carboniferous strata in Gaspe* : these, 
 so far as examined, are chiefly sandstones and conglomerates. To the 
 south-west, however, on the Famine River, and on lakes St. Francis and 
 Memphramagog, fossiliferous limestones are met with, apparently of Devon- 
 ian age. The true relations of these various rocks and their subdivisions, 
 are as yet but very imperfectly made out ; but we propose to give, in the 
 present chapter, the facts which, up to the present time, have been observed, 
 with regard to their characters and their distribution, from Gaspe*, south- 
 westward, to the boundary of the province. 
 
 THE GASPlS LIMESTONES. 
 
 On the south side of the St. Lawrence, in the counties of Gaspe* and 
 Rimouski, the rocks of the Quebec group are unconformably overlaid by 
 a series of calcareous strata, which we have been accustomed to call the 
 Gaspe* limestones : full details with regard to them have, however, not yet 
 been ascertained. On the Chatte and Matanne Rivers, on Lake Matapedia, 
 
OHAP. XVI.] GASPfi LIMESTONES. 391 
 
 and on the rivers Metis and Rimouski, the lower portion of this series of 
 limestones appears to belong to the Anticosti group. It is as yet uncertain 
 how far the strata of this group may extend on the strike, to the east and 
 to the west. They must, however, thin out in some part of the distance 
 of one hundred miles, which intervenes between Cape Chatte and Cape 
 Gaspe*, at the extremity of the peninsula, where they are wanting ; while 
 to the westward, it is not quite* clear that they extend beyond Temiscouata 
 Lake. The limestones met with at Cape Gaspe*, appear to be a great cape Gasps 
 development of strata of the age of the Lower Helderberg group. They 8e 
 here rest upon black shales, which are supposed to be those already 
 described as underlying the Quebec group. These limestones present the 
 following series, in ascending order : 
 
 Feet. 
 
 1. Grey limestones in layers of from six to eight inches thick, which are Limestones. 
 
 separated by bands of greenish calcareo-argillaceous shale, gradually 
 increasing in amount towards the upper part. The limestone beds 
 abound with fossils, and contain, among other species, large crinoidal 
 columns, Favosites Gothlandica, F. basaltica, F. cervicornis, with 
 undetermined species of Zaphrentis, Dictyonema, and Fenestella, two 
 undetermined species each of Lucina and Strophomena, with S. rhom- 
 boidalis, S, punctulifera, two or three undetermined species of Orthis, 
 Rhynchonella acutiplicata, two or three species of Orthis, Pentamerus 
 galeatus, three undetermined species of Spirifera, Athyris Icevis, Atrypa 
 reticularis, Cyrtodonta orbicularis, C. lata, C. flexuosa } Modiolopsis cul- 
 trata, JLvicula Bronni, A. naviformis, Loxonema Gaspensis, L. gracilis, 
 Bellerophon Laurenticus, two undetermined species of Platyceras, an un- 
 determined Conularia, with several undetermined species of Orthoceras, 
 Dalmanites pleuroptyx, an undetermined Phacops, Bronteus Canadensis, 
 and an undetermined species of Beyrichia, 70 
 
 2. Greenish calcareo-argillaceous shales, which are interstratified with less Red and 
 
 calcareous layers, of various shades of red. The only fossils observed, green shales, 
 
 occur about the middle of the deposit, and consist of flattened stems of 
 marine plants, apparently replaced by oxyd of iron, 90 
 
 3. Olive-green calcareo-argillaceous shales, with occasional nodules and lay- 
 
 ers of compact limestone ; the former from an inch to a foot in diameter, 
 and the latter from six inches to two feet thick. Some of the layers are 
 rather arenaceous ; remains of fucoids occur at the top, 170 
 
 4. Grey limestones in thin beds, separated by grey calcareous shales, of which 
 
 there are more towards the bottom than the top. The whole mass is 
 interstratified with three or four bands of olive-green calcareo-argilla- 
 ceous shale. About fifty feet from the bottom, there is a bed of seven Corrugated 
 feet, made up of several thin layers of limestone and limestone shale, and beds, 
 presenting a singularly wrinkled structure, from which the beds above 
 and below are free. It would appear as if the layers, after their deposit, 
 had been contorted by lateral pressure, the underlying stratum remain- 
 ing undisturbed ; and had then been worn smooth, before the deposition 
 of the next bed. Where the inverted arches of the flexures occur, some 
 of the lower layers are occasionally wanting ; as if the corrugated bed 
 had been worn on the under as well as the upper side. The corrugations 
 are precisely in the direction of the dip, and the peculiarity is not con- 
 
392 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Feet. 
 
 fined to a small part of the deposit, for the same thing is observed at the 
 Petit Portage and Cape Bon Ami, the only two localities in which these 
 limestones have been observed ; these are upwards of a mile asunder. 
 The fossils of these calcareous strata are not so numerous as those of 
 the limestones at the base of the section. Among them however are 
 fucoids or compressed stems of plants, an undetermined species of Cho- 
 netes, Leptoceelia coucava, L. Jlabellites, Spirifera crispata, with undeter- 
 mined species of Conularia and Orthoceras, 200 
 
 Shales. 5. Grey or slightly greenish calcareous shales, associated with bands of dark 
 grey. Both are interstratified with layers of arenaceous limestone, which 
 are occasionally sufficiently coarse grained to approach the character of 
 a fine conglomerate. Fossils are somewhat abundant ; in addition to 
 marine plants, which are chiefly confined to long flattened serpentining 
 stems, the species which prevail are two undetermined species of Lucina, 
 and two ofLingula, Strophomena rhomb oidalis, an undetermined Chonetes, 
 Leptoceelia concava, L. Jlabellites, and Spirifera crispata, with two unde- 
 termined species of Orthoceras and one of Phacops, 380 
 
 6. Grey calcareous shales or shaly limestones, interstratified, particularly at 
 the top, with thin beds of purer limestone fit for burning. The organic 
 remains of this part, which do not appear to be abundant, are chiefly 
 obscure serpentining fucoids ; which are accompanied by species of 
 Lingula, Discina, a Conularia resembling C. Sowerbyi, and an undeter- 
 mined species of Pterygotus, 300 
 
 1210 
 
 The accompanying wood-cuts show the characters of the corrugations, in 
 four different parts of the bed of seven feet, which we have just de- 
 scribed as interstratified in the thin bedded grey limestones, 4, of the above 
 
 425. COBKUGATED LIMESTONE BEDS AT CAPE GA8PE. 
 
 Scale about ^. 
 
 section. The heavy black lines are intended to represent the limestones 
 of the bed ; and these, it will be perceived in one instance, are occasionally 
 broken up into fragments. 
 
CHAP. XVI.] GASPE LIMESTONES. 
 
 These strata dip south-west, at an angle of twenty-four degreees, and are 
 beautifully seen in the cliffs ; which present a vertical naked face nearly 700 
 feet in height, on the north-east side of Gaspe* promontory. The lowest lime- 
 stones, 1, constitute the first step in the ascent to the mountains encoun- 
 tered in passing from Cape Rosier to Grand Grve. The second hard 
 calcareous band, 4, forms another step in the same ascent ; it makes also 
 Cape Bon Ami, from which the grey calcareous shales, 5, present a steep 
 slope up to the foot of the grey shaly limestones, 6. These rise in a verti- 
 cal and sometimes overhanging escarpment, up to the edge of the precipice ; 
 from which the harder beds that form the summit of the above section, slope 
 down into a valley. This valley divides the hills of the promontory into a 
 double range, and maintains its character with some constancy, farther 
 into the interior. 
 
 From this valley, the succeeding members of the series are piled in a 
 second escarpment, and constitute the loftier of the two ranges : these 
 strata, as before, dip S. W. < 24, and are, in ascending order, as follows : 
 
 Feet. 
 
 1. Grey nodular shaly limestones, succeeded by grey limestones of a purer Limestones, 
 nature ; these are followed by a second series of beds like the first, on 
 which rest greenish calcareo-arenaceous shales, terminating in a thin 
 layer, which is nearly grass-green. A fossil strongly resembling Fucoides 
 cauda-galli, is common throughout the deposit, and some surfaces are 
 almost completely covered by it ; the only species observed accompany- 
 ing it was Dalmanites pleuroptyx, 300 
 
 8. Grey limestones fit for burning, in beds of from six to twelve inches thick, 
 some of them holding chert at the summit. Fossils abound ; among the 
 species are Fucoides cauda-galli, Favosites Gothlandica, F. basaltica, F. 
 cervicornis, two undetermined species of Zaphrentis and one of Fenestella, 
 Orthis oblata, with two or three undetermined species of this genus, 
 Strophomena rhomb oidalis, S. Secki, S. perplana, with two undetermined 
 species of Strophomena, three undetermined species of Chonetes, and two 
 of Rhynchonella, with R. acutiplicata, Leptoccelia concava, L. flabellites, 
 Eatonia peculiaris, Rensseleeria ovoides, two undetermined species of 
 Spirifera, with S. arenosa, Jltrypa reticularis, JLthyris Icevis, two unde- 
 termined species of Modiolopsis and two of Jlvicula, with undetermined 
 species of Murchisonia, Pleurotomaria, Loxonema, Orthoceras, Phacops, 
 and ProetuSj with Dalmanites pleuroptyx, 500 
 
 800 
 
 The entire volume of these Upper Silurian limestones would thus be Distribution, 
 about 2000 feet. They occupy the whole of the promontory of Cape 
 Gaspe*, which extends from the mainland for a distance of about seven 
 miles, with a breadth of no more than seven tenths of a mile ; except at 
 its junction with the low land extending to Cape Rosier, where it grad- 
 ually assumes a greater breadth. They skirt the north-east bank of the 
 north-west arm of Gaspe* Bay, and the left bank of Dartmouth River ; 
 
394 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 constituting a range of mountains, some of whose summits, according to 
 Bayfield, are about 1500 feet high. From Little Gaspe*, they are flanked 
 by a strip of the succeeding formation, the junction of the two being seen 
 in Little Gaspe* Cove. About seventeen miles above Little Gaspe*, these 
 limestones cross the north branch of the Dartmouth, upwards of two miles 
 from the mouth of the tributary ; on which a partial section, directly across 
 the measures, presents a thickness of 1800 feet. At the bottom of this, 
 there are interstratified layers of chert, which have not yet been observed 
 at Cape Gaspe*. 
 
 THE GASPE SANDSTONES. 
 
 Succeeding the calcareous rocks just described, and resting upon them 
 conformably, there occurs an important group of sandstones. The contact 
 of the two series, as already stated, is seen at Little Gaspe* ; but between 
 the visible base of the sandstone group and the place of its greatest 
 development, therfe are two considerable undulations, and a probable dislo- 
 cation, of an uncertain amount. These render it difficult as yet to unite 
 the whole series, with a certainty that no strata are repeated or left out. 
 But though the section which shows the greatest unbroken series of strata, 
 does not reach to the base, it is probably not far removed from it ; and it 
 may therefore, for the present, be assumed, probably without much inaccu- 
 racy, to represent the whole group. In ascending order, the strata are 
 as follows : 
 
 Shales. 1. Grey arenaceous and argillaceous shales, with beds of grey sand- 
 
 stone, varying in thickness from one to twenty feet, and one of them 
 seventy-five feet. A three-inch band of argillaceous iron ore occurs 
 about a hundred feet from the top. Towards the bottom, the beds 
 weather of a rusty brown color, and contain abundance of plants. 
 
 Fossil plants. One of these, in its arrangement on the surface of the beds, resembles 
 
 Fucoides graphica, but it may be the broken roots or stems of the 
 other species of plants, which have been recognized in this de- 
 posit; surfaces thus characterized were met with in more than one 
 locality. Many of the beds abound with the comminuted remains 
 of carbonized plants, most of which are too obscure to be deter- 
 mined. Among them, however, are Prototaxites Logani, Lepido- 
 dendron Gaspianum, Psilophyton princeps, P. robustius, Selaginites 
 formosus, and Cordaites angustifolia ; all described by Dr. Dawson. 
 
 Coal seam. Towards the lower part, there is a small seam of coal, with carbon- 
 
 aceous shale, measuring together about three inches ; which appears 
 to hold a regular course, having a bed of clay beneath, marked by 
 what seem to be the roots of Psilophyton ; while the stems and leaflets 
 of the plant are met with in a thin seam of shale above the coal, 
 and in the carbonaceous shale associated with it. On some of the 
 
CHAP. XVI.] GASP& SANDSTONES. 395 
 
 Feet. Feet. 
 
 leaflets, small shells of the genus Spirorbis are met with. More 
 than 130 feet above the coal seam, there is a hard rough grey bed, 
 looking like fire-clay ; with the fibrous impressions of Psilophyton 
 roots penetrating it at right angles. Ripple-mark occurs on some 
 of the surfaces, 528 
 
 2. Drab sandstones, many of them with a reddish tinge ; they present Sandstones. 
 
 spheroidal masses harder than the general character of the rock, and 
 
 are marked by extensive ferruginous stains. A few scattered pebbles 
 
 of quartz and jasper occur in some of the beds, which are in general 
 
 thick, and separated from one another by layers and partings of grey 
 
 argillaceous and arenaceous shale. Nodules of argillaceous iron 
 
 ore are contained in some of the layers, and comminuted carbonized Iron ore. 
 
 plants are frequently seen on the divisional surfaces ; those which 
 
 have been determined belong to the species already mentioned, .... 916 
 
 3. Drab sandstones, inclining to reddish at the bottom and greenish at 
 
 the top ; with occasional scattered quartz and jasper pebbles, and 
 large spheroidal masses, as above. Ferruginous stains are frequent, 
 and the beds, usually massive, are separated by layers of grey 
 argillo-arenaceous shale, which, as well as the sandstones, some- 
 times contain nodules of argillaceous iron ore. In the middle and 
 lower part, there are interstratified two conspicuous beds of claret- 
 red, green, and dark grey argillo-arenaceous shale ; in the upper one 
 of which are two, and in the lower, eight bands of a grey tough 
 rock, much like fire-clay, penetrated vertically by the rootlets of 
 Psilophyton, 428 
 
 4. Drab sandstones, inclining to green ; some of which contain quartz 
 
 and jasper pebbles ; many parts have large hard spheroidal 
 masses, as before. The beds are in general very thick, and they are 
 separated by layers of grey argillaceous shale, from which large 
 argillaceous masses occasionally protrude into the superincumbent 
 sandstone, some of these being as much as three feet high and as 
 broad. Comminuted carbonized plants, similar to those already 
 named ; occur on the surfaces of the lower beds, 2052 
 
 5. Drab sandstone, in massive beds, in only a few of which there are 
 
 scattered quartz and jasper pebbles. The sandstones are interstrati- 
 fied with five conspicuous bands of claret-red, green, and grey 
 argillo-arenaceous shale, of an aggregate thickness of 140 feet,. . . . 442 
 
 6. Drab strong and coarse conglomerates, in massive beds, one of them Conglome- 
 
 156 feet thick. The pebbles of these consist of white quartz, black rates - 
 
 chert, yellow, green, and blood-red jaspers, and jasper porphyry; 
 with which are sometimes found others of feldspar and of limestone, 
 the whole enclosed in a matrix of drab-colored sandstone. In some 
 portions of the deposit, the pebbles diminish in quantity, so that the 
 rock becomes a rather fine-grained sandstone, with only occasional 
 pebbles. The carbonized comminuted remains of plants occur on 
 the surfaces of the beds, and in their oblique elementary layers or 
 false bedding. Among the organic remains of this division, fish- 
 spines or ichthyodorulites occur, of the genera Onchus and Mack- 
 
 aracanthum ; one of them, the M. sulcatus of Newberry, 856 
 
 5222 
 
 7. Red sandstones, sometimes slightly calcareous, with green stripes and Ked sandstones. 
 
 spots, many of the beds massive ; associated with occasional drab 
 sandstones, and with two thin bands of conglomerate, holding peb- 
 
396 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Little Gasp6 
 Cove. 
 
 Gaspe" Bay. 
 
 Tar Point. 
 
 Feet. Feet. 
 
 bles of quartz, jasper, and limestone. All of these are interstratified 
 with red argillaceous and arenaceous shales, spotted and striped with 
 green. In many cases, the sandstones exhibit on their under sur- 
 faces, highly relieved casts of shrinkage cracks and of rain drops, 
 and on the upper surfaces ripple-marks. The shales are sometimes 
 penetrated by branching plants, in vertical, oblique, and prostrate 
 attitudes ; while one or two beds have fibrous root-like impressions, 
 
 probably of Psilophyton, running across them at right angles, 1151 
 
 8. Drab massive sandstones, which in the lower part are clouded or 
 mottled with a reddish tinge, and at the bottom exhibit an inter- 
 stratification with red shales ; at the summit the beds are inclined 
 to grey. In many parts, they hold scattered pebbles of white and 
 greenish quartz, and blood-red jasper, with some of limestone ; but 
 the pebbles never become so numerous as to constitute a conglom- 
 erate. On the surfaces of many of the strata, and in the oblique 
 elementary layers or false bedding of some of them, there occur 
 carbonized comminuted remains of plants ; which are too imperfect 
 to be determined, 663 1814 
 
 7036 
 
 The lower portions of this great series of sandstones are met with in 
 Little Gaspe* Cove ; where, in addition to the various species of fossil 
 plants already mentioned, are found the remains of what appears to 
 be a species of Calamites ; one specimen of which shows a flattened 
 stem four feet long, with a breadth of four inches. The inferior por- 
 tion of the formation skirts the north-eastward side of Gasp6 Bay, and the 
 North- West Arm, from the cove, as far as the north branch of Dartmouth 
 River ; where it occupies a breadth of about 9000 feet, across the mea- 
 sures ; giving, at an average dip of twenty-six degrees, a thickness of 
 about 4000 feet. On the south-west side of Gaspe* Bay, in the neighbor- 
 hood of Gaspe* Basin, the same strata rise with an opposite and more 
 precipitous slope, forming a trough under the bay. The thickness there 
 exposed is again about 4000 feet. The same beds next fold over an 
 anticlinal axis, which comes out upon the bay near Cape Haldimand; then, 
 dipping at a very moderate angle on the south-west side of the axis, beneath 
 the lagoon at the mouth of the river St. John, they re-appear, with a nearly 
 opposite slope, at the south-eastern end of Douglastown village ; and exactly 
 face Great Cape Oiseau (Cap Brule* of Bayfield's chart) and Little Gaspd, 
 on the north-east side of the bay. Following the coast, they exhibit a 
 slight sinuosity in Seal Cove (Bre*haut Bay of Bayfield) ; and at the 
 extremity of Tar Point, between this cove and the next one farther on, 
 they fold over another anticlinal axis ; the position of which is indicated by 
 a remarkable greenstone dyke, holding petroleum. The direction of both 
 of these anticlinals is nearly north-west and south-east. 
 
 It is from this point to the termination of the series, in the cove imme- 
 diately northward of Pointe Jaune or Yellow Head, that the strata given 
 
CHAP. XVI.] 
 
 GASPfi SANDSTONES. 
 
 397 
 
 in the vertical section are found. The coast cuts them obliquely ; and in 
 every step south-eastward from Tar Point, higher strata are met with, in 
 advancing, until Long Cove is reached, where the red sandstones are seen. Long Cove. 
 
 426. PLANTS 
 
 426. Psilophyton princeps (Dawson) ; a, rhizome ; 6, stem ; c, termination 
 of a branch ; d, vernation ; e, fructification ; /, longitudinal 
 section of stem, all of natural size ; g, areole of rhizome en- 
 larged ; h, restoration of the plant, reduced. 
 
 In this cove, the measures have a very moderate inclination, and a slight 
 protrusion in the line of strike causes the coast section of the cliff to present 
 a gentle arch in the centre, repeating a part of the beds. Farther on, 
 
398 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Anticlinals. 
 
 the section still gains upon the strata, in the vicinity of Red Head, and 
 beyond it ; until they are suddenly cut off by a fault, at the spot already 
 indicated as the termination of the series. Throughout the whole distance, 
 the strata are seldom concealed ; and though several small faults occur, 
 the allowance that is to be made for them, may be seen in the cliff, which 
 is generally bold. 
 
 The two anticlinals which have been mentioned, appear to run parallel, 
 as well to the mountain ranges of the neighborhood, as to the calcareous 
 rocks on the north-east side of Gaspe* Bay. They may be about three 
 miles asunder in a direct line. The northern one is traceable for seven 
 miles, from the vicinity of Cape Haldimand to the inner basin at Gaspe* ; 
 which it crosses about 350 yards south-west of the Narrows at the entrance. 
 It brings to the surface, on the north side of the basin, some beds of 
 
 427. Psilophyton princeps (Dawson) ; portions of stem magnified three 
 hundred diameters ; a, cortical cells ; b, scalariform tissue of 
 the axis ; c, parenchyma. 
 
 sandstone, which are rendered calcareous by an abundance of fossils. 
 These beds contain comminuted remains of land plants, and impres- 
 sions that bear a strong resemblance to Fucoides caudargallL With 
 these are associated, among other species, Strophomena Blainvilli, Rens- 
 selceria ovoides, two undetermined species of Chonetes, Spirifera Grasp- 
 ensis, Leptocoelia fldbellites, Avicula Woodwardi, and Grammysia Ver- 
 neuili. The beds to the north-east of these, along the south-west side of 
 Gaspe* Harbor and Bay, as already indicated, are upwards of 4000 feet 
 higher in the series. They contain a few interstratified bands of a red 
 color near the top, some of them with casts of shrinkage cracks ; and along 
 the strike, between Pointe Lourde and Cape Haldimand, some of the best 
 characterized specimens of the land plants of the formation are to be 
 obtained. In the upper 760 feet, eight beds are seen to be marked by 
 the vertical rootlets of Psilophyton ; and on one of these, two hundred 
 of the rootlets were counted in a square of six inches. 
 
CHAP. XVI.] 
 
 GASPfe SANDSTONES 
 
 399 
 
 The mark which has been taken as indicating the direction of the 
 southern anticlinal axis, is the course of the greenstone dyke in its 
 vicinity ; this, however, has as yet been traced only a short distance, as it 
 soon becomes covered up, after striking into the forest. It is probable that Dislocation. 
 this dyke is connected with a dislocation, throwing down the measures to 
 the north-eastward. It is not easy, however, to say how much higher in 
 the series the beds on that side may be, than those on the south-west. The 
 latter are, as has already been stated, at the base of the 7036 feet of strata 
 given in the vertical section ; while on the north-east side, between Tar 
 Point and Douglastown, a section of 3800 feet was observed, after which 
 the summit of the series became concealed. At about 500 feet from the Fossa 
 base of this section, there are met with the remains of a coniferous tree, conifer - 
 
 428. PLANTS. 
 
 428. Selaginites formosus (Dawson) ; a, fragment of shale, with portions 
 of a large and a small specimen of Selaginites, showing the im- 
 bricating scales ; accompanied by three fragments of Psilophy- 
 ton princeps, and two of Cordaites angustifolia (Dawson) ; 
 &, small specimen of Selaginites, and c, scale of larger specimen, 
 both enlarged. 
 
 described by Dr. Dawson under the name of Prototaxites Logani. The 
 stem of one of these, obtained by Dr. Dawson, must have been twelve 
 inches in diameter, before it became compressed. About 600 feet still 
 higher among these strata, several surfaces in succession are marked by 
 serpentining impressions, about an inch wide, deeply grooved into the stone, 
 marked by small parallel transverse furrows, which are about a quarter of 
 an inch apart. These are perhaps worm-tracks, and are associated with a 
 few bivalve shells of the genus Hemselceria, probably R. ovoides. All of 
 these strata, and most of those above them, in which sandstone greatly pre- 
 dominates over shale, are in general drab colored, though some are grey. 
 Many of the surfaces are marked by carbonized comminuted plants, similar 
 
400 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Veins of 
 galena. 
 
 to those which have already been mentioned ; and argillaceous iron ore 
 occurs in nodules in several beds, about the middle of the mass. 
 
 The dips on the north-east side of both of these anticlinal flexures are 
 more precipitous than those on the south-west. In this they accord with 
 the general character of the undulations in the Lower Silurian strata south 
 of the St. Lawrence. The strikes of the anticlinal beds are not precisely 
 parallel, but converge towards the south-east ; from which it results that 
 the ridges or crowns of the folds have a slope in that direction. 
 
 The limestones, in their exposure of four miles, at Cape Gaspe*, present 
 numerous dislocations, with dykes, and with veins of calcareous spar, some- 
 times with galena. One of these localities is in the bight of Little Gaspe" 
 Cove, where the limestone is washed by the waters of the bay. Here are 
 several fissures, holding these two minerals, and having a direction of N. 55 
 E., with an underlie to the northward. Near to these veins, is a dislocation, 
 
 429. PLANT JJ. 
 
 6 
 
 429>Lepidodendron Gaspianum (Dawson) ; a, small branch and leaves ; 
 6, decorticated branch ; c, areoles of a larger branch ; all of 
 natural size. 
 
 with a downthrow on the north-west side, by which the limestone is brought 
 against the higher sandstones. It is probable that the mineral veins have 
 some connection with this dislocation. An attempt recently made to work 
 this deposit of galena, has given promise of favorable results. 
 
 Indian Cove. The other locality of galena is in Indian Cove. Here is a downthrow to 
 the south-eastward, of at least thirty fathoms, by which the higher sand- 
 stone is brought opposite to the limestone. Between these walls, there is 
 a lode about twelve feet wide ; composed of the ruins of the two rocks 
 cemented together by calcareous spar, and including numerous small veins 
 of the same mineral, with crystals of galena. The principal one of these 
 veins is about two inches wide in the thickest part : it has an underlie 
 
CHAP. XVI.] 
 
 GASPfe SANDSTONES. 
 
 401 
 
 N. 74 W. < 55; but the general course of the whole lode, in which the 
 small veins occur, is about N. 18 E., and the underlie appears to be 
 westward. The dislocation in this place points to a transverse valley or 
 depression in the hills behind, which appears to run across to the oppo- 
 site side of the promontory, in a course nearly N.E. In a dislocation 
 on the north-east side of the promontory, which is supposed to correspond 
 with this fault, and where a continuation of the lodes might be expected, 
 no ore has yet been observed. 
 
 Transverse dislocations are of common occurrence in this vicinity. One Dislocations, 
 of them, in a recess about a quarter of a mile above Indian Cove, is filled 
 with white calcareous spar, which has a thickness of nine feet in one part, 
 
 429, 430.: 
 
 429. Prototaxites Logani (Dawson) ; a, cross section magnified forty dia- 
 meters, showing growth line and medullary ray ; 6, longitudi- 
 nal section ; c, transverse section, each magnified three hun- 
 dred diameters. 
 
 430. Scalariform tissue, probably from the axis of a Lepidodendron, magni- 
 fied three hundred diameters. 
 
 and one foot in another. The underlie of the vein is S. 65 E. < 76, while 
 the dip of the strata at the spot is S. 55 W. < 22. On the north side 
 of the promontory, seven dislocations, in the space of about a mile and a 
 half, may be seen at one view, from a convenient distance out on the 
 water. The displacements in six of these, compensate one another ; and the 
 slope or underlie of the faults, in every instance, is in the direction of the 
 downthrow. 
 
 Greenstone dykes, intersecting both the limestones and the sandstones, Dyke's, 
 are seen in several places. One of these is found, cutting the strata, with- 
 out any apparent displacement, a little to the north of the Petit Portage, 
 in Cape Rosier Bay. Its breadth is eight feet, and it traverses a part of 
 
 AA 
 
402 GEOLOGY OF CANADA. [CHAP. XVI. 
 
 the shale which is between the lower two bands of limestone. The rock 
 on each side is a little harder than elsewhere, but it is not otherwise altered. 
 The course of the dyke, which is very nearly vertical, is N. 79 W. 
 
 Another of these greenstone dykes intersects the sandstones, about a 
 mile and a quarter above the outside point of Little Gaspe* Cove. It is 
 about four yards wide; and its course, as far as seen on the shore, is S. 
 89 E. There is, however, a turn in the dyke, running for five yards in 
 the direction S. 31 W. ; and coinciding with this, is a cross fault, of 
 which the underlie is S. 59 E. < 68. Here is a space of six or eight 
 inches, filled with a compact feldspar, holding opaque white feldspar crys- 
 tals, and irregular veins of carbonate of lime. In that part of the dyke 
 which is near, thin veins of iron pyrites occur, which have an irregular 
 parallelism with the cross fault. The dyke is nearly perpendicular ; and 
 the strata on each side, which have been indurated, dip S. 49 W. < 28. 
 
 Another dyke occurs about 300 yards below Little Cape Oiseau (Cape 
 James of Bayfield). Its course is about N. 86 E.; and its underlie, 
 which is southward, eighty-eight degrees. There is an angular turn in it, 
 which carries it N. 6 E., for a few yards. The mineral character is much 
 the same as the previous one, and it exhibits a tendency to a transverse 
 columnar structure. Another dyke stands up like a wall, at the mouth of 
 a small brook, about 300 yards above Little Cape Oiseau. Its course is 
 N. 69 E. 
 
 Still another greenstone dyke occurs, on the opposite side of Gaspe* 
 Bay, in Ance Cousin, close by the mill and brook, about a mile and three 
 quarters above the bluff, on the upper side of the entrance to the South- 
 West Arm. Its course is S. 61 W. ; and its underlie, to the southward, 
 seventy-eight degrees. Its breadth is fifteen feet ; two feet of which, on 
 the northward side, weather of a more rusty color than the rest, and 
 exhibit an imperfect transversely columnar structure. The sandstone on 
 each side of the dyke, dipping N. 41 E. < 58, is hardened for a short 
 distance; and it displays a more than usual number of joints, which are 
 parallel with the dyke. 
 
 retroieum. There is still to be described the greenstone dyke, connected with the 
 southern anticlinal, at Tar Point. This dyke, which does not occur in 
 the centre of the fold, but about 200 yards to its north-east or precipitous 
 gide, has a breadth of ten or twelve yards, with a direction N. 83 W. 
 Its color is dark grey, weathering to a rusty red, and it is traversed by 
 numerous horizontal and vertical joints, and abounds in large and small 
 druses; which, as well as the joints, are often lined with chalcedony; some- 
 times, in the ease of the druses, presenting botryoidal surfaces, and at 
 others, incrusted with crystals of quartz and calcite. These cavities, as 
 well as others which are not thus lined with chalcedony, are filled with 
 petroleum: this, in some instances, has hardened to the consistency of 
 
CHAP. XVI.] ' GASPS SANDSTONES. 403 
 
 pitch. The peculiar odor of this substance, which has given the name of 
 Tar Point to the locality, may be perceived at a distance of fifty yards. 
 
 Two petroleum springs occur along the line of this anticlinal. One of on springs, 
 these is on the south side of the St. John River, about half a mile above 
 Douglastown. Here the oil oozes from the mud and shingle of the beach, 
 and is seen in globules, rising through the water, at high tide. Portions 
 of the oil are said to have been observed, under similar conditions, as far 
 as the extremity of the first marshy island, a distance of three fourths of 
 a mile above ; and they may probably extend much farther in the same 
 direction. 
 
 The second spring was observed about 200 yards up a small branch of 
 the Silver Brook, which is a tributary of the South-West Arm, falling into 
 it about six or seven miles from Gaspe* Basin. The orifice of the spring 
 was not seen ; but the oil, which is not observed higher up on the brook, 
 here collects on the surface of quiet pools, as a thick film. These two 
 petroleum springs are nearly in a right line with the bituminous dyke ; 
 and in the direction indicated by the bearing of the latter, which is distant 
 about twenty miles from the farthest spring. It is therefore likely that 
 these occur along the line of the undulation, with which, as we have 
 already remarked, the dyke seems to be connected. 
 
 The rock adjoining the dyke, and underlying both of these springs, is 
 sandstone ; but it is not improbable that here, as in Western Canada, the 
 source of the oil may be in the more fossiliferous rocks beneath ; so that 
 we may hope to find other springs of it, not only along the line of twenty 
 miles, just indicated, but still farther along this and other undulations in 
 the same region; where borings and wells may furnish more abundant 
 supplies of petroleum. 
 
 As has already been stated, the limestones of Cape Gaspe* appear, for onskany 
 the most part, to belong to the Lower Helderberg group. The fossils formation - 
 at the summit, however, bear a striking resemblance to those of the Oris- 
 kany formation, with which several of them are identical. It appears 
 probable, therefore, that we have here a passage from the Lower Helder- 
 berg to the Oriskany, and the latter formation may be more especially 
 represented by the lower part of the Gaspe* sandstones. The organic 
 remains discovered in these sandstones are as yet too few to enable us to 
 separate the series into distinct members. We have already mentioned 
 that a species of Rensseloeria, identical with or closely resembling R. 
 ovoides, which occurs in the upper part of the limestones, is met with at 
 1100 feet above the base of the sandstone series. This fact, together with 
 the constancy in the lithological characters of the latter, makes it not 
 improbable that at least this lower portion of the sandstones, will ultimately 
 be classed with the Oriskany formation. 
 
404 GEOLOGY OF CANADA. [CHAP. XVI. 
 
 In the land plants, there appears to be but little difference from the 
 commencement of the series to the base of the red sandstones : a thickness 
 of over 5000 feet. These strata present analogies with the whole series of 
 formations in New York, from the Marcellus shales to the summit of the 
 Chemung sandstones; in all of which, according to Dr. Dawson, are 
 found several of the species of plants that occur in the Gaspe* sandstones. 
 The whole of these 5000 feet resemble, lithologically, the Portage and 
 Chemung sandstones of New York ; and it may hereafter be found that 
 in this eastern part of the continent, the Oriskany fauna, which occurs at 
 the base of this Devonian series, merges gradually, towards the summit, 
 into that of the Portage and Chemung group. In lithological characters, 
 the remaining upper 1800 feet of the Gaspe* series, resemble the Catskill 
 group of New York, which is regarded by Mr. Hall as the base of the 
 Carboniferous system. As yet however no comparison can be made by 
 fossils ; those found in Gaspe* being chiefly confined to a few obscure plants. 
 
 The Gaspe* limestones and sandstones have been traced for a consider- 
 able distance to the eastward of the localities just noticed ; but before 
 giving what is known of their distribution, it will be convenient to describe 
 the succeeding formation ; which is, so far as yet known, the highest mem- 
 ber of the palaeozoic rocks 'in Canada. 
 
 THE BONAVENTURE FORMATION. 
 
 This formation, which is shown by the section on the Bay of Chaleurs, 
 
 to belong to the base of the Carboniferous series, rests in unconformable 
 
 stratification upon the rocks hitherto described ; and consists of a series 
 
 of red sandstones, interstratified with beds of a coarse calcareous conglom- 
 
 Bonaventure erate. The island of Bonaventure, opposite to Perce*, is entirely composed 
 
 island. O f this series ; for which we have, in consequence, chosen the name of the 
 
 Bonaventure formation. The best section of it is however seen on Gasp 
 
 Bay, extending from a small cove immediately on the upper side of Pointe 
 
 Jaune (which is the first small cape above what is named White Head 
 
 on Bayfield's chart), to the extremity of Point Peter. 
 
 Congiom- The pebbles and rounded masses of the conglomerate, which often weigh 
 
 erate. from seven to fifteen pounds, are chiefly of grey limestone and calcareous 
 
 sandstone ; in some of which are found encrinites, and JEatonia peculiarity 
 belonging to the upper part of the Gaspe* limestones. Besides these, are 
 pebbles of red shale and sandstone, with others of red feldspar, syenite, 
 porphyry, and white, yellowish, and greenish quartz. Associated with 
 these, are others of agate, and of red, yellow, and green jaspers, often bril- 
 liant in color; which have probably been derived from the conglomerates 
 
CHAP. XVL] BONAVENTURE FORMATION. 405 
 
 of the Gaspe* sandstones. These jaspers and agates are known among col- Gasps pebbles. 
 
 lectors as Gaspe* pebbles, and are found in abundance along the sea-shore 
 
 in this region. The matrix of this conglomerate is usually a red sand, 
 
 which is often pervaded by a calcareous cement ; this, in some parts, is 
 
 seen as a white calcareous spar among the pebbles. The prevailing color 
 
 of the conglomerate, arising from this mixture, is a pale red ; while the 
 
 associated sandstone beds are of a deeper red, and sometimes drab-colored 
 
 or brown, with occasional partings of shale. Ripple-marks and casts of 
 
 shrinkage-cracks occur in the sandstone ; and the remains of plants are 
 
 found in many of the beds, sometimes carbonized, and sometimes as casts 
 
 only. The impressions of plants in one bed of red shale, are tinged with 
 
 a green color. 
 
 The entire volume of this section is 2766 feet ; of which a little less than 
 one fourth is made up of conglomerate beds, varying in thickness from one 
 foot to one hundred and eighty-seven feet. The highest part of the sec- point peter, 
 tion is at the very extremity of Point Peter ; where a succession of strong 
 conglomerate beds, plunges, at an angle of fifteen degrees, beneath a rock 
 called Flat Island, lying just half a mile distant, and composed of strata 
 dipping in the same direction as those at the point, but at a less angle. If 
 there be no fault or undulation in the channel, and if we assume for the dip 
 of the intermediate strata an angle of seven or eight degrees, it would 
 give about 300 feet additional, to be added to the vertical thickness; 
 making the volume of the formation at this point, upwards of 3000 feet. 
 It is not improbable that there may be something to be added to the lower, 
 as well as to the upper part ; for in the cove above Pointe Jaune, the base 
 of the section is let down against the Gaspe* sandstones, by a dislocation of 
 unknown amount. The direction of this fault appears to be S. 18 W. ; 
 and the older strata, which, at a distance of 500 yards across the measures, 
 have a dip not exceeding ten degrees, and not more than twenty degrees 
 at half that distance, are gradually bent down to forty, and even to sixty 
 degrees, as they approach the fault. The strata of the Bonaventure 
 formation, on the contrary, are slightly turned up at the junction, where 
 they abut against the Gaspe* sandstones, and thence present a moderate 
 dip of from twelve to eighteen degrees, which they preserve with consider- 
 able uniformity, to the extremity of Point Peter ; the direction of the dip 
 being S. 86 E. From Pointe Jaune to Tickel Inlet, the salient parts of 
 the shore are composed of the conglomerate beds, while the re-entering 
 angles correspond to the softer and less resisting red sandstones. This 
 explains the zigzag line of the coast ; the general course of which, on both 
 sides of Point Peter, is oblique to the stratification. 
 
406 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 THE DISTRIBUTION OF THE GASPE SERIES. 
 
 Limestones. The Gaspe* limestones are traceable from Little Gaspe* Cove, on the north 
 side of the North-West Arm, and its tributary, the Dartmouth River, for 
 twenty-four miles. They appear to preserve a pretty uniform breadth, 
 which, at seven or eight miles above Little Gaspe* Cove, is about a mile 
 and a quarter; the inclination of the strata being to the south-west, at an 
 angle of twenty-two degrees. The first exposure on the road from Griffin 
 Cove, occurs at the Ruisseau de la Grande Carriere ; where the base of the 
 series appears as a pure grey limestone, interstratified with some beds, 
 which contain an arenaceous mixture, and, on the weathered surfaces, are 
 converted, to a depth of half an inch, into a porous white earth. Similar 
 beds overlie the limestones, which contain nodules of chert, and abound in 
 fossils: among these are Favosites G-othlandica, Strophomena rhomboi- 
 dalis, and Atrypa reticularis, with crinoidal stems. These beds dip S. 54 
 W.', at an angle of twenty degrees ; and after a mile and a quarter in this 
 direction, an exposure of iron-grey limestone is seen, dipping S. 4 W., at 
 an angle of twenty-two degrees. This is supposed to be at the summit of 
 the series ; and would give for the section at this place, a thickness of about 
 2100 feet. From this point, to the margin of the bay, there is a distance 
 of a mile and a half; in which occurs an exposure of greenish sandstone, 
 dipping S. 29 W., at an angle of thirty^ine degrees. Judging from the 
 outcrops on the coast farther down, it is probable that the whole breadth is 
 occupied by the Gaspe* sandstones, which would thus have a thickness of 
 about 4000 feet ; and, as already stated, are here dipping down on the 
 north side of a synclinal, to appear with a contrary dip on the opposite 
 side of the bay. 
 
 At a distance of seventeen miles above Little Gaspe* Cove, the lime- 
 stones are met with about two miles from the Dartmouth ; but at the end of 
 the twenty-four miles already mentioned, the upward course of the river is 
 nearly north, and would cross the limestones, if they continued in their 
 north-westward bearing. They are however wanting on the river ; while a 
 short distance to the southward, the serpentines of the Quebec group rise 
 into a hill. There must thus be either a transverse dislocation, or a turn 
 in the limestones around a synclinal to the south. This latter would 
 coincide with the synclinal of the North- West Arm, the axis of which would 
 run with the lower part of the Dartmouth River. It is therefore probable 
 that the limestones will present a spur, projecting into the township of 
 Gaspe* Bay South, between the Dartmouth and York rivers, on the 
 Haldimand anticlinal. 
 
 Dartmouth 
 River. 
 
CHAP. XVL] DISTRIBUTION OF THE GASPfi SERIES. 407 
 
 SECTION FROM THE MAGDALEN TO THE DOUGLA8TOWN BIVEE. 
 
 About three and a half miles west of the turn in the Dartmouth River, 
 just mentioned, the limestones re-appear at the eastern extremity of a trough; 
 which has a length of thirty-six miles, extending to Clear Water Brook, a 
 tributary of the Magdalen, a little west of longitude 65 30'. It is pretty 
 well ascertained that the limestones surround this trough, in which the 
 included sandstones are divided into two areas, by a transverse undulation 
 bringing up the limestones; the western area of sandstone being more 
 than twice the length of the eastern. The width across this synclinal, Magdalen 
 including the limestones on each side, is about six miles in the eastern, and basm ' 
 seven in the western portion. Along the northern limit of this, the Mag- 
 dalen River flows for a certain distance ; and then turns northward, at a 
 point fourteen miles from the St. Lawrence. Here, at the turn, the whole 
 volume of the limestones is seen in the flank of a mountain, which rises up 
 from the river hi successive terraces. The dip of the strata is very regular 
 and uniform, being from S. 5 E. to S. 14 E. < 38- 35. The forma- Limestones, 
 tion occupies a breadth of twenty-four chains, and its uppermost beds 
 appear 1375 feet above the base. In going over the mountain, the exposures 
 met with, are at considerable distances. In the section measured, only 
 210 feet of brownish-grey shaly limestone and calcareous shale were vis- 
 ible, at intervals varying from thirty to nearly 600 feet ; while 2072 feet 
 were concealed, making the total volume of the series 2285 feet. No 
 fossils were seen ; and only one loose fragment of limestone holding organic 
 remains, was met with. This occurred at the foot of the mountain, near 
 the base of the formation ; but the fossils in it resemble some of those which 
 occur at the top of the limestones, near Ship Head, in Gaspe* Bay. Among 
 the species are Strophomena rhomboidalis, with undetermined species of 
 Chonetes and Platyostoma. 
 
 The crest of the hill and the summit of the limestones, as given above, 
 coincide ; and the Gaspe* sandstones are supposed to come in on the line 
 of section, some short distance to the southward, on the slope of the hill. 
 The junction of the two formations, however, was not seen ; and the first 
 exposure indicating a change in the strata, was met with in a spot, whose 
 place on the line of section would be a mile and a half from the limestones. 
 The rock at this point is a greenish-grey or drab sandstone, having dissem- 
 inated throughout it small scales of silvery mica. The beds are from two sandstones, 
 to six inches thick, and abound in comminuted carbonized remains of land 
 plants, and brachiopodous shells ; but it is difficult to procure these suffi- 
 ciently well preserved to be properly identified. The number of species 
 does not appear to exceed two or three ; and the most abundant is identical 
 
408 GEOLOGY OF CANADA. [CHAP. XVI. 
 
 with a small fiensselceria ovoides ? from the sandstones of Gasp6 Bay. 
 The dip of these fossiliferous beds is S. 14 W. < 55. 
 
 About a mile and three quarters southward of this, similar drab sand- 
 stones, but without fossils, occur on a small stream: here the dip is 
 N. 1 W. < 14. Between this stream and the next one, about a mile 
 and a half farther south, a hill is interposed, rising to the height of about 
 800 feet. On the north side of this hill, the sandstones are very generally 
 seen up to the summit, which is about a quarter of a mile north of the 
 second brook. At the summit, the dip is N. 18 E. < 39 ; and the 
 escarpment, down to the brook, is very abrupt. No rock in place was 
 observed, either in the escarpment or on the brook ; but numerous large flat 
 fragments of calcareo-arenaceous shale, abundantly marked with carbon- 
 ized remains of plants, are mingled with others of a very arenaceous 
 limestone : these are accompanied with fragments of chert, The brook is 
 therefore supposed to be the southward limit of the sandstones ; which thus 
 lie between it and the crest of the hill above the Magdalen, in the form of 
 a trough, measuring on the line of section about four miles and a half. 
 This, according to the dips observed on the opposite sides of the syncli- 
 nal, would give for the sandstones a thickness of about 6000 feet. 
 
 Crossing the measures southward, towards York River, the only exposure 
 of limestone that has been met with on the south side of the trough is a 
 little over a mile and a half forward. This occurs about half a mile down 
 an escarpment ; descending from the summit of a gradual rise, which attains 
 a height of 700 feet. It consists of about thirty feet of dark brownish 
 limestone, without observed fossils ; weathering partly white and partly 
 brown, with patches and nodules of chert. The dip of these limestone 
 strata is N. 9 E.<15-20. 
 
 York River. The distance from this position to York River, is rather over four miles ; 
 and in the interval, no exposures of rock have been observed ; but on the 
 river, dark grey calcareous shales occur, showing fine lines of stratification, 
 and breaking into flat fragments of from one to six inches thick ; which, like 
 some of the calcareous rocks in the terrace over the Magdalen, weather 
 white. The dip of the strata is S. 1 E. < 43. About two miles down 
 the stream, not much out of the strike of these beds, a height of 400 feet 
 above the river is capped by 100 feet of calcareous shale, of a somewhat 
 softer character, and weathering brown and white. In this Were met with a 
 few fragments of brachiopods, and two small species of Orihoceras ; one of 
 which strongly resembles an undescribed species from the limestone cliffs 
 of Cape Gaspe*. 
 
 These calcareous shales, and the limestones four miles to the north, 
 appear, without much doubt, to be equivalent strata on the opposite sides 
 of the Haldimand anticlinal. There is space enough between the two expo- 
 sures for a portion of the Lower Silurian series. The strike of the York 
 
CHAP. XVI.] DISTRIBUTION OF THE GASP6 SERIES. 409 
 
 River beds would carry them to a junction with the supposed limestone 
 spur in the township of Gaspe* Bay South ; and in their progress they would 
 pass sufficiently near to the northern beds, to make it probable that the two 
 join on the axis of the anticlinal, to the westward of the serpentine. 
 
 The course of the York River strata, to the westward, has not yet been 
 ascertained ; but fourteen miles south of this band, limestones occur on River ' 
 the Douglastown or St. John River, occupying nearly twenty-five miles of 
 its bed, and reaching to within thirteen miles of its mouth. In these twenty- 
 five miles, the valley of the stream, which is nearly straight, is upon the 
 axis of an anticlinal; and while the limestones dip at pretty high angles 
 northward on the north side and southward on the south, they are followed, 
 usually at no great distances, by sandstones ; which compose the flanks of 
 the hills on each side. Some of the limestones are blue, hard, and silicious, Limestones, 
 while others are blue and grey, hi thin beds : they are associated with grey 
 calcareous shales. The thin bedded portions are frequently nodular, and 
 chert accompanies them in some places. Some of the beds may yield 
 good lime, but the great mass appears to be too silicious for such a pur- 
 pose. The only fossils detected in them were fucoids resembling Fucoides 
 cauda-galli, and similar to those which are so abundant at the top of the 
 limestones of Gaspe* Bay. 
 
 The inferior portion of the sandstones is seen at a turn on the Douglastown sandstones. 
 River, a short distance above the Alexander, which joins it on the right bank. 
 The beds, here resting on the limestones, are dark brown fine grained ferru- 
 ginous sandstones, abounding with fragments of carbonized plants. They 
 are marked with ferruginous spots from decomposing iron pyrites, and 
 parted by thin layers of black carbonaceous shale. They are succeeded 
 by thick beds of a fine conglomerate, composed chiefly of small pebbles of 
 transparent and translucent whitish quartz, with lumps of black shale, in a 
 hard calcareo-arenaceous matrix. Between the aspect of these beds, and 
 the strata somewhat higher in the series, there appears but little difference ; 
 their general character being that of drab coarse grained sandstones, 
 sometimes in massive beds, and at others in thin irregular layers, inter- 
 stratified with drab arenaceous shale. The sandstones are occasionally 
 separated from one another by thin carbonaceous layers, composed almost 
 entirely of the comminuted remains of plants. Various sized pebbles are 
 frequently scattered irregularly through the sandstones, although nowhere 
 observed in sufficient numbers to constitute a conglomerate. Large loose 
 masses of the sandstone were often found on the banks, and in the bed of 
 the river, holding shells enclosed in an arenaceous matrix. These so 
 strikingly resemble the fossiliferous strata brought up on the Haldimand 
 anticlinal, on the north side of Gaspe* Basin, both in the species of shells 
 and in the mode of their occurrence, as to leave little doubt that they are 
 derived from an equivalent bed, situated somewhere on the Douglastown 
 
410 GEOLOGY OF CANADA. [CHAP. XVI. 
 
 River. Among the species are Strophomena perplana, Leptoccelia fior 
 fylUtes, Rensselceria ovoides ? and Spirifera G-aspensis. 
 
 In the thirteen miles of the lowest part of the river, sandstones alone 
 are met with, usually of the character just described. The dip in this 
 part, while it is constantly northward, is reduced to a moderate inclination, 
 sometimes seven degrees, and never exceeding twenty. The axis of the 
 anticlinal would thus appear to leave the river, at a turn to the northward, 
 some five miles above the west side-line of the township of York, and to 
 bear thence towards Point Peter. 
 
 Three anticii- Not far from half-way between the Douglastown and Haldimand anti- 
 clinals, the distribution of the strata will probably be modified to a 
 certain extent, by the effect of a third anticlinal, which runs from the 
 coast at Tar Point. The axis of this anticlinal would probably coincide 
 with the valley of the York River, for about fifteen miles above the Silver 
 Brook ; but no examination of this part of the river having yet been made, 
 it is not known whether the limestones occur upon it. The double trough 
 formed by the three anticlinals, with the effect produced on the strata by 
 the intrusive granite of Table-top Mountain, will almost certainly bring 
 the York River limestones round to those on the Douglastown River, 
 with an eastward spur on the intermediate ridge ; but how far westward the 
 band may run before turning, can only be determined by exploration. 
 
 What may be the geographical arrangement of the limestones and sand- 
 stones, in striking westward from the Douglastown River, on the south side 
 of the anticlinal there, and in passing the southern extremity of the gran- 
 itic mass, must, for the present, be left mainly to conjecture ; there being 
 about fifty miles to the westward in which no facts have yet been collected 
 in respect to any of the rocks, and about seventy miles in which nothing 
 is known of the limestones. The next position along their outcrop to the 
 westward, in which the latter have been examined, is on a traverse made 
 obliquely across the measures, from the Chatte to the Great Cascape- 
 dia. The fossil remains obtained on this traverse were a portion of the 
 collections that were lost by shipwreck, and it is only those belonging to 
 the very base of the series that have been renewed. 
 
 SECTION OP THE CHATTE AND CASCAPEDIA KIVEK8. 
 
 Chatte Elver. On the south side of the Shickshock mountains, the main tributary 
 sources of the Chatte unite, before entering the deep gorge which there 
 traverses the range. Two of these tributaries flow from opposite directions, 
 in a depression running close along the foot of the mountains ; and in this 
 depression, the nearly vertical epidosite rocks of the Quebec group are un- 
 
CHAP. XVI.] DISTRIBUTION OF THE GASPfi SERIES. 411 
 
 conformably overlaid by a yellowish-white fine grained sandstone. This, as 
 far as seen, is about fifty feet thick, and is divided into massive beds. 
 Where the surfaces of these are weathered, the rock loses its yellowish 
 tinge, and has then a somewhat vitreous aspect. This sandstone, which 
 dips southward at an angle of from twenty to twenty-five degrees, is fol- Limestones, 
 lowed by about 200 feet of grey limestone, interstratified with some beds 
 of grey shale, dipping in some places at an angle of from sixteen to twenty- 
 five degrees, which moderates in others to one or two degrees. The lower 
 part of the mass is fossiliferous, and holds, among other species, an undeter- 
 mined Ptilodictya, Strophomena pecten, S. antiquata, S. rhomboidalis, a 
 new species of Orthis, 0. Davidsoni, with Stricklandia lens, S. brevis, 
 Atrypa reticularis, Calymene Blumenbachii, Phacops Orestes, and an un- 
 determined Encrinurus. All of these species are found in the Anticosti 
 group, and appear more especially to belong to the upper part of it. It 
 is probable that the whole 200 feet of limestone may belong to the same 
 group ; but before this can be determined, a new collection of its fossils 
 must be procured. 
 
 In the traverse made from the Chatte to the Cascapedia, after leaving 
 the limestones at the base, calcareous strata, moderately inclining to the 
 southward, were observed at the height of land, and in another position 
 beyond ; both included in a direct breadth of six miles across the measures. 
 In this distance, the fragments observed among the roots of overblown 
 trees, were of the same calcareous character ; but on reaching the first 
 tributary of the Cascapedia, a short distance beyond, there were met with, 
 in the bed of the brook, flat fragments of drab sandstone, presenting on 
 their surfaces comminuted carbonized remains of plants. Similar frag- 
 ments, mingled with others of limestone, continued to be occasionally seen 
 in the brooks, and among the roots of trees, to the end of the traverse, 
 equal to five additional miles directly across the measures. Fossiliferous Limestones, 
 limestones, were again observed in place, on reaching the Cascapedia ; but 
 the loss of the specimens makes it impossible to state to what portion of 
 the series they may belong. 
 
 At' the end of the traverse, the strata are disturbed by a mass of intru- conical 
 eive rock, constituting the Conical Mountain. This is a sharp pointed Mountam - 
 hill, 1910 feet above the sea, situated on the north side of the Great Cas- 
 capedia ; about thirty miles from the St. Lawrence, and about forty-five 
 miles from the Bay of Chaleurs. The igneous rock of which it is composed 
 is probably of the same character as the masses of trachytic granite to the 
 eastward ; but without specimens to institute a comparison,, this cannot be 
 stated with confidence. Its breadth on the river is about a mile ; and it is Cascapedia. 
 probably connected with another mass, which rises to some height on the 
 south side. It may extend altogether, as far as can be judged by the eye, 
 about five miles, in a direction a little west of south. 
 
412 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Sandstones. 
 
 Red sand- 
 
 In descending the river, grey fine grained slightly micaceous sand- 
 stones succeed the trap. They are interstratified with leaden-grey shales, 
 occasionally greenish and reddish, and both the shales and the sand- 
 stones hold bivalve shells. These strata are about 230 feet thick. Towards 
 the middle, some of the sandstones are yellowish and rather coarse grained, 
 and the surfaces of a few grey beds among them are studded with the 
 carbonized comminuted remains of plants. Some of the sandstones, which 
 are pyritiferous, show dark brown stains, and disintegrate readily under 
 the influence of the weather. The beds lean against the trap, their dip 
 being S. 52 E. < 50-44. 
 
 After an interval of concealment of about three quarters of a mile, direct- 
 ly across the measures (including probably about 3000 feet of strata), red 
 sandstones and shales make their appearance, dipping S. 53 E. < 60-40, 
 and occupying such a breadth as shows them to be about 900 feet thick. 
 Many of the beds present casts of shrinkage-cracks on the under surfaces, 
 and ripple-marks on the upper. Vertical upward-branching plants pene- 
 trate some of the red beds, which contain a few drab colored interstratified 
 layers, abounding in carbonized comminuted vegetable remains. Still 
 farther down the stream, the red rocks continue ; but the dip gradually 
 moderates to an inclination of nine degrees ; and 900 feet additional of 
 strata similar to those just described, are met with. 
 
 Where all these beds occur, the river runs southward across the measures ; 
 but it then turns eastward, and continues in a valley worn out in the strike 
 of the red rocks, for ten miles. In this, the strata present a very regular 
 dip to the east of south, for the first half of the distance, and south for the 
 remainder, never exceeding about ten degrees of inclination. To the south- 
 ward of this valley, and parallel with it, at the distance of about a mile, there 
 rises a range of hills ; some of the summits of which are about 1000 feet 
 over the river. These hills appear to be composed of greenish-grey sand- 
 stone, consisting of grains of quartz and opaque white feldspar, with a little 
 mica. The rock holds occasional pebbles of white quartz, blackish and 
 greenish silicious slate, soft greenish shale, and blood-red jasper, and the 
 surfaces of some of the beds are covered with carbonized comminuted plants. 
 These strata may be 1000 feet thick : they dip to the southward, and no 
 doubt overlie the red sandstone and shales already noticed, but between 
 the two there may be some strata wanting. 
 
 Turning southward, the Cascapedia twice intersects the strata of these 
 hills, in the distance of about ten miles, on the opposite sides of a synclinal. 
 The intermediate dips prove a gradual sweep in the stratification ; render- 
 ing it probable that a considerable portion, if not the whole mass of 
 sandstones, will crop out on the axis, not very far to the eastward ; a 
 result very likely to arise from the effect of the intrusive mass of Table-top 
 Mountain on the distribution of the strata. 
 
CHAP. XVI.] DISTRIBUTION OF THE GASPE SERIES. 413 
 
 SECTION OF THE MATANNE RIVJ 
 
 From the Chatte, the limestones strike along the south foot of the Shick- sandstones, 
 shock mountains to the Matanne. Here, the white quartzose sandstone at 
 the base, is speckled with small red ferruginous spots, and weathers of a 
 rusty yellowish color. It shows an occasional outcrop on the Matanne, 
 between its tributaries the Trout and the Tawagadie, and attains a thickness 
 of seventy feet at the mouth of the latter. In the eight and a half miles 
 between the gorge leading from Lake Matanne and the Trout, the lime- 
 stone escarpment rises boldly over the south bank of the Matanne, to a 
 height of between 500 and 600 feet. In this, the lower members of the Limestones, 
 series consist of blue limestones and grey calcareous shales, with thin 
 bands of blue limestone interstratified. A few fossils are met with in the 
 limestones, but none as yet sufficiently well defined to be recognized. The 
 upper part of the ridge is composed of massive beds of blue and grey lime- 
 stone holding numerous fossils. These have usually been much distorted 
 by molecular movements, and thus rendered somewhat obscure. Among 
 them are an undetermined species of Stenopora, and a large undeter- 
 mined species of Fenestella, Strophomena rhomboidalis, S. radiata? 
 S. perplana ? Spirifera perlamellosa ? S. pleiopleura ? undetermined 
 species of Athyris and Modiolopsis ? several undetermined species of 
 Platyceras and Platyostoma, and one of Conularia. While the sand- 
 stones at the base of the series would seem to ally this portion to the 
 Anticosti group, the beds at the summit have more the aspect of the Lower 
 Helderberg ; but better specimens of the organic remains will be required 
 to establish their equivalency with certainty. 
 
 The sandstones at the base, and the limestones at the summit, might 
 become serviceable for building purposes ; but it appears doubtful whether 
 the latter are not generally too silicious to be burned for lime. The Trout 
 River, intersecting the measures at right angles, exhibits a section of the 
 lower portion of the limestones, in which the lowest beds dip S. 38 E. 
 < 54 ; but at the end of the section, the inclination diminishes to twenty- 
 eight degrees, and the measures probably become nearly horizontal to the 
 southward, corresponding with the level character of the country ; in 
 which, however, no examination has yet been made, before reaching the 
 Matapedia. 
 
 SECTION OP THE MATAPEDIA LAKE AND RIVER. 
 
 The north-east side of Lake Matapedia appears to be occupied by rocks Lake Mata- 
 of the Quebec group. For four and a half miles from the upper or north- ped 
 western end, they consist of dark grey soft clay slates, enclosing, about 
 
414 GEOLOGY OF CANADA. [CHAP. XVI. 
 
 Quebec group, half-way down, a mass of conglomerate nearly a hundred feet thick, com- 
 posed of limestone pebbles, in a matrix of whitish sandstone ; bands of 
 which, without pebbles, separate the layers of conglomerate. The dip of the 
 conglomerate, with that of the slates to the north-westward of it, is north- 
 ward ; but the slates to the south-eastward have a contrary slope. In 
 
 siiieryfor- the latter direction, they are followed by sandstones, which probably 
 represent the Sillery series. A promontory about a mile and a half 
 below the mouth of the Awaggan, displays a section of these, in which 
 upwards of 700 feet of the usual greenish colored sandstones are inter- 
 stratified with occasional red layers. Similar sandstones, with red slates, 
 appear still farther down the lake, and are intersected by trap dykes. 
 Associated with these strata, is a large body of a peculiar dioritic rock, 
 often concretionary, and similar to masses which are met with among the 
 
 Epidotic rock, altered strata of the Quebec group in the Eastern Townships. This rock 
 abounds in epidote, which occurs among the concretions, and in veins. 
 Upwards of three miles of the lower part of the coast, and three or four 
 islands near, are occupied by these rocks ; the lowest of the islands, called 
 Makwash, being about a mile above the narrows leading to the lower lake. 
 The strike of the rocks on the north-east side of the lake is about 
 W. S. W., and from the conglomerate downwards, the dip is southward; 
 the inclination of the strata varying from thirty to eighty degrees. It is 
 very probable that in some parts they present overturn dips. On the 
 opposite side of the lake, the general strike is about N. N. W., with the 
 trend of the lake, and the dip is always to the westward. In only one or 
 two isolated instances, does the slope exceed ten degrees, and it is often 
 
 Gaspe- gand . not greater than three or four. The lowest strata on this side belong to 
 stones. the band of sandstone which we have just described on the Matanne ; 
 and from its attitude in relation to the rocks on the north-east side of the 
 lake, there is little doubt that it overlies them unconformably. This sand- 
 stone on Lake Matapedia is generally white, sometimes speckled with 
 small red spots : it frequently assumes a pinkish tinge, and occasionally 
 presents a band or two of a red color. Its thickness is computed to be 
 from sixty to seventy feet, but its contact with the rocks beneath it has 
 not been observed. It must come upon the lake somewhere near the 
 outlet, and it appears to occupy the south-west margin to within about four 
 miles of the upper end ; leaving the remainder, with the exception of a 
 point half-way, which is tipped with it, for the succeeding limestones. The 
 sandstones would afford very good material for building purposes ; and Mr. 
 Brochues, who is settled on the lake, has obtained from them good mill- 
 stones, which are used in his mill in the neighborhood. Loose blocks, 
 undoubtedly derived from some of the beds near, are occasionally met 
 with, holding fossils ; the whole of which are obscure, with the exception 
 of a cast of Pentamerus, strongly resembling P. oblongus. 
 
CHAP. XVI.) DISTRIBUTION OF THE GASPfi SERIES. 
 
 The calcareous rocks which succeed to this band of sandstone, have been Limestones, 
 examined only at their base ; where they occupy the upper part of the 
 south-west side of the lake, and are seen in contact with the underlying 
 beds. In this part, which may have a thickness of 150 or 160 feet, they 
 consist of dark brownish-grey somewhat arenaceous limestones, weathering 
 to a lighter grey. They enclose nodules of a purer limestone than the 
 mass, which is made up of irregular and uneven surfaced beds. The fos^ 
 sils of these strata are Favosites polymorpha, Holy sites catenulatus, DipTiy* 
 
 phyttvm f Strophomena rhomboidalis, S. f a variety of 
 
 Pentamerus galeatm, Spirifera crispa, 8. radiata, Atrypa reticularis f 
 and an undescribed Pleurotomaria ; all of Middle Silurian age. 
 
 On the Matapedia Kiver, between the lake and the Devil's Elbow, a 
 bend about three miles beyond the Causapscal, the whole of the Gaspe* 
 and limestones are met with ; but the absence of observed fossils makes it 
 difficult to compare the different portions with the section of Cape* 
 Gaspe*. The entire distance is about seventeen or eighteen miles ; in th& 
 first part of which, to the Umpui, there are no exposures. In the remain- 
 der of the distance, there are many intervals of concealment ; but, judging 
 by the strata which are visible, the masses, in succession, seem to be dark 
 grey calcareous shales, occasionally nearly black, terminated by dark grey 
 limestones, weathering to a rusty yellowish-brown. This mass is succeeded 
 by a grey hard, compact, and somewhat gritty calcareous slate, weathering 
 to a yellowish-white. The slate has a cleavage independent of the bedding ? 
 and the thinness and closeness of the strata, with their slight differences of 
 color, often give to the planes of cleavage a ribbon-like aspect. Following 
 these, black soft calcareous slates occupy the river for two and a half milea 
 above the Causapscal ; succeeded below it, by dark grey calcareous slates^ 
 weathering whitish and yellowish, with occasional beds of black limestone- 
 
 About a mile and a half south from the Causapscal, on the Campbelltown 
 road, the calcareous series is followed by grey argillaceous slate, weathering 
 to olive-green, and sometimes to opaque white, perhaps where affected byr 
 fire. The mass, which does not appear to be calcareous, occupies a mile sandstones, 
 and a half on the road, and then gives place to a succession of arenaceous 
 strata, representing the Graspe* sandstones. These occupy the road for 
 about six miles, and consist of greenish-grey or drab sandstones and arena* 
 ceous shales, with occasional layers of red and purplish-grey. Some of 
 the surfaces are ripple-marked, but no carbonized remains of plants have 
 been observed upon them. On the Matapedia, which is a short distance 
 to the westward of the road, the breadth of the sandstones is. somewhat 
 less than six miles. The dips at the opposite extremes of the distance, 
 indicate that the strata lie in a synclinal form ; on the axis of which, it 
 seems probable that they will be found to crop out to the westward, at no 
 very great distance. They do not reach the Patapedia, which ia distant 
 about twenty miles in that direction. 
 
416 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Great Metis 
 Hirer. 
 
 Limestones. 
 
 SECTION OP THE GREAT METIS AND PATAPEDIA RIVERS. 
 
 From the upper end of Lake Matapedia, the base of the Gaspe* limestones 
 turns southward of west, following the valley of one of the tributaries of 
 the lake for five or six miles ; and thence reaches the Great Metis River, 
 which it crosses at a distance of fifteen miles from the St. Lawrence. 
 On this river, a little below the mouth of its tributary, the Musquege- 
 gish, large loose angular blocks of fine grained white sandstone are abun- 
 dant ; but the beds from which these are derived are concealed. At the 
 mouth of the tributary, however, the overlying calcareous rocks make 
 their appearance. With a dip of S. 66 E. < 45, they present an escarp- 
 ment of about twenty feet high, and consist of grey nodular limestone, 
 divided into beds of two and three feet. The rock is fossiliferous, but the 
 fossils are difficult to extract. In one of the fragments, at the foot of the 
 escarpment, were however obtained a Pentamerus resembling P. KnigUii, 
 a Strophomena resembling S. incequistriata, and another species, which is 
 resupinate and resembles S. punctulifera. 
 
 Farther up the Great Metis, at a distance of about 850 yards at right an- 
 gles to the strike, another exposure occurs. Here the beds consist of lime- 
 stones of the same character as before, interstratified with greenish shale; 
 the dip being S. 65 E. < 30. About fifty chains farther up, strat#are 
 again met with; but here the dip is N. 75 E. < 2-6. These beds 
 consist of dark grey argillo-calcareous shale, interstratified with greenish 
 layers. At the base, a bed of about three feet thick, consists of greenish 
 arenaceous limestone, and contains obscure fossils, one of which resembles 
 Pentamerus oblongus. These three exposures are supposed to overlie one 
 another ; and the total thickness, with what is concealed, is computed to be 
 about 2000 feet. 
 
 Kiyer Rouge. For two miles above this, no exposures occur ; but in the succeeding two 
 and a half miles, to its tributary, the Rouge, several are met with. The 
 first one consists of greenish arenaceo-calcareous shales, and the others 
 of grey micaceo-arenaceous limestones or strongly calcareous sandstones, 
 well fitted for flagging stones, interstratified with purplish-brown arenaceo- 
 calcareous shale. Masses of similar characters constitute the rocks of the 
 falls between the Rouge and the Metis lakes, and near the lowest lake. 
 Both above and below the Rouge, they show various and sometimes opposite 
 dips, occasionally with very high angles. In a part of the distance, the 
 rocks exhibit a cleavage independent of the bedding, and it is often difficult 
 to distinguish the one from the other. It has, in consequence, as yet been 
 found impossible to compute their thickness ; but from the amount of cal- 
 careous matter which they contain, these strata are supposed still to belong 
 to the Gaspe* limestones, and to represent a higher portion than those 
 mentioned above. 
 
CHAP. XVI.] DISTRIBUTION OP THE GASP SERIES. 417 
 
 No rocks have been seen on Lower Metis Lake ; but strata are met with Metis lakes. 
 in several places in the upper half of the middle lake ; consisting of 
 grey granular limestones, weathering brownish-yellow, and containing 
 obscure fossils. The beds are from six to twelve inches thick, and are 
 interstratified with less calcareous layers, greenish-grey in color and 
 weathering brown. An obscure cleavage exists in the less calcareous 
 layers, and they separate with difficulty in the direction of the beds. These 
 strata, with several minor undulations, appear to preserve a general horizon- 
 tality, and they are supposed to be a repetition of the lower part of the 
 Gaspe* limestone series. 
 
 The shores of Upper Metis Lake are strewed with many large flat frag- 
 ments of calcareo-arenaceous shale, mixed with sandstone ; and in one place, 
 the bottom of the lake is paved with a greenish sandstone, interstratified 
 with greenish shale : the beds appear to be horizontal. After passing the 
 water-shed, an exposure, about half-way down the Awaganasees, consists of 
 greenish calcareous sandstones, in beds of from six to eight inches, dipping 
 N. 3 W. < 24. Below this, to within a mile of the Patapedia, there 
 appear flagstones, very similar in character to those below the Lower Metis 
 Lake, and near the Rouge, except that they are more even and regular 
 in their divisional planes. In some parts, the thicker slabs are separated 
 by calcareous slates, which split into large and remarkably even plates, no 
 more than the eighth of an inch thick ; of a dark grey internally, but chang- 
 ing rapidly in the weather to a greyish-yellow or light drab. Rocks of a 
 similar character, but not so evenly bedded, prevail for the remainder of 
 the distance to the Patapedia. They are considered to be a repetition 
 of the upper part of the Gaspe* limestone series, to which we here assign 
 a total breadth of between fourteen and fifteen miles. 
 
 Between the mouth of the Awaganasees and Indian Rivers, and half a 
 mile below the latter, the rocks are dark grey compact thin-bedded lime- Biver - 
 stones, interstratified with blackish calcareous slates. These recur twice, 
 and on each occasion are followed by dark grey calcareous slates. Below 
 this, for seven miles, as far as Pollard's Brook, there prevails a greenish- 
 grey arenaceous slate, which weathers yellowish-brown, and is sometimes 
 calcareous. At this brook, and for a short distance below it, there is 
 a recurrence of dark grey calcareo-argillaceous finely laminated slates, 
 splitting into large slabs about the thickness of roofing slates, and weather- 
 ing to a greyish-yellow or drab, like those of the Awaganasees. With the 
 exception of these drab-weathering strata, the prevailing rocks, for five 
 miles below Pollard's Brook, are dark grey argillaceous slates, interstratified 
 with occasional non-calcareous layers. For six miles farther, the rock 
 is a dark grey calcareous slate, interstratified, in the last two miles, with 
 more calcareous bands. For a mile and a half farther, thin-bedded black 
 limestones occur a third time, interstratified with black and dark grey 
 
 BB 
 
418 GEOLOGY OF CANADA. [CHAP. XVI. 
 
 argillaceous slates ; beyond which, the only rocks, for two miles, to the 
 junction of the Patapedia with the Restigouche, are dark-grey calcareous 
 slates, interstratified with arenaceous and greenish sandstones. 
 
 In all of these rocks on the Patapedia, there is a cleavage independent 
 of the bedding, and it is often very difficult to distinguish the one from 
 the other. Occasionally the strata are much contorted ; and it has been 
 found impossible, up to the present time, to determine what may be their 
 thickness, or the number of repetitions of equivalent groups of strata. No 
 fossils have been found in these rocks ; and it is difficult at present to 
 establish their age ; but they are not supposed to be older than the Gaspe* 
 limestones. 
 
 SECTION ON THE RIMOU8KI RIVKR. 
 
 From the Metis River, the base of the Gaspe* limestones continues its 
 course south of west, parallel with the margin of the St. Lawrence, at the 
 distance of fifteen miles ; then sweeping around the western extremity 
 of Mont Commis, it approaches to within ten miles of the St. Lawrence. At 
 this distance, it again runs parallel with it for about five miles, across one 
 half of the township of Neigotte, and then makes another sweep forward, 
 towards the front of Macpes ; reaching the Rimouski River at a point about 
 nine miles, in a straight line, from its mouth. The base of the Gaspe* 
 limestones are, however, not more than seven miles from the coast, between 
 Rimouski and Bic. 
 
 KimouBki On the right bank of the Rimouski, the rocks of this series rise in a well- 
 
 Rlver> marked escarpment, over a hundred feet high. The rock at the base is a 
 
 whitish-grey calcareous sandstone, of which between twenty and thirty feet 
 are seen, dipping S. 39 E. < 7 -9. This is succeeded by beds of 
 bluish argillaceous limestone from six inches to two feet thick, which 
 constitute the remainder of the escarpment. Limestones of a similar char- 
 acter are mot with at intervals, for about five miles up the Rimouski, to a 
 large marsh, on the fourteenth lot of the third range of the township of 
 Duquesne; which would bo about two and a quarter miles across the 
 measures. The dip is hero S. 60 E. < 45, and the rock is a dark groy 
 calcareo-argillaceous slate, interstratified with greenish .calcareous sand- 
 stones, in beds of from one to two inches thick. To the south of the marsh, 
 a ridge rises to the height of about 150 feet, having at its southern base a 
 valley ; which on the east side of the river contains Lake Macpes and its 
 discharging stream, and on the west, the river Touradiff. This depression 
 is over half a mile from that of the marsh, and the rocks seen in it are 
 much the same as those just described, with perhaps a somewhat smaller 
 quantity of slate : the dip is S. 59 E. < 30. 
 
CHAP. XVI.] DISTRIBUTION OP TIIE GASPfi SERIES. 419 
 
 A milo and a quarter above this, there is another depression, occupied, 
 on the west side, by the Riviere France ; and two and a half miles farther 
 up, we have the fall of the Rimouski, on the twenty-fourth lot of the sixth 
 range of Duquesno. The rook at the fall is a greenish-grey calcareous J<a11 ' 
 sandstone, in beds of two or three inches, separated by grey calcareous 
 shale ; the shale and the sandstone being about equal in amount, but 
 irregularly intcrstratified. The dip at the fall is S. 44 E. < 60 ; but 
 just below it, there occurs a small undulation, by which the same beds are 
 kept at the surface for a distance of about forty-five yards across the 
 measures. The Rimouski, for a considerable distance below the fall, flows 
 in a very deep and inaccessible chasm. The strata, in consequence, have 
 been examined only at considerable intervals ; and if there should bo many 
 undulations similar to that at the fall, these would materially diminish the 
 thickness to be deduced from the ascertained dips. 
 
 About a hundred yards below the fall, the rock is very evenly divided 
 into bods of from one to four inches thick, and would yield excellent flag- 
 stones, two to three feet wide, and from four to six foot long. They 
 very much resemble the flagstones already described on the Metis, and 
 their stratigraphical place may very probably bo the same. Fossils have 
 been observed in several parts of the series, but the only one that can bo 
 identified is a pear-shaped variety of Favosites basaltica. 
 
 No exploration has yet been made farther up the Rimouski, nor has the 
 base of this series of limestones been consecutively traced, with accuracy, 
 farther west. After crossing the Rimouski, the base appears to keep on 
 the south side of its tributary, the Little Rimouski, very nearly to the 
 water-shed between it and the eastern tributaries of the Trois Pistoles 
 River. Here, turning more southward, it runs a course about parallel to the 
 Tuladic, and comes upon Lake Temiscouata. 
 
 SECTION OF LAKH TEMISCOUATA AND THE MADAWA8KA UIVKR. 
 
 That part of Lake Temiscouata which is above Fort Ingall, extends to 
 the north-eastward, with the strike of the rocks, and at right angles to its 
 lower part. This lower portion, with the Madawaska River, to Little 
 Falls, and the St. John in continuation, to the vicinity of Woodstock, afford 
 a transverse section of the strata. 
 
 The upper part of the lake, on the north-west side, gives a fuller develop- 
 ment of certain strata, which occupy the last two and a half miles on the 
 Temiscouata Portage road, and which, at the time of examination, in 1849, it 
 was supposed might possibly belong to the Devonian series. As soon above 
 Sandy Point, which is four and a half miles from Fort Ingall, they consist 
 
420 GEOLOGY OF CANADA. [CHAP. XVI. 
 
 shales and of grey slaty limestones, splitting into thin firm laminae, apparently in the 
 
 limestones, direction of the beds ; which are nearly vertical, and would yield excellent 
 tiles and flagstones. Lower down the lake, grey clay slates are inter- 
 stratified with calcareous sandstones, which weather to a yellow earth or 
 rotten-stone : in some parts, nodules of a similar character occur. In 
 addition to these strata, clay slates, sometimes lead-grey, or of a darker 
 hue, are found, interstratified with thin bands and lenticular masses of a 
 fibrous or columnar limestone ; the fibrous structure running at right 
 angles to the beds, and quite across them. These slates and limestones 
 prevail, not only on the north-west side of the lake and for a mile above, to 
 the mill on Mill Brook ; but they are seen extending along the south-east 
 side of the lake, from its head, to a point immediately opposite Mill 
 Brook. Here, there is some irregularity in the structure, and the grey 
 slates are associated with beds of grey calcareous sandstone and of arena- 
 ceous limestone, with dark banded green slates. 
 
 Beds similar to these, occur to the north-west of the Shickshock 
 mountains, on the Chatte River ; and the peculiarity of the fibrous structure 
 of the limestones in both places is so striking, as to induce the supposition 
 that the rocks in the two localities must be equivalent. The strata on 
 Temiscouata Lake having been classed with the Devonian series, those on 
 the Chatte were placed in the same horizon ; and they were so represented 
 on a small map published in Paris, in 1855, to illustrate a sketch of the 
 
 Quebec group, geology of Canada. The light recently thrown on the Quebec group by 
 the fossils discovered at Point LeVis, however, leads us to suppose that 
 these strata on the Chatte, and on Lake Temiscouata, belong to the base of 
 this group. 
 
 Mount After proceeding for three fourths of a mile to the south-east, transverse 
 
 to the strike from these lower rocks, we come upon the higher strata 
 which constitute Mount Wissick or Mount Lennox. This mountain rises 
 on the north-east side of Lake Temiscouata, and consists of the following 
 strata in ascending order : 
 
 Feet. 
 
 Whitish massive sandstone, of a moderately fine grain, , 45 
 
 Conglom- Grey coarse calcareous conglomerate ; the matrix is a greenish sand, and 
 crates, holds a large amount of angular fragments, and some rounded masses of 
 grey limestone, with a much smaller number of quartz pebbles. No fos- 
 sils have been observed in the enclosed portions of limestone, 20 
 
 Measures concealed, 90 
 
 Ked and Green sandstone, with a few conglomerate bands similar to the previous one, 20 
 green shales. R e d an d green shale in alternating bands, none of which were observed to 
 be calcareous. There are three successive exposures of this shale, with 
 fossiliferous limestones between them ; but two of these are supposed, 
 from differences in the strike, and from one observed anticlinal, to be 
 repetitions ; the shale being subjacent to the limestones, 125 
 
CHAP. XVI.] DISTRIBUTION OF THE GASPfi SERIES. 421 
 
 Feet. 
 
 Grey nodular limestone, abounding with fossils ; among which are Favosites Limestones, 
 
 Gothlandica, Atrypa reticularis, and an undescribed species of Pentamerus. 
 The limestone presents a vertical columnar structure, due to two sets of 
 
 joints, which divide the beds into irregular rhombic prisms, 60 
 
 . Grey hard sandstone, without observed fossils, 10 
 
 Grey fossiliferous limestone with a columnar structure, 20 
 
 Grey arenaceous limestones and sandstones, with fossils at the base and 
 summit, and probably throughout. Some of the beds have very little 
 carbonate of lime, and many have none at all. This constitutes the 
 main body of Mount Wissick, and its thickness is estimated from the 
 height of the mountain, which is 550 feet. No rocks were seen for 
 a considerable distance, across the measures, from the band of grey 
 sandstone above mentioned, 500 
 
 880 
 
 The dip of these strata is S. 50 E. < 13 ; and to the middle of the 
 valley between Mount Wissick and the next ridge running to Black Point, 
 there would, if the dip remains constant, be room for 1000 feet above 
 them. No exposures of strata however appear on either side of the lake, to 
 tell of what the interval may be composed ; and between the middle of the 
 valley and the rock of Black Point, there is another concealed interval, 
 whose breadth, directly across the measures, would be 400 yards, equal to 
 276 feet more in thickness. 
 
 Black Point, and Burnt Point, which is opposite, consist of a very coarse Black Point; 
 conglomerate, composed chiefly of pebbles of quartzite and limestone, con g lomerate - 
 the former prevailing. The colors of the quartzite pebbles, which occa- 
 sionally hold a few spangles of mica, are green and grey, but principally 
 green, and some of them are from six to eight inches, and even a foot in 
 diameter. The calcareous pebbles generally weather to a yellowish tint ; 
 but many of them remain grey, while some of the pebbles consist of red 
 slate. The matrix of the rock is a sandstone of a dark grey color, which 
 appears to be slightly calcareous. The first or lowest band of this con- 
 glomerate is about 400 feet thick ; and it is followed by others, varying from 
 one to sixty feet, which are separated by beds of sandstone of from one to 
 fifteen feet thick. The whole breadth of these coarse rocks is about 400 
 yards, and the dip remains very uniformly S. 63 E. < 51 - 56 ; which 
 would give a total thickness of very nearly 1000 feet. 
 
 This conglomerate rock constitutes a sharp and prominent ridge, which 
 can be traced, as viewed from the summit of Mount Wissick, running far 
 into the country north-east of the lake, on the north-west side of the 
 Tuladie River ; whose course is very probably guided by it for ten or 
 twelve miles. From the same height, the fossiliferous range to which the 
 mountain itself belongs, can be seen extending in a parallel line for up- 
 wards often miles ; the last visible eminence in the range bearing N. 23 E. 
 
422 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Cabineau 
 Biver. 
 
 Slates and 
 sandstones. 
 
 On the west side of the lake, the fossiliferous band is not so conspic- 
 uous, nor so clearly traceable, but it is supposed to direct its course to 
 a hill to the north of the Cabineau River, in the bearing S. 23 W. ; while 
 the conglomerate will probably be found in a better marked ridge, which 
 occupies the south side. 
 
 In the lowest four miles of the Cabineau River, where strata interme- 
 diate between the conglomerate and the fossiliferous limestone might be 
 expected, there appear to be only two exposures of rock. The first, nearly 
 three miles from the mouth, consists of grey thin-bedded contorted lime- 
 stones, without fossils ; and the second, half a mile beyond, of green slate, 
 banded with black, and interstratified with pure limestone bands, also with- 
 out fossils. Except that these limestones are not fibrous, the measures 
 resemble the lower strata on the north-west side of the lake. 
 
 Beyond the conglomerates of Black Point, the next rock exposed is a 
 grey soft scaly argillaceous slate, becoming a little lighter in color under 
 the action of the weather, which splits it into small flat fragments. On 
 the west side of the lake, it occupies about three quarters of a mile, in the 
 distance of a mile and a half, across the measures, and it probably forms 
 the bed of the Tuladie, a few miles up from its mouth. This slate may be 
 much contorted, and it is for the present impossible to state its thickness. 
 
 The rocks which immediately succeed this slate on the west side of the 
 lake, are given in the following horizontal section, whose distances corre- 
 spond to a line at right angles to the general strike : 
 
 Yds. Yds. 
 
 Grey argillaceous scaly slates, of the same kind as described above, 
 interstratified with bands of sandstone, varying in thickness from 
 an eighth of an inch to one inch. Some of the beds are partially 
 calcareous, and they are generally cut by veins of quartz, not exceed- 
 ing the thickness of paper, 31 
 
 Measures concealed, 14 
 
 Grey argillaceous slates, with sandstones as before, 69 
 
 Measures concealed, but supposed to be the same, 13 
 
 Measures concealed, but so thickly covered with large angular blocks of 
 a light grey sandstone with a greenish tinge, that there is little 
 
 doubt that this rock is present beneath, in thick beds, 24 
 
 Light grey sandstone slightly tinged with green, of the same character 
 as before, but in thick beds. It is hard and fine grained, approach- 
 ing a granular quartzite, and is in a slight degree calcareous. The 
 
 dip is S. 63 E. < 83, ? 
 
 Measures concealed, but probably the same description of sandstone, . . 38 
 Light grey sandstone of the same character as before, with a few beds 
 
 of slate separating the layers, 9 
 
 Measures concealed, 7 
 
 Light grey sandstone as before, weathering of a lighter grey than the 
 
 interior color, 10 
 
 Grey argillaceous slate, becoming green, and crumbling under the 
 influence of the weather, 1 
 
 223 
 
CHAP. XVI.] DISTRIBUTION OF THE GASPE" SERIES. 423 
 
 Yds. Yds. 
 
 Dark grey hard argillaceous sandstone, slightly calcareous. It has a 
 greenish hue within, and weathers more green externally ; there 
 are a few quartz pebbles at the bottom of the bed. Fragments of 
 the rock held in a proper light, show a peculiar reflection, from the 
 symmetrical arrangement of crystalline grains of calcite or of 
 dolomite, 10 
 
 Dark grey tough argillaceous sandstone, like the last, without any cal- 
 careous matter ; alternating with beds of jasper, the color of which 
 in some layers is a uniform purplish black, 10 
 
 Measures concealed, probably beds of a similar kind to the last, and Pointe aux 
 
 constituting Pointe aux Trembles, 30 Trembles. 
 
 Greenish tough argillaceous sandstone^ alternating with beds of a uni- Jasper beds, 
 
 form purplish brown jasper. The sandstone beds have grains of 
 red in them, but their general tint is green, 25 
 
 Measures concealed, 86 161 
 
 Greenish tough argillaceous sandstone ; in some parts it holds a few red 
 pebbles, and others of grey and greenish hues. The pebbles are very 
 obscure, and tightly soldered into the matrix ; fractures go through 
 both without deflection, 18 
 
 Measures concealed, 18 
 
 Greenish tough sandstone as above ; the occasional presence of pebbles 
 is more observable than before, and they sometimes stand up in re- 
 lief on the surface ; the rock towards the top partakes of a conglom- 
 erate character. Some of the pebbles are from five to six inches 
 in diameter, and they are all highly crystalline, appearing in gen- 
 eral to be from metamorphic rocks. The matrix, which is not very 
 fine, continues to be a mixture of red and green grains, giving a 
 green tinge in the aggregate. Some of the interstratified bands are 
 of a darker hue than the general mass, approaching to an iron-grey, 
 
 but weathering to a yellowish-white By these bands, and by others Epidotic rock, 
 
 of a deep purplish-red slate, the dip, which is S. 56 E. < 76, can 
 be readily distinguished. There are thin vertical transverse veins of 
 epidote cutting some parts, and the same mineral seems to exist 
 also as a constituent of portions of the rock. There is*a very regular 
 set of joints in the rock, of which the underlie is N. 85 W. < 22J, 96 132 
 
 516 
 
 These rocks constitute two points on the west side of the lake. The 
 upper one, called Pointe aux Trembles, just opposite the Tuladie River, is 
 very conspicuous. The second point is of no importance in the configura- 
 tion of the coast, but it runs back into a ridge, with a valley on each side 
 of it, which marks well the course of the sandstone composing it. It is Quebec group, 
 probable that the conglomerate of Black Point, and the chief part of 
 the strata included between it and Pointe aux Trembles, may belong to the 
 Quebec group. These, from their highly inclined attitude, as contrasted 
 with the moderate dip of the rocks of Mount Wissick, would appear to 
 underlie the Gaspe* limestones unconformably ; but not having yet been 
 traced out to any distance on the strike, it will require further investigation 
 before their relations can be completely understood. 
 
424 GEOLOGY OP CANADA. [CHAP. XVI. 
 
 The rocks of the second point would come upon the section about five 
 hundred and forty yards, at right angles to the strike, from the last 
 described sandstones. The intervening strata, judging by the first rocks 
 seen on the south side of the Tuladie, at a corresponding point, would prob- 
 ably be calcareous slates of a bluish-grey color and fine texture, with 
 some thin bands and patches of a coarser grain. The stratigraphical 
 divisions of these slates are obliterated by cementation, and it is only by 
 slight differences of color that the beds can be distinguished. These 
 strata are followed by grey slates, which are not calcareous, and appear to 
 be slightly micaceous. They weather to a dull dark olive-green, and cleave 
 into very thin leaves. These alternate with, and pass into a grey tough, 
 feebly calcareous sandstone, which is fine grained, slightly micaceous, 
 and has a dull granular earthy fracture. They all weather greenish, 
 where washed by the water and spray of the lake ; but surfaces removed 
 from the lake, and denuded of moss and trees, are often of a dull white, 
 with a reddish-yellow tinge, perhaps the result of the action of fire. The 
 beds succeeding the calcareous slates, have a transverse measure of 290 
 yards : their dip, where it could be determined, was S. 55 E. < 50. 
 
 The next five miles across the measures, are occupied, on the west side 
 of the lake, by calcareo-argillaceous slates, occasionally interstratified with 
 non-calcareous bands, which are more or less arenaceous. The colors are 
 dark bluish-grey, light grey, and black ; and the divisions of the original 
 bedding have become very much obscured ; so that in fresh fractures, it is 
 only by different shades of color, that the stratification can be made out. 
 The action of the weather and water on the ice-rounded surfaces upon 
 the lake, however, distinctly shows the bedding, by the unequal wearing 
 contorted of the more and less calcareous layers. The beds are almost always 
 thin, and the surfaces display a great variety of the most complicated 
 contortions ; sometimes in folds, to the north-west, and sometimes in invo- 
 lutions, which it is impossible to understand, without a larger exposure 
 than usually occurs. Combined with these contortions, there are often 
 disruptions or dislocations ; which, however, show no veins of foreign 
 matter. The torn and twisted mass has been apparently compressed 
 together, and cemented in such a way, that, except for the colors or the 
 unequal weathering, it would never be suspected that it had been dis- 
 turbed. In some parts, however, the contorted rocks are cut up by a 
 multitude of small veins of calcareous spar. The figure on the next page 
 represents the contortions and dislocations upon a surface on which no 
 veins, whatever, appear. 
 
 In the vicinity of Little Island, which stands opposite to Grand Bay, in a 
 section of three quarters of a mile across the measures, including the island, 
 no calcareous matter is found in the slates, which weather of a greener color 
 than the beds farther up. There is a small amount of carbonate of lime in 
 
CHAP. XVI.] 
 
 DISTRIBUTION OF THE GASPfc SERIES. 
 
 425 
 
 the hard bands, which are very thin sandstones. The calcareoargilla- 
 ceous slates then appear again, and continue for a mile and a half farther. 
 The remaining distance, to the exit of the lake, another mile and a half, 
 transverse to the general strike, shows occasional thicker beds of sand- 
 stone ; with grey calcareo-argillaceous slates, holding thin calcareous sand- 
 stones, and black and dark grey non-calcareous beds. The last exposure, 
 just at the exit, on the right bank of the Madawaska, consists of non- 
 calcareous sandstones and slates ; which are grey internally, but weather 
 to a dull olive-green, resembling those near the Tuladie River. The beds 
 are all slightly micaceous ; the slates more so than the sandstones. 
 
 About half a mile down the Madawaska, where the rock comes close 
 upon the river, the same grey, greenish-weathering slate is seen, with thin Biver> 
 
 431. SECTION OF SLATES ON LAKE TEMISCOUATA. 
 
 Scale about $. 
 
 light colored slightly calcareous bands marking the bedding. The expo- 
 sures on the river, all the way to Little Falls, at its junction with the 
 St. John, are not numerous. They consist pretty uniformly of the same 
 slates and sandstones as before, the slates greatly predominating, and oc- 
 casionally holding a small amount of calcareous matter. At Little Falls, Little Fails, 
 the color of the rock is grey internally, weathering generally to a 
 dull obscure olive-green, sometimes so dark as to give it a chloritic aspect. 
 The slate, which is micaceous, is interstratified with occasional hard com- 
 pact bands, cleaving with difficulty, and possessed of sufficient grit to 
 entitle them to the name of sandstones. 
 
 BOCK8 ON THE WALLOOSTOOK OB ST. JOHN BIVEB, AND SOHE OV ITS TBIBUTABIES. 
 
 Slates and sandstones, similar to those at Little Falls, are seen farther 
 down on the St. John, near its tributary, the Squesibish ; where there is 
 a transverse exposure of 200 or 300 yards. Here the slate, internally 
 
426 GEOLOGY OF CANADA. [CHAP. XVI. 
 
 grey, weathers greenish, and is interstratified with bands of feebly calca- 
 reous sandstone, some of which are from four to twelve inches thick. The 
 bedding is well displayed at this place, and a few contortions in the strati- 
 fication are visible. 
 
 Shiguash. Still lower down, and about a mile and a quarter above the mouth of 
 another tributary, the Shiguash, a band of coarse conglomerate, which 
 crosses the road, bears a strong resemblance to that of Black Point, on 
 Lake Temiscouata, and holds a great amount of large pebbles and small 
 boulders of black limestone, weathering to an ash-grey. Some of the cal- 
 
 congiom- careous boulders are themselves of a conglomerate character, holding peb- 
 bles of a stratified rock, while their matrix includes organic remains. 
 With the calcareous portions of this conglomerate band, are mingled 
 others of black jasper and of chalcedonic quartz : with these, were observed 
 
 serpentine several pebbles of a blackish-green serpentine. The matrix is a hard 
 
 pebbles. calcareous sandstone, with grains of white and colored quartz : it is grey 
 internally, and weathers to a yellowish tinge. Vertical beds of the 
 conglomerate, running N. &0 E., alternate with beds of a sandstone sim- 
 ilar in character to the matrix : a breadth of seventy-five yards is visible, 
 giving a thickness of 225 feet. As the strata above and below are 
 concealed, the volume may be greater, particularly to the south-east; 
 where the ground rises in a small hill, for a quarter of a mile. At this 
 distance, the conglomerates are followed by calcareous slates, which at 
 first are interstratified with a few bands of sandstone, resembling that 
 associated with the conglomerate, but, farther on, display strongly calca- 
 reous beds, weathering to a rotten-stone. Sometimes the slates, without 
 being themselves calcareous, are interstratified with slightly calcareous 
 sandstones. These alternations are occasionally visible for about 500 
 yards ; between which and the Shiguash, there are no exposures on the 
 road. The examination in this vicinity has not been carried farther. 
 
 Rocks similar to those of the lower part of the Madawaska and the 
 Squebish, prevail along the St. John, as far as the St. Francis, and even 
 to the Black River, twenty miles higher. Both the slates and the sand- 
 
 st. Francis stones are in general micaceous, and occasionally calcareous. On the St. 
 Francis, no traces have been found of the Black Point conglomerates, or 
 of the jasper rocks of Pointe aux Trembles ; nor have we been successful 
 in meeting with the fossiliferous limestones of Mount Wissick, though 
 the distance from Temiscouata is scarcely more than twenty-two miles. 
 The lowest exposure belonging to the Quebec group, on this river, con- 
 sists of a coarse greenish chloritic sandstone, associated with green slates. 
 It occurs just to the north of the province line, at the foot of a lake called 
 by the Indians, Wollenabe'geg : below this, the country appears to consist 
 chiefly of clay slate. The most calcareous ridge met with, occurs about 
 three miles above another lake, which is called by the Indians, BatteVich- 
 
CHAP. XVI.] DISTRIBUTION OF THE GASPfi SERIES. 427 
 
 cagameg. The rocks of this ridge, however, shew no fossils, and they do 
 not hold a sufficient quantity of carbonate of lime to entitle them to the 
 name of limestones. A mountain on the north-east side of this lake, displays 
 some strong beds of sandstone, associated with bluish-black or dark grey 
 slates, both slightly micaceous ; but the sandstones alone are somewhat 
 calcareous. Similar micaceous sandstones, sometimes holding a little 
 carbonate of lime, prevail to the mouth of the lake. 
 
 On the Black River, twenty miles above the St. Francis, there occur Black River, 
 the same grey micaceous slates and sandstones, occasionally calcareous. 
 The sandstones weather greenish, and, where washed by the water, acquire 
 a slightly reddish tinge. Large angular blocks of a calcareous conglomerate 
 are occasionally met with ; but the rock, in situ, does not occur below the 
 province line. Both below and half a mile above this line, calcareous slates 
 occur, with black or dark grey coarse limestone bands ; and half a mile congiom- 
 above this, there is seen a conglomerate, of which three exposures occur erate ' 
 in a breadth of 300 yards. It holds boulders of a fine silicious conglomerate 
 and of grey quartzite, with blackish vitreous quartz grains and fragments 
 of green slate. The matrix appears to be composed of this green rock 
 in a comminuted state, with a fine grey slate. The fact that this conglom- 
 erate itself contains pebbles of an older conglomerate rock, resembling 
 some portions of the Sillery series, connects it with the conglomerate of 
 Black Point, on Lake Temiscouata, and with that near the Shiguash ; which 
 last encloses pebbles of serpentine. These characters suggest the prob- 
 ability, that all of these conglomerates may be newer than the Quebec 
 group, the sandstones of which were seen between three and four hundred 
 yards farther up the Black River. They were examined for a distance of smery series, 
 about a mile and a quarter, and resemble those of the Sillery series ; being 
 greenish, massive, and coarse grained, with scales of mica and of graphite, 
 and interstratified with occasional bands of red slate. 
 
 SECTION OF THE CHAUDIERE RIVER. 
 
 We have already stated that in the valley of the Chaudidre River, the 
 Quebec group is limited to the south, by a series of Upper Silurian strata. 
 These appear in the parish of St. Francis, a few miles above the Guillaume 
 River, and consist of dark grey and black clay slates, interstratified with a 
 few beds of sandstone. Similar beds prevail as far as the vicinity of St. vaudreuii, 
 Francis church, in the seigniory of Vaudreuil, Beauce ; and at the turn in 
 the river, some distance above, there is met with a light grey calcareous 
 bed, overlaid by a massive feldspathic sandstone. This is followed, higher 
 up, by dark grey clay slates, with quartzite bands of the same color, fol- 
 
428 GEOLOGY OF CANADA. [CHAP. XVI. 
 
 lowed by impure blackish limestones. Three hundred yards farther, occurs 
 another band of feldspathic rock similar to that just mentioned, and having 
 the aspect of a fine conglomerate. Beyond this band, which is about a 
 mile and a half above the church, the prevailing rock is clay slate. 
 
 On the Touffe des Pins, about a mile above its mouth, these clay slates 
 are bluish-black, striped with a lighter color. They are occasionally slightly 
 calcareous, while the somewhat feldspathic interstratified sandstones, are 
 
 Famine strongly so. These slates preserve the same character up to the river 
 
 Bdver * Famine, where, with a dip S. 37 E. < 65, they plunge beneath a grey 
 slaty micaceous limestone without fossils, succeeded, about fifty yards to 
 the southward, by dark fossiliferous limestones, not exceeding from ten to 
 twenty yards in breadth ; which form a low short ridge, overlooking the 
 Famine. The fossils have a Devonian aspect : among them are Favo- 
 sites G-othlandica, F. basaltica, Syringopora Hisingeri, Diphyphyllum 
 arundinaceum, an undetermined Zaphrentis, Heliophyllum Oneidaense, 
 Orthis striatula, Strophomena rhomboidalis, two undetermined species of 
 Chonetes, a small Productus, like an undescribed one occurring in the 
 Corniferous formation ; Spirifera duodenaria, S. gregaria, S. acuminata, 
 Atrypa reticularis, and a Cyrtia like 0. ro strata. 
 
 Approaching the mouth of the RiviSre du Loup, the proportion of sand- 
 stones somewhat increases, and continues to do so for three miles up 
 
 jersey Fall, this tributary, as^ well as up the ChaudiSre to the Great or Jersey Fall. At 
 this fall, there is a considerable exposure, measuring about 150 yards across 
 the strata, which appear to dip S. 37 E. < 62. The beds consist chiefly 
 of grey sandstones, some of which are schistose, and approach to a coarse 
 mica slate, while others are massive. They weather to a greenish tinge 
 when above the water-line ; but where washed by occasional floods, they 
 have a reddish cast. These sandstones are interstratified with calcareous 
 beds, which are harsh and gritty to the touch, and contain a great proportion 
 of sand ; none of them would burn to lime. Other and thinner bands 
 are blackish on the exterior ; and these, which are smoother than the rest, 
 are soft and wear into grooves ; while the sandstones stand out in relief. 
 The black bands are finely laminated, and split into brittle plates, with 
 glossy surfaces. The sandstones weather to a lighter grey than the cal- 
 careous beds, some of which approach to a pale olive-green color on the 
 exterior. A quarter of a mile below the fall, there is another exposure of 
 similar strata, with some more highly calcareous beds. 
 
 Riviere du Rocks related in character to those given above, consisting of fine and 
 coarse grey micaceous clay slates, with grey micaceo-argillaceous sand- 
 stones, which weather greenish in the air, and become reddish and very 
 smooth where exposed to running water, occur much farther up the RiviSre 
 du Loup and the ChaudiSre ; reaching near to the province line on the one 
 hand, and to Lake Megantic on the other. The information collected in 
 
CHAP. XVI.] DISTRIBUTION OF THE GASP SERIES. 429 
 
 regard to these rocks is not yet sufficiently detailed to enable us to give a 
 connected description of them. Both above and below the junction of the ciay elates, 
 two rivers just named, the clay slates are often observed to have a cleavage 
 independent of the bedding ; and they will, in some places, very probably 
 yield material fit for roofing. On the Riviere du Loup, about half a mile 
 above its mouth, a band of the rock, exceeding half a mile in breadth, would 
 in several parts afford both roofing and writing slates, as well as excellent 
 flagstones. Of the latter, good even slabs may be obtained of five and 
 six feet in length, by three or four in width, with a thickness of from two 
 to three inches. 
 
 BOCKS OP THE ST. FRANCIS AND SOME OP ITS TRIBUTARY LAKES AND EIVER8. 
 
 From Yaudreuil, Beauce, on the Chaudidre, the base of the Upper 
 Silurian clay slates, in its course south-westward, reaches the north or 
 lower end of Lake St. Francis. Here the lower part of these slates Lake st. 
 occupies from one half to three quarters of a mile, between the water's Francis - 
 edge and the magnesian and epidotic rocks of the Quebec group, and 
 stretches away to the east corner of the Augmentation of Ham. Higher 
 beds occupy both sides of Lake St. Francis, farther up ; first becoming 
 interstratified with occasional layers of an argillaceous sandstone, and then 
 assuming a slightly calcareous character. A few beds, more arenaceous 
 than others, contain a considerable proportion of carbonate of lime. 
 
 Ten miles up the lake, two opposite points project, and form the Narrows. 
 That on the right side, consists of very quartzose talcoid slates, showing 
 a breadth of about 300 yards. These are immediately succeeded, to the Limestones, 
 southward, by two or three layers of fossiliferous limestone, in which the 
 species, chiefly corals, are rendered too obscure by crystallization, to be 
 identified. These fossiliferous beds, whose total breadth does not exceed 
 ten feet, dip N. 28 W. < 84, very probably showing an inversion of 
 the strata, and are followed by a light grey thin bedded limestone, weath- 
 ering to a yellowish red. Beyond these, occur coarser and more arena- 
 ceous limestones, mixed with micaceo-calcareous sandstones. These latter 
 become interstratified with other sandstones, which contain little or no 
 carbonate of lime, clay slates often separating the beds. 
 
 The fossiliferous limestones just mentioned, are not much out of the LakeAyimer. 
 position which the general strike would give to a continuation of the fossil- 
 iferous strata of the Famine. Ten miles farther in the same direction, 
 towards the south-west, limestones of a similar aspect, though not fossilif- 
 erous, occur two and a quarter miles south of Lake Aylmer, on the forty- 
 fifth lot of the road through Stratford. The interval between this lime- 
 
430 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Ward's Bay 
 
 Quebec group, stone and the margin of the lake, is occupied by strata resembling some of 
 those belonging to the Quebec group ; consisting of green chloritic slates 
 and sandstones, with a serpentine-like rock on the thirty-ninth lot, and 
 nacreous slates nearer the lake ; besides a band of dolomite about twenty- 
 five yards wide, on the twenty-eighth lot. 
 
 On Lake Aylmer, beds of limestone, supposed to belong to the higher 
 rocks, are seen at the upper point, separating Ward's Bay from the body 
 of the lake. Within the bay, there is a small point composed of hard 
 sandstones and very coarse conglomerate beds ; some of the rounded 
 masses in which are a foot in diameter, most of them being very feld- 
 spathic, and apparently of intrusive rocks. These sandstones and conglom- 
 erates, interstratified with hard fine green slates, dip S. 38 E. < 80. 
 They have a breadth of about 110 yards, and are followed to the north- 
 ward by 140 yards of the same green slates, without sandstones. These 
 strata may belong to the Quebec group; but clay slates, supposed to 
 be of the upper series, succeed, and have a transverse breadth of four 
 miles and a half, to Lake Coulombe, on the road to Wolfestown, near the 
 east corner of the Augmentation of Ham ; where they reach a band of cal- 
 careous serpentine, which has been previously mentioned. The bed of the 
 St. Francis River, between Lakes Aylmer and St. Francis, consists of clay 
 slates, often holding flattened nodules of grey yellow-weathering limestone. 
 
 About seven miles up Lake St. Francis, a little way above the mouth of 
 the Blueberry River, an intrusive mass of granite, composed of white 
 quartz and feldspar, with black or brown mica, forms opposite points, nearly 
 east and west of one another. The breadth of the granite appears to be 
 about 400 yards ; and where the strata come in contact with it, on the north 
 side, the effect of the igneous rock on them is plainly discernible, in the 
 presence of an abundance of small crystals of a dark colored mica, and 
 of reddish translucent andalusite, in the argillaceous beds. The sandstones 
 appear as a dark grey quartzite, with disseminated grains of pyrites. On 
 the worn surfaces of loose fragments of slate, found in several parts around 
 the. lake, are seen slender raised forms, which are due to the presence of 
 imperfect crystals of andalusite. 
 
 The same intrusive granite occurs in two small hills on the Felton River, 
 which falls into Lake St. Francis on the left side ; one of them about half 
 a mile, and the other three miles, from its mouth. It also occurs in a hill 
 upwards of three miles long, in Winslow, about five miles to the south-east 
 of Lake Aylmer, and in another hill about a mile to the south-east of Lake 
 Louisa. It is very probable that most of the abrupt isolated eminences 
 of the district, are composed of the same rock. 
 
 Between Lake St. Francis and Lake Megantic, the few exposures of 
 stratified rock which have been observed, are composed of clay slates and 
 sandstones, such as have been just described ; but on the western side, 
 
 Intrusive 
 granite. 
 
 Andalusite 
 
CHAP. XVI.] DISTRIBUTION OF THE GASPE SERIES. 431 
 
 and at the southern end of Lake Megantic, chloritic and epidotic rocks, Lake Megan- 
 
 with nacreous slates and quartzite, again make their appearance, and tic - 
 
 probably belong to the Quebec group. A granite dyke intersects these 
 
 strata, about a mile and a half from the upper end of Lake Megantic ; and in 
 
 the region between this lake and the river St. Francis, there are intrusive 
 
 mountain masses of granite, which very probably produce considerable 
 
 disturbances in the stratification. The largest mass constitutes the Great Megantic 
 
 Megantic Mountain, at the united corners of Hampden, Marston, and M 
 
 Ditton. This, with a length of six miles, and a maximum breadth of three, 
 
 may cover an area of twelve square miles. It has not yet been visited 
 
 by any of the officers of the Survey ; but we have been assured by a 
 
 competent person, that the rock is of the same lithological character as 
 
 the intrusions farther west. Another large granitic mass occurs in the 
 
 Little Megantic Mountain, which may cover an area of six square miles, 
 
 not more than one to two miles to the south-west of the line between 
 
 Aylmer and Grayhurst townships. The bold and pointed form of Gosford Granite hiiie. 
 
 Mountain, at the head of the Arnold River, flowing in at the upper 
 
 extremity of Lake Megantic, makes it probable that it, also, is composed of 
 
 this rock. Granite appears on the Kennebec road, a short distance south 
 
 of the boundary line of the state of Maine. It there rises into bold 
 
 mountains on each side of the road ; and it will probably be found to form 
 
 the range of elevations described as running thence, north-eastwardly, to 
 
 Bathurst, on the Bay of Chaleurs. 
 
 The base of the clay slates, at the east corner of the Augmentation of ciay slates. 
 Ham, is five miles nortn-westward from the limestone which forms the 
 upper horn of Ward's Bay in Lake Aylmer ; but in tracing the outcrops 
 of the two, to the south-westward, the distance between them gradually 
 diminishes, and, after crossing Weedon, they are scarcely more than a mile 
 apart, on the line between that township and Dudswell. On the Gosford 
 road, in Dudswell, the clay slates become concealed, and the limestones 
 rest upon the altered strata of the Quebec group, which form the Stoke 
 Mountain range. With the exception of a few points, where the clay 
 slates appear along the southern flank of this range, the limestones are 
 seen in contact with the rocks of this group, all the way to the eastern 
 shore of Lake Memphramagog, a little north of the province line ; where 
 they both cross the lake, and are continued southward into the state of 
 Vermont. 
 
 In this part of their distribution, from Dudswell to the province line, F 
 these upper strata become of much more importance than before. They hme8t 
 occupy a breadth of about fifteen or sixteen miles, and consist of crystal- 
 line micaceous limestones, interstratified with fine and coarse mica slates. 
 The limestones are much more abundant in the first three miles of the 
 breadth than in the remainder ; and in this portion they are usually of a 
 
432 GEOLOGY OF CANADA. [CHAP. XVI. 
 
 dark grey color, and often of a dull earthy black. These black beds are 
 frequently separated by thin black brittle calcareous carbonaceous slates, 
 which have a silky lustre in fresh fractures, resulting probably from the 
 presence of very fine scales of graphite. The black limestones weather to 
 a deep brown, and the slates to a brownish-black ; and it often happens 
 that a thickness of from six to twelve inches, at the surface, is found in a 
 friable, disintegrating state. 
 
 The light grey limestones, which are of a rather more durable character, 
 sometimes exhibit 300 feet of vertical thickness, in a single exposure. The 
 color of the rock, from light grey, becomes, in some layers, of a uniform 
 yellowish-white or cream color. The beds of this color seem to be more 
 compact than other portions of the rock, and some of them will probably 
 Marbles, yield excellent marble. Both these beds, and others near them, of a mottled 
 dark and light grey, are penetrated by a multitude of reticulating veins of 
 yellow dolomite. On the surface of cut slabs, portions of the grey limestone 
 occasionally approach to black. If any of these beds should be found to 
 give a more uniform and darker grey, or a black, they would yield a marble 
 approaching in character to the celebrated Portor, or black and gold 
 marble. In this, also, the black ground is a pure limestone, while the 
 yellow reticulating veins are of dolomite. 
 
 In some parts, considerable masses of the limestone are striped with 
 grey and white, running in the strike ; and the rock appears to be fissile in 
 the direction of the colors, from the presence of mica between the layers. 
 The light colored varieties are not so easily discolored or disintegrated 
 by the influence of the weather, as the brown-weathering black limestones. 
 The latter usually hold a considerable quantity of iron pyrites, disseminated 
 in isolated cubes of various sizes, up to half an inch ; which are often thinly 
 encased in white quartz. 
 
 The upper end of Massawippi Lake affords examples of the black lime- 
 stones ; while the vicinity of the bridge over the Burrows River, on the 
 Stanstead and Sherbrooke road, displays the grey variety. The striped 
 limestones are seen at Magoon's Point, on Lake Memphrainagog ; and 
 the white and mottled varieties occur at Dudswell. 
 
 Magoon's In the latter two localities, organic remains are met with. At Magoon's 
 Point. Point, they consist of encrinites, which are plainly visible in relief, on 
 weathered surfaces of the rock, and are also perceptible in fresh fractures, 
 notwithstanding the metamorphic condition of the rock ; which is crystal- 
 line and finely granular, with mica running, as already stated, in parallel 
 planes. The sections of the encrinal stems appear as oval rings, with 
 smooth surfaces, resulting from a cleavage oblique to the axis. These 
 rings are surrounded by the finely granular limestone, and show a spot of 
 the same in the centre. 
 
CHAP. XVI.] DISTRIBUTION OF THE GASPfi SERIES. 433 
 
 At Dudswell, in addition to encrinal columns and disks, there is a 
 great abundance of corals ; which occur chiefly in the light grey beds, and 
 are readily distinguished by their whiter color. The whole rock is highly 
 crystalline ; but the corals appear more evenly and finely grained than the 
 enveloping matrix, and are free from mica. Their structure is often plainly 
 discernible on the weathered surfaces, where deeply-worn lines mark the 
 divisions of the cells, columns, and concentric layers. Some of the 
 species appear to be Favosites G-othlandica, F. cervieornis, F. polymorpha, 
 Halysites catenulatm, Heliolites Murchisonia, Syringopora compacta, a 
 Diphyphyllum like D. arundinaceum, undetermined species of Zaphrentis 
 and Heliophyllum, Stromatopora concentrica, and an undetermined 
 Platyostoma. 
 
 The mica slates, which are interstratified with the calcareous portions Mica slates, 
 of the formation, are usually of a soft and fine texture, resembling clay 
 slates, with the addition of mica. In the following seventeen miles of the sec- 
 tion, as seen on the Coaticook road, across Compton, Barford, and Hereford, 
 the calcareous beds diminish in frequency, while the mica slates become 
 stronger and more quartzose, and finally form very thick bands. The 
 usual color of these beds is grey, the limestones sometimes very dark 
 grey, and often silicious. They almost all weather brown, and usually 
 exhibit a thick disintegrated coating; while their ruins constitute a consid- 
 erable portion of the soil. Among the fine mica slates, a few black beds 
 with waved surfaces, are sometimes met with, displaying small crystals of 
 chiastolite in cross fractures. The whole formation is very pyritiferous ; 
 isolated cubes of sulphuret of iron being often thickly disseminated 
 throughout, all the beds. There is but little doubt that these strata are 
 much affected, both by large undulations and by minute corrugations; 
 but in the majority of cases, the dips are towards the north-west, and 
 usually at high angles. By one of th'ese undulations, the serpentine of 
 the Quebec group is brought to the surface, on the fourteenth lot of the 
 eighth range of Eaton, the property of Mr. Farnsworth ; where, as usual, 
 it holds traces of chromium and of nickel. 
 
 The most south-eastern bed of limestone observed, is on the sixth lot 
 of the eighth range of Barford. In the remainder of the distance to 
 Canaan in Vermont, which may be of about twelve miles, mica slates 
 prevail, in alternating black and grey bands, the black holding more 
 mica, the grey more quartz. Bands of light grey or whitish quartzite, 
 weathering to an ochre yellow, are interstratified with the slates, and, 
 about three miles forward on the road, constitute the ridge of a hill. In Hornblende 
 the immediate vicinity of Canaan, some of the strata exhibit a large and garnets< 
 amount of crystallized black hornblende, with small imbedded garnets. 
 Cubes of iron pyrites are met with in all the beds. The prevailing dip 
 appears to be to the north-west, though there are probably many undu=- 
 
 cc 
 
434 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Intrusive 
 granite. 
 
 lations. This part of the formation gives a bold, rugged country, and 
 appears to constitute the range of hills, which furnish the main sources of 
 the Connecticut and St. Francis rivers. 
 
 The strata in the region between the Massawippi River and Canaan, 
 are, in many parts, pierced by considerable masses of a beautiful granite, 
 which consists of white quartz and feldspar, with a rather sparing amount 
 of black mica very uniformly mixed. It is precisely similar to the granites 
 of lakes St. Francis and Megantic, and the intrusive nature of the masses is 
 clearly shown by the granite dykes which proceed from them in various 
 stanstead. directions. One of the largest masses of this region, measuring about six 
 square miles, occurs between Stanstead Plain and Lake Memphramagog, 
 
 432. GRANITE DYKES, CUTTING DEVONIAN LIMESTONES, AT STANSTEAD. 
 
 Dip of the strata, N. N. E. < 30. Scale, about ^. 
 
 occupying from the first to the sixth lot of the fourth, fifth, and sixth 
 ranges of the township. It appears to displace the calcareous strata, which 
 it penetrates, as these are observed to dip from it in several places. On 
 the fifth lot of the fifth range, on the east side of the road, within a short 
 distance of the edge of the granitic nucleus, a great number of dykes 
 of the granite are seen, cutting the basset edges of the limestone beds ; 
 the whole having been worn down to a horizontal surface. Some 
 of the main dykes are from two to three feet in breadth, and divide 
 into a multitude of irregular and reticulating branches, many of which 
 are no more than the eighth of an inch wide. In the face of an escarp- 
 ment, which rises from the granite nucleus to this horizontal surface, a 
 large dyke, of which all the others are probably ramifications, can be 
 traced down towards its source. 
 
 Intrusive masses of the same description of granite are met with on the 
 south side of Barnston and Barford, and farther north in Hereford, in six 
 different localities; in addition to several dykes of a few feet in width, which 
 
CHAP. XVI.] DISTRIBUTION OF THE GASP& SERIES. 435 
 
 are traceable for short distances. In the immediate vicinity of Stan- 
 stead Plain, there is a granite dyke of from seventy to a hundred feet in 
 breadth ; which has been traced for a distance of nearly four miles, from 
 the fourth lot of the ninth range, to the north side of the thirteenth lot of 
 the eleventh range of the township. It appears to cut the stratification in 
 the direction of the strike, which runs north or a little east of north; and 
 it is traversed and broken by transverse faults in two places, in each of 
 which it is heaved to the eastward, on the north side, upwards of 600 
 yards. The direction of these important dislocations seems to bear for the 
 vicinity of Owl's Head Mountain ; and they serve, in conjunction with the 
 intrusive granite masses and dykes, together with the tilted and occasionally 
 inverted attitude, and the contorted condition of the strata, to illustrate 
 the violent disturbances which the rocks of this region have suffered at 
 different epochs. 
 
 The Stoke Mountain range, as we have already described it (page 252), stoke Moun- 
 is a narrow belt of rocks of the Quebec group ; which crosses the southern tams> 
 part of Lake Memphramagog, and extends north-eastwardly, through 
 Stoke, to Weedon. The upper slates and limestones are traced along its 
 south-eastern base, and around its northern extremity, into another 
 synclinal area, which is occupied by the same higher strata. This area western 
 is of a narrow and irregular form, with a length of sixty miles, extend- 6 r nclinaL 
 ing from the Owl's Head Mountain, oa Lake Memphramagog, to Ham 
 Mountain ; and with a breadth of from five to fifteen milea, between the 
 Stoke Mountains and the Shipton Pinnacle ridge. In the south-western 
 extremity of the area, there are two narrow belts of grey fossiliferous Fossiiiferous 
 limestone, interstratified with clay slates; the space between them being hme6tone8 - 
 occupied by dark grey clay slates, with several bands of a yellow- 
 weathering rock, which i& probably magnesian. The belts run in the 
 longer direction of the area, the western one being about three quar- 
 ters of a mile, and the eastern about a mile and a half wide. To the 
 south-west, they are united or nearly so, beneath the waters of the lake ; 
 while in the opposite direction, they diverge a little, the least measure 
 across them both being two miles, and the greatest, including the interme- 
 diate space, four miles and a quarter. The eastern belt is somewhat 
 longer than the western, a& the latter does not reach the Granby and Out- 
 let road, while the former crosses it ; the distance to this road from the 
 Owl's Head being about sixteen miles. The eastern belt underlies the 
 northern half of the lake, while the western passes to the west of it, 
 crossing only the western bay, near Potton Ferry. 
 
 There is little doubt that these two belts of limestone, which contain the 
 same fossils, are equivalent rocks ; and they are supposed to be in the form of 
 two distinct long parallel-sided troughs. The dips of the strata, however, 
 do not assist in making out the structure ; for while the beds on both sides 
 
436 GEOLOGY OF CANADA. [HAP. XVI. 
 
 of the western trough, are as nearly as possible vertical, those of the eastern, 
 dip to the southward at a high angle. These dips might induce the 
 supposition that the two belts of limestone are arranged in the form of a 
 single trough ; but in that case the belts should come to a junction to the 
 northward, which they do not. The fossils common to these belts are 
 Favosites G-oihlandica, F. basaltica, F. polymorpha, Syringopora Hisin- 
 geri, with undetermined species of ZapTirentis and Heliophyllum, a Diphy- 
 phyllum like D. arundinaceum, crinoidal columns, and Stromatopora 
 concentrica. The schistose plumbaginous limestones, at the Owl's Head, 
 abound in obscure fossils, among which a species of Zaphrentis may be 
 recognized. 
 
 ciay slates. Grey clay slates, banded with black, both with glossy surfaces, flank these 
 limestones on each side. On the west side of the western belt, their 
 breadth is pretty uniform, being probably from a quarter to half a mile ; 
 but on the east side of the eastern belt, beginning near Lake Memphramar 
 gog, close upon the edge of the limestone, the breadth occupied by them, 
 gradually increases to the north-east, and, opposite the outlet, may be about 
 five miles. Beyond the termination of the limestones, these slates appear 
 to have a breadth of about ten miles ; reaching from the Sherbrooke and 
 Montreal road in the fourteenth range of Orford, to the Sherbrooke and 
 Massawippi road in the fifth range of Hatley . Farther to the north-eastward, 
 their distribution is affected by two undulations, which bring the strata of 
 the Quebec group to the surface, on their anticlinals, in the neighborhood of 
 
 Brompton. Sherbrooke. On the St. Francis, these slates occupy nearly the whole 
 front of Brompton, and include the rocks of Brompton Falls ; where they 
 are nearly flat, and where the distinction between cleavage and bedding is 
 well marked. They underlie the Windsor River and all its tributaries ; 
 and in the upper part of this river, in Stoke, there rests upon them a third 
 synclinal portion of fossiliferous limestone ; in which, however, the species 
 are rather obscure. This limestone appears to occupy part of the eleventh, 
 twelfth, and thirteenth lots, of the eighth and three sequent ranges ; where 
 it is about a mile and a half removed from the north-western flank of the 
 Stoke Mountains. 
 
 The fossils from the limestones of the western area, are, like those of 
 the Famine, Devonian ; and the species from the extension of the eastern 
 area on Lake Memphramagog, in Vermont, are of the same age. Those 
 of Dudswell are so altered by crystallization, that some little doubt 
 attaches to the determination of their species. Most of them, however, 
 appear to be Devonian ; but Haly sites catenulatus and Syringopora com- 
 pacta, which are supposed to be found there, have not been hitherto 
 recognized higher than the Lower Helderberg group. These facts seem 
 to indicate that a portion of these fossiliferous strata may belong to the 
 summit of the Graspe* limestones, or perhaps represent the base of the Gaspe* 
 
CHAP. XVI.] DISTRIBUTION OP THE GASP SERIES. 437 
 
 sandstones. Nothing, however, having the lithological characters of these 
 sandstones, as they appear at the eastern extremity of the province, has been 
 seen in Lower Canada to the west of the Matapedia River. There is 
 not much doubt that the clay slates which underlie the limestones represent 
 some part of the Gaspe* limestones, though the want of fossils makes it, 
 for the present, difficult to say which part. The lower portion of the Gaspe* 
 series, to the westward, gradually becomes less calcareous and more argil- 
 laceous ; and to the west of Temiscouata Lake, no considerable mass of 
 it can be recognized as a limestone. 
 
 These upper clay slates, on the ChaudiSre and the St. Francis, are inter- Gold veins, 
 sected, in several places, by white quartz veins, generally running with the 
 strike. Some of these, on the ChaudiSre, hold a little blende and argentif- 
 erous galena, with small portions of native gold ; but they are not yet 
 with certainty known to be the source of the drift gold of the Eastern 
 townships. The heaviest masses of gold that have there been met with, 
 weighing from ten to a hundred and twenty-six pennyweights, have been 
 found resting on this slate formation. One of these, in the Museum of 
 the Geological Survey, weighing four ounces, has a considerable portion 
 of quartz adhering to it, and penetrating it ; so that there is little doubt that 
 gold-bearing quartz veins exist in the region, but whether they belong to 
 the Lower or the Upper Silurian series, or to both, has yet to be determined. 
 
 The micaceous slates and quartzites of the third and fourth lots of the Copper lodes, 
 sixth range of Barford, are cut by several quartz veins nearly transverse 
 to the stratification. One of these, which is three or four feet wide, 
 contains dendritic native copper, and yellow sulphuret of copper, asso- 
 ciated with magnetic pyrites, white or pale green apatite, and crystals 
 of silvery white mica. 
 
 COAST SECTION PEOM GASPS BAY TO THE BAY OP CHALEUB8. 
 
 The strata of the Bonaventure formation, between Yellow Head and Gaep<5 Bay. 
 Point Peter, have a general dip to the south-eastward. They strike across 
 the land, forming the south horn of Gaspe* Bay, and run along the coast, 
 all the way to Tickel Inlet. From this inlet to Beach Corner, they are 
 covered up, for about five miles, by the barrier of sand and gravel, which 
 separates the lagoon at the mouth of Malbay River, from Malbay itself. One 
 hundred and seventy yards beyond the brook at Beach Corner, the strata 
 of the formation again make their appearance ; not however with the 
 moderate southern dip of the inlet, but bent up to a high angle, with a 
 northern dip, and occasionally presenting a perpendicular face. One of 
 the conglomerate beds shields the cliff for some distance ; but pursuing the 
 strike, transverse openings, and the channels of one or two brooks, show 
 
438 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Barry Cape. 
 
 Split Rock 
 of Perc6. 
 
 red shales, fine grained sandstones, and other conglomerate layers beneath 
 it ; and on reaching a gap called the Little Blow-hole, a mass of limestone, 
 belonging to an older series, makes its appearance. This however becomes 
 again covered up, farther on, by conglomerate beds, which are nearly ver- 
 tical at the base, but present a curved face, diminishing in slope at the top. 
 By these, the lower rocks are concealed, until near the Great Blow-hole; 
 where they are once more exposed, and run out in vertical or highly 
 inclined strata, into Les Murailles and Barry Cape. This cape is the 
 extremity of a sharp narrow ridge of mottled reddish and yellowish lime- 
 stone, standing between the bay and Barry Brook. The highest point of 
 the ridge, called the Peak, is 660 feet above the water, and is crowned 
 with the conglomerate ; which lies in a horizontal attitude upon the edges 
 of the unconforrnable beds beneath. 
 
 The pierced or Split Bock, from which the village of Perce* takes its 
 name, is an isolated, almost inaccessible mass of the same mottled yellowish 
 and reddish limestone, which stands like a wall, in continuation of Barry 
 Cape. It overhangs the perpendicular, ten degrees north-eastwardly, with 
 a length of 1500 feet, a breadth of 300, and a height of 290 feet ; and 
 presents two arched openings, which have been pierced through it by the 
 action of the waves. Mount Joli and Battery Point are parallel strata, 
 consisting of grey thin bedded limestones and calcareous shales, whose 
 strike eastward would carry them south of the pierced rock. It is plain 
 from their strike in the opposite direction, that they run under the Perce* 
 Mountains ; the whole of the summits of which, are composed of the Bona- 
 venture conglomerate. 
 
 The flat top of the pierced rock, and that of Les Murailles, extending to 
 the cone of that portion of them termed the Peak, are probably portions of 
 the ancient surface, on a continuation of which the conglomerate is based. 
 Perc Moun- The height of this surface being about 300 feet above the sea level, while 
 that of the most elevated summit of the Perce* Mountains is 1230 feet, 
 according to Bayfield's chart ; it would appear that a vertical thickness of 
 not less than 900 feet of the conglomerate is present in these mountains. 
 Lofty perpendicular precipices of it are seen on several sides of the Table 
 Roulante, and of Mount St. Anne, and its base may be traced along the 
 eastern flank of the latter, descending as it proceeds southward ; though 
 where it probably reaches the shore, at Robin's Brook, about three fifths of 
 a mile from Mount Joli, it is concealed from view by the gravel of the 
 beach. Perce* Reef, however, is composed of this rock, and probably marks 
 the direction of its submarine connection with Bonaventure Island, which is 
 wholly formed of the conglomerate. Here its massive beds rise up, at a 
 moderate inclination to the north-east side ; where they form vertical cliffs of 
 several hundred feet in height, which give shelter to myriads of gannets, 
 
 Bonaventure 
 Island. 
 
CHAP. XVI]. DISTRIBUTION OF THE GASPti SERIES. 439 
 
 cormorants, gulls, and other sea fowl. It is from this island that the name 
 of the Bonaventure formation is derived. 
 
 Proceeding southward along the main shore, from Robin's Brook, the 
 base of the Bonaventure formation again makes its appearance near Lafes- 
 tie's Brook, upwards of a mile from Mount Joli. Here it gradually rises 
 up, at an angle increasing from two to seven degrees, and once more exposes 
 lower unconformable strata in White Head ; which is composed of a limestone White Head, 
 fit for burning, tilted up at an angle of seventy degrees. The two forma- 
 tions are seen in juxtaposition for between 500 and 600 yards ; the lowest 
 member of the upper formation being a ten-feet bed of whitish-grey hard 
 calcareous roCk, greenish at the bottom, with many small veins of red and 
 white chert. 
 
 In the White Head limestones there are a few fossils : the limestones of Fossiiiierous 
 the pierced rock and of Barry Cape abound with them, though the species '" 
 do not appear to be numerous. Among them, in addition to fucoids, are 
 Strophomena perplana, two undescribed species of Chonetes, different from 
 those of Cape Gaspe*, Leptocoelia concava* L. flabellites, Rensselceria 
 ovoides, two undetermined species of Spirifera, S. arenosa, undetermined 
 species of Athyris, Platyostoma and Platyceras, Dalmanites pleuroptyx, 
 and an undetermined Phacops. Among the species of Mount Joli are 
 Favosites G-othlandica, F. basaltica, F. cervicornis, with an undetermined 
 Zaphrentis, and fragments of a Rhynchondla. These older rocks, which 
 all present high angles of inclination, are affected by undulations, and 
 broken by transverse faults, and their precise relation to one another has 
 n4 been finally determined. The strata at Battery Point and Mount Joli 
 have a breadth of about 500 yards. After a small interval of Concealment, 
 those of the pierced rock, Barry's Cape, and Les Murailles, follow, with a 
 breadth of about 400 yards. These appear to be succeeded to the northward, 
 by yellowish-white fine grained calcareous sandstones, which may have a 
 transverse measure of 120 yards. The only fossil found in these strata is a 
 worm-track, very much resembling that of the Gasp6 sandstones near Tar 
 Point. There comes in contact with them, on the north side, a band of 
 greenish-black^soft argillaceous fossiliferous shale, in which were observed 
 the following genera: Chonetes, Nucula, Pleurotomaria, Bellerophon, Aci- 
 daspis, and Ampyx, with the pygydia of two other trilobites, and Serpu- 
 lites. A thin bed of limestone, near the black shale, contains Halysites 
 catenulatus. The geographical sequence of these rocks, from south to A 
 north, in connection with their fossils, would appear to bring them into st;s;ta - 
 comparison with the Gasp6 limestones, and the lower part of the Gaspe* 
 sandstones ; and to place them, with the exception of the black shales, on 
 the horizon of the Lower Helderberg and Oriskany formations. The shales 
 can scarcely be higher, and may be lower than the Niagara formation ; in 
 which case there must exist in these older rocks, on the south side of 
 
440 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Malbay, a considerable longitudinal dislocation, which, with all the undu- 
 lations and transverse faults that have been mentioned, is covered over 
 by the Bonaventure rocks. 'The white sandstones would afford a beautiful 
 material for building purposes. In one of the numerous veins of calcspar, 
 with which the mural precipices of the reddish and yellowish limestones are 
 , traversed, there are traces of galena ; the occurrence of which still farther 
 
 assimilates these rocks to the series on the north side of Gaspe" Bay. 
 Fault. Continuing to trace out the geographical distribution of the rocks, along 
 
 the coast ; a dislocation occurs, about 500 yards westward of White Head, 
 letting down the edge of the Bonaventure rocks against the fossiliferous 
 limestones. These are here seen in a transverse sectkm, with a dip 
 S. 7 E. < 58 ; showing the direction of the fault to be S. 67 W. The 
 upper rocks, consisting chiefly of red sandstone, with only a few conglom- 
 erate layers, slope in towards the limestones, maintaining an eastern dip 
 for about a mile. They begin with an inclination of twenty degrees, but 
 gradually diminish to four, and at length become horizontal on the crown 
 of a flat arch. This causes a repetition of some of the beds in ascend- 
 ing order, farther on, and brings the general strike of the measures to 
 coincide pretty nearly with the coast, as far as Beaufils Bay, with a 
 gentle slope to the south-eastward. 
 
 FAULTS IN THE BONAVENTURE SANDSTONES. 
 
 Bearing and 
 inclination of 
 the underlie. 
 
 Number. 
 
 Bearing. 
 
 Inclina- 
 tion. 
 
 Down- 
 throw. 
 
 Up- 
 throw. 
 
 Number. 
 
 Bearing. 
 
 Inclina- 
 tion. 
 
 Down- 
 throw. 
 
 Up- 
 throw, 
 
 1 
 
 227 
 
 80 
 
 7 
 
 . . 
 
 13 
 
 187 
 
 65 
 
 8 
 
 . . 
 
 2 
 
 202 
 
 58 
 
 90 
 
 .. 
 
 14 
 
 187 
 
 65 
 
 100-f 
 
 .. 
 
 3 
 
 352 
 
 65 
 
 6 
 
 
 
 15 
 
 235 
 
 90 
 
 1 
 
 
 
 4 
 
 m 
 
 68 
 
 6 
 
 .. 
 
 16 
 
 352 
 
 83 
 
 30 
 
 .. 
 
 5 
 
 172 
 
 61 
 
 8 
 
 .. 
 
 17 
 
 ? 
 
 ? 
 
 .. 
 
 30 
 
 6 
 
 187 
 
 56 
 
 1 
 
 .. 
 
 18 
 
 192 
 
 75 
 
 12 
 
 .. 
 
 7 
 
 187' 
 
 65 
 
 2 
 
 .. 
 
 19 
 
 7 
 
 75 
 
 30 
 
 .. 
 
 8 
 
 2 
 
 75 
 
 - 
 
 1 
 
 20 
 
 187 
 
 75 P 
 
 
 
 50-J- 
 
 9 
 
 187 
 
 65 
 
 7 
 
 .. 
 
 21 
 
 187 
 
 60 
 
 30 
 
 .. 
 
 10 
 
 187 
 
 65 
 
 4 
 
 
 
 22 
 
 177 
 
 70 
 
 5 
 
 .. 
 
 11 
 
 197 
 
 65 
 
 2 
 
 
 
 23 
 
 352 
 
 75 
 
 10 
 
 .. 
 
 12 
 
 192 
 
 65 
 
 1 
 
 
 
 24 
 
 352 
 
 65 
 
 5 
 
 
 
CHAP. XVI.] DISTRIBUTION OP THE GASPfi SERIES. 441 
 
 The red sandstones between White Head and Beaufils Bay, are exposed 
 for nearly four miles, in a cliff. This varies from twenty to one hundred 
 feet in height, and displays in that distance, not less than twenty-four dislo- Dislocations, 
 cations ; the extent of nearly the whole of which, may be seen in the cliff. 
 On the preceding page is a list of them, with the bearing and inclination of 
 the underlie of each, so far as it could be determined by the evidences on 
 the beach, and in the cliff; together with the number of feet of upthrow or 
 downthrow, proceeding westwardly along the coast. The bearings are 
 given in degrees, numbering eastwardly from north as zero. The under- 
 lie of one of the faults, 17, could not be ascertained. 
 
 After an interval of about three quarters of a mile, covered over by the 
 sandy beach of Beaufils, or Upper Cape Cove village, another mile and 
 a half of red sandstone cliffs occurs, presenting a second flat arch, with 
 a sweep in the strike, keeping it with the trend of the coast; which has 
 more of southing in it. Here, eleven dislocations, of a similar character 
 with the preceding, occur. Another interval of sandy beach, occupied by 
 Lower Cape Cove village, brings us to Cape d'Espoir, where 110 feet, cape 
 composed chiefly of conglomerate beds, with a dip S. 17 E. < 4, are d ' E6 P ir - 
 presented in a vertical cliff. The coast continues on the strike of these, 
 for nearly three miles, to Little River ; where lower unconformable strata 
 once more break through. 
 
 These lower rocks consist of hard arenaceous limestones, in beds of from 
 one to ten inches thick, separated by layers of fine bluish-grey argillaceous 
 and slightly calcareous slate, dipping N. N. W.< 73 . These, after appear- 
 ing at intervals, for half a mile, at the base of the conglomerates, and in 
 contact with them, again become hidden for three quarters of a mile, in 
 which the conglomerates alone occupy the cliff. A layer of trap becomes interstratmed 
 intercalated with these beds, at a spot called Les Roches Noires. Its trap- 
 thickness is from ten to fifteen feet, and, occupying the upper part of the 
 precipice, which varies from sixty to a hundred feet in height, it main- 
 tains a constant position for about a mile. In the latter part of this 
 distance, the lower strata, in a disturbed attitude, are again seen underlying 
 the conglomerates. The three rocks are visible at once in the cliff section. 
 This is composed of ten feet of conglomerate at the top, succeeded below 
 by the same thickness of trap, and by thirty feet of conglomerate ; which 
 are underlaid by ten feet of the inclined calcareous strata. 
 
 In the interval between this and the Grand River, the cliff is divided 
 between the horizontal conglomerate, and the tilted strata beneath it, each 
 occupying about one half of the height. Ravines, occupied by brooks, how- * 
 ever, cut the cliff down to the base of the conglomerate. Approaching Grand Kiver. 
 the Grand River, after a distance occupied by the conglomerate, in a low 
 cliff, there is a space covered with sand and gravel. Another bed of 
 trap, perhaps a continuation of the previous layer, paves the beach at the 
 
442 GEOLOGY OP CANADA. [CHAP. XVI. 
 
 extremity of Green Point, and the conglomerate coming from below it, crops 
 out and forms a narrow flat strip on each side of the mouth of the river. 
 
 It is probable that in the whole distance from Little River, the conglom- 
 erate beds, which have a gentle dip to the south, have but little breadth, and 
 are nothing more than portions of the rim of the formation, saved from the 
 wearing action of the sea, which has carried off the other parts, by the pres- 
 ence of the harder tilted strata at high water mark. It may be seen that 
 wherever the flat conglomerate alone occupies the cliff, the waves, dashing 
 against its base, wear deep horizontal caverns beneath. Great portions 
 being thus deprived of support, are cracked off vertically, and fall in huge 
 fragments, forming a temporary talus ; which it is probable the ice of winter, 
 with other causes, may aid in removing. 
 
 With the exception of the narrow strip at the mouth of the stream, none 
 of the conglomerate is seen on the Grand River, for six miles up. Its 
 banks are composed of dark grey slates, with a cleavage independent of the 
 bedding, associated with dark grey limestones and occasional arenaceous 
 layers. The age of these strata, for want of fossils, has not been determined. 
 The coast line westward, however, with the exception of those parts covered 
 by sand, and particularly of the barrier to the lagoon of Little Pabos, is 
 wholly occupied by the conglomerate ; which is displayed in cliffs, varying 
 from ten to forty feet, and not exceeding sixty feet in height. They 
 belong to a narrow belt of the deposit, which is continuous, until reaching 
 Pabos. a brook about a mile and a quarter eastward of Grand Pabos beach, 400 
 yards beyond which it terminates. Between this termination and the 
 rock of Grand Pabos beach, there is only one thin small patch of the 
 conglomerate, at the Pointe du Portage, extending about half a mile ; where 
 it is seen resting on the lower rocks, now changed in their characters from 
 calcareous to arenaceous. 
 
 From the rock of Grand Pabos lagoon, none of the upper formation 
 occurs, with the exception of a small patch at a point called Jardin a 
 Naveau, until attaining the south side of Point Maquereau. The interval 
 along the coast is thirteen miles, and, as has already been stated in 
 describing the distribution of the Quebec group, it is occupied by these 
 lower rocks. The vertical strata of this group extend along the coast 
 towards Anse a la Vieille, where they are overlaid by the inclined strata 
 of the Gaspe* limestones, which, in their turn, support the Bonaventure 
 conglomerates ; the three series being unconformable with each other. 
 Discordance The proofs of this double discordance lie within a space of half a mile, 
 f01 " a ^ e * ess t * ian two m ^ es westward of the line between the counties of 
 Gaspe* and Bonaventure ; and as there is no concealment of strata, the 
 whole is readily apparent to the eye. The smoothly worn edges of the 
 vertical strata of the Quebec group, here support an even layer of four 
 feet of hard greyish-white strong silicious conglomerate, which divides 
 
CHAP. XVI.] DISTRIBUTION OP THE GASPfi SERIES. 443 
 
 into layers of a foot or two, and would make good millstones. It dips 
 S. 4 W. < 38, and is conformably overlaid by a great series of fossil- 
 iferous limestones and shales. At a point about 230 yards, along the beach, 
 from the millstone layer, these calcareous strata dip S. 3 E. < 45, in a 
 cliff from 100 to 120 feet high. Upon the basset edges of these, the 
 beds of the upper conglomerate are seen to repose, with a dip S. 42 E. 
 < 20. These stretch along for 200 yards, presenting a perpendicular 
 precipice in front; while the underlying calcareous series forms a talus, 
 and occupies sometimes more and sometimes less than one half of the 
 height of the cliff. 
 
 The conglomerate is here of a deep red color, and holds many boulders, 
 as well as pebbles of various kinds. Those of a red sandstone are the 
 most numerous, and some of them may attain a weight of one hundred 
 pounds, while others of a silicious conglomerate would not be less than 
 seventy pounds. Pebbles of fossiliferous limestone, of ten pounds weight, 
 were met with, and others of a compact limestone were equal to two hun- 
 dred pounds, and, in one instance, to half a ton weight. 
 
 In the next ten miles along the shore, two small areas only of the Bona- 
 venture formation are met with ; but the underlying calcareous strata are 
 conspicuously displayed in the coast cliff. The base of the series is the p rt Daniel 
 four feet of millstone conglomerate already described ; and the section pre- 6ection - 
 sents, in ascending order, the following rocks : 
 
 Feet. Feet. 
 
 1. Reddish-grey micaceo-arenaceous limestone, weathering to a dull Silicious con- 
 
 ochre-yellow, interstratified with six bands of silicious con- glomerates. 
 
 glomerate ; (of which the four-feet millstone bed at the base, 
 
 is one ;) and abounding in fossils, 140 
 
 2. Greenish calcareous shale, including a few beds of yellow-weath- Green shales. 
 
 ering limestone, with many nodules of the same, and holding 
 
 many fossils, 200 
 
 There is here a break in the succession, occasioned by a fault, 
 which creates an interval of great confusion. The cliff shows 
 many of the details of the disturbance, but is not high enough 
 to afford evidence of the amount of displacement. Judging 
 however, by the different color of the strata on the west side, 
 it appears probable that there is a downthrow to the west, 
 which would cause no repetition, to exaggerate the apparent 
 volume of the formation. On the west side of the dislocation, 
 the following is the succession : 
 
 3. Grey hard limestone, in beds of from six inches to a foot, 50 Limestones 
 
 4. Red micaceo-arenaceous shale, with very few fossils, 200 and red shales. 
 
 5. Grey limestone shale, inclining to green, with many corals,. . . . 900 
 
 6. Grey or greenish limestone, partly of a slaty character, and full 
 
 of organic remains. It includes a band of yellowish-grey cal- 
 careous sandstone in the middle, equal to about half the 
 
 amount, yielding excellent tilestones and flagstones, 150 
 
 1. Greenish calcareous shale, with Fucoides like F. cauda-galli,. . . 500 2140 
 
444 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Feet. Feet. 
 
 Among the organic remains of all the preceding beds, are 
 the fucoid just mentioned, Pal&ocyclas porpita, Heliolites inter- 
 stincta, H. Murchisonia, H. inordinata, Favosites Gothlandica, 
 F. Hisingeri, Stenopora pulchella, Halysites catenulatus, an un- 
 determined species of Syringopora, two species of Cyathophyllum, 
 and two of Zaphrentis, two of Diphyphyllum, and one of Cysti- 
 phyllum, Stromatopora concentrica, an undetermined species of 
 Strophomena, S. rhomboidalis, Orthis elegantula, 0. Davidsoni, 
 Rhynchonella neglecta, R. cuneata, R. nodostriata, Stricklandia 
 Gaspensis, Pentamerus Knightii ? Mhyris intermedia, and Euom- 
 phalus rugosus. 
 
 Bed shales. 8. Light red shale with green streaks and spots, 500 
 
 9. Grey limestones, in beds of from six to eight inches, with fossils. 
 Among the species are Heliolites interstincta, H. Murchisonia, H. 
 inordinata, Favosites Gothlandica, Halysites catenulatus, unde- 
 termined species of Diphyphyllum and Fenestella, Stromatopora 
 concentrica, Strophomena funiculata, with a new species of the 
 last genus, and one of Orthis, Spirifera ciispata, and an unde- 
 termined Illoenus, 200 
 
 10. Light grey compact limestone, indistinctly bedded, and filled 
 with corals, broken encrinites, and other fossils. Here and 
 there, a portion of red arenaceous limestone runs for a short 
 distance in the supposed direction of the strata ; which are inter- 
 rupted by shapeless lumps of compact limestone. The red 
 layers contain white broken encrinal columns, and are pierced 
 by white cylindrical corals. Among the fossils are Favosites 
 Gothlandica, two undetermined species of Strophomena, with 
 S. rhomboidalis, S. funiculata, two undetermined species of 
 Rhynchonella, with R. Stricklandi, R. Wilsoni, R. cuneata, an 
 undetermined species of Spirifera, S. crispata, S. radiata, 
 three undetermined species ofjithyris, Atrypa reticularis, three 
 undetermined species of Pleurotomaria, and one of Orthoceras, 
 Bronteus Canadensis, Lichas Canadensis, with undetermined 
 species of Jlcidaspis and Chururus, 500 
 
 Grey lime- 
 stones. 
 
 1200 
 
 3340 
 
 Anticosti 
 group. 
 
 The fossils of this series would appear to place it at the summit of the 
 Anticosti group, about the horizon of the Niagara formation. We may 
 expect in future explorations of the interior of Gaspe* to find this series, 
 in some part of its distribution, between the equivalents of the white 
 sandstones of the Chatte, with their immediately succeeding limestones, 
 and the calcareous strata of Cape Gaspe*. 
 
 Between Cape Maquereau and Port Daniel, the lower members of the 
 section, to the sixth division inclusive, form the eastern part of Anse a la 
 Vieille, up to the brook. The seventh and eighth constitute the remainder 
 of the cove, and also Anse au Gascon ; while the ninth, and about seventy 
 feet of the tenth or upper division, compose Pointe aux Bouleaux, which 
 separates these two coves. The Gros Morbe, between Anse au Gascon and 
 Anse a la Barbe, displays the whole thickness of the two higher members. 
 
CHAP. XVI.] DISTRIBUTION OF THE GASP& SERIES. 445 
 
 These two also constitute the coast, nearly the whole way to Port Daniel, p or t Daniel 
 "by Harrington Cove. The two conspicuous points on the east side of Port Bay - 
 Daniel Bay, of which the northern one is called the Devil's Cape, exhibit 
 the uppermost limestone in a nearly vertical attitude, with its encrinal char- 
 acter well marked ; and it is again seen on the front of Mr. Carter's land, 
 between the great and little lagoons. Following up the West River, it is 
 found to cross it several times, first with a south-west, and then with 
 a north-west dip. Though it does not again occur in the five miles of this 
 stream which have been examined, there is not much doubt that it will be 
 found higher up, with a final southward dipping outcrop. 
 
 Following round Port Daniel Bay, from the exit of the little lagoon, the 
 strata are covered over by sand and gravel for upwards of a mile ; beyond 
 which, the green calcareous shales, 7, are seen dipping northwardly, then 
 southwardly, and finally resting upon the red shales, 8. The upper 
 limestones are again displayed in South- West Point, and from this, run along 
 the coast, for two miles, to the neighborhood of Indian Point ; where they 
 are once more concealed, at the water-line, by the overlying unconformable 
 red sandstone and conglomerate. 
 
 The base of this calcareous series, in the vicinity of Port Daniel, is prob- 
 ably near to the junction of the Middle River with the great lagoon. From shale8 ' 
 beneath these strata, higher up on the stream, beds of black bituminous 
 graptolitic shales come to the surface, and are seen, at intervals, for several 
 miles. The position of these shales is between the calcareous series, and 
 the strata of the Quebec group, at Cape Maquereau. Their absence in 
 the coast section is explained by the unconformability of the overlying 
 formation ; while their relations to the rocks above and below, would assimi- 
 late them to the black shales which underlie the Gaspe limestones near 
 Cape Rosier, and which are supposed to be near the base of the Quebec 
 group. 
 
 Some .portions of these black shales hold hydrocarbonaceous matters in 
 sufficient quantity to burn with flame, when subjected to heat. This prop- 
 erty, in connection with their color, has in this, as in other instances, led 
 persons to suppose these shales to be indications of the presence of work- 
 able coal seams. The structure of the neighborhood, however, places 
 these strata at a much lower geological horizon than that of the coal 
 formation, and renders the discovery of profitable coal seams in them, 
 contrary to present geological experience. 
 
 The Port Daniel limestone is of an excellent description for burning, 
 and is well fitted for mortar or for agricultural purposes. Very beautiful 
 flag and tile stones might be obtained from some calcareo-arenaceous strata, 
 which occur a little westward of the brook, in Anse a la Vieille, and split 
 readily into large and very even plates of almost any required thickness 
 from a quarter of an inch to three or four inches, from the presence of a 
 
446 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Bonaventure 
 formation. 
 
 small quantity of mica in the divisional planes. The bed of silicious con- 
 glomerate at the base of the limestone series, as well as others of similar 
 character, and of greater amount, on the West River, would yield good 
 millstones. 
 
 Returning to the unconformable Bonaventure formation, there are 
 between Anse a la Vieille and Indian Point, two localities where portions 
 of the conglomerate rest upon the limestones. One of these is in Har- 
 rington Cove, where a breadth about forty yards of it is seen, and where 
 its enclosed masses are angular, and are derived from the immediately 
 underlying strata. The fragments are large, and one, which protrudes 
 from the red sandstone matrix, cannot be much under eight tons in weight. 
 The other portion occupies the banks of a small brook flowing into Port 
 Daniel Bay, a little to the east of the great lagoon. From the mouth of 
 the brook, it runs up the dingle, and crosses the road about a mile east of 
 the sand beach. It is a strip, which occupies a valley in the surface 
 where it was originally deposited, and has been protected from erosion 
 by the defences of older rocks on each side of it. 
 
 New Carlisle. From Indian Point, a great stretch of this formation, with only such con- 
 cealment as arises from the sand beach of Nouvelle, and that of Paspebiac 
 (to the landward of which there is a precipitous bank clearly marking 
 the presence of the rock), carries us to New Carlisle. In this distance 
 of twenty miles, its prevailing character is that of a red sandstone, with but 
 few conglomerate layers. The rocks upon which it rests, are seen, at 
 high-water mark, only in the first part, as far as Cape Loup Marin, and 
 again at Mashigoweech. 
 
 Less than a mile and a half from the town-lot of New Carlisle, the older 
 strata again appear, presenting at the same time a new feature in the coast 
 section. Proceeding westward, the upper rocks, consisting chiefly of red 
 sandstone, have a gentle dip, not exceeding one or two degrees, to the east- 
 ward ; and repose upon the truncated extremities of a group of trap dykes, 
 not much less than fifty in number, and from eighteen inches to twenty feet 
 in breadth. These cut through the lower formation, which here consists 
 of red calcareo-arenaceous shale, with a few thin bands of limestone. 
 The intrusive rock is sometimes a greenstone porphyry, containing tabular 
 crystals of greenish-white feldspar, which have their flat faces turned to the 
 walls of the dyke towards each side, but are occasionally transverse to the 
 dyke, in the middle. On reaching the town-lot, the overlying red sand- 
 stones cease, and crystalline rocks cover nearly the whole of the area. 
 These appear to be of different characters in different parts : a ledge 
 running N. N. E. and S. S. W., consists, in one part, of greenish-white 
 feldspar, with black hornblende and a small quantity of black mica. In 
 another part, to the south of this, the feldspar assumes, when weathered, a 
 light flesh-red tint, and the rock is nearly made up of it. This is on the 
 
 Trap dykes. 
 
 Crystalline 
 rocks. 
 
CHAP. XVI.] DISTRIBUTION OF THE GASPE SERIES. 447 
 
 thirty seventh lot, where it appears to hold a small vein of the specular 
 oxyd of iron, which, from the decomposed condition of the rock, it was 
 found impossible to trace to a distance ; but it is said, that for a consider- 
 able distance around, lumps of micaceous iron ore are frequently turned up 
 by the plough. 
 
 The breadth inland, of the Bonaventure rocks, in the neighborhood of 
 New Carlisle and Paspebiac, is a little over two miles. They extend to the 
 foot of a hn% composed of the upper Port Daniel limestones, which rises 
 rather boldly to the height of about 300 feet, and runs in a direction to 
 join the limestone on Mr. Carter's land. From New Carlisle to Red Cape, Red Cape, 
 and a little beyond it, in the township of New Richmond, a distance of 
 about twenty-three miles, the coast displays the upper red sandstones ; 
 with the exception of about five miles at the mouth of the Bonaventure or 
 Wagamet River, where they are covered over by drift clay. They occur 
 about five miles up the Bonaventure, and have probably a breadth of four 
 miles in the township of Hamilton. 
 
 At Capeling River, the Bonaventure formation is a conglomerate, with 
 limestone pebbles, and the beds lie nearly flat ; but at Red Cape they dip 
 S. S. E. < 20, and, about five furlongs farther, suddenly turning down to a 
 dip S. 35 W. < 55, they abut against a great mass of trap ; which extends 
 about a mile along the coast, and at its termination, constitutes Black Cape. Black cape. 
 The direction of the dislocation is N. 55 W., and, at the junction of the 
 two rocks, the conglomerate contains boulders and great fragments of 
 trap, in the usual matrix of red sandstone ; together with large calcareous 
 pebbles holding organic remains, which are like those of the upper lime- 
 stones of Port Daniel. 
 
 In the coast section, this mass of trap, in its eastern part, is homogeneous 
 in appearance, and has a uniform dark green color, with occasional red 
 iron stains. On the western side, it forms a breccia, which is interstratified 
 with several beds of reddish limestone, similar to the upper rocks of Port 
 Daniel ; forming together a cliff of about fifty feet, with a dip S. S. E. 
 < 46- 68. Much of the trap in this portion weathers of a rusty purple, Trap breccia, 
 but is of a dingy bottle-green within. It encloses large angular masses, 
 which differ but little in color, but are harder than the matrix, and stand 
 out in bold relief on the weathered surfaces ; sometimes with smooth faces, 
 resembling huge crystals. With these, are also found large angular 
 amygdaloidal masses, holding carbonate of lime : these, also, sometimes 
 weather in relief. Fragments of indurated red shale, and others of lime- 
 stone, like that of the adjacent beds, are also common in this trappean 
 breccia. The limestones retain their reddish-white color, and often exhibit 
 corals and encrinites on their weathered surface, though these are not 
 apparent in recent fractures. The limestone fragments are chiefly met 
 with in the paste or matrix of the breccia ; and though they occasionally 
 
448 GEOLOGY OP CANADA. [CHAP. XVI. 
 
 occur in the amygdaloid, are entirely absent from the harder angular 
 masses. 
 
 This lower part of the trap has much the aspect of having resulted from 
 a flow of viscid matter, which had rolled over on its own crust, enclosing 
 fragments of this, and of everything met with in its progress. Another 
 portion seems to be arranged in beds, holding a collection of trap boulders, 
 pebbles, and fragments enclosed in a trappean cement. All these 
 characters accord with the relation which the trap bears to the strata to 
 the west ; and it may have been poured over them, at different times, when 
 they were in a horizontal position. The thickness of this mass, including 
 the interstratified beds of limestone, appears, from the data obtained on 
 the coast, to be 650 feet. 
 
 The strata to the westward, along the bay, have the same general charac- 
 ters as those of the Port Daniel section. At the summit, there is a limestone 
 like the upper divisions there, and another at the base, resembling that of 
 Anse a la Vieille ; while the intermediate strata, as a whole, are very similar 
 to those of the last named locality, and of Anse au Gascon. The total thick- 
 ness in this vicinity, as exposed in the two miles succeeding Black Cape, is 
 more than three times that of the other, owing to the augmentation of the 
 middle portion of the series. 
 
 cascapedia This great exposure terminates just one mile east of the cove at the 
 mouth of the Little Cascapedia River, where the limestones run inland, 
 with a strike S. 5 E. The whole coast, from this to the mouth of the 
 Great Cascapedia River, is occupied by drift clays, with their usual accom- 
 paniment of marine shells. On the west side of the Great Cascapedia, the 
 Bonaventure conglomerates again make their appearance. They are seen 
 in a conspicuous hill, in which the strata gradually rise from Indian Point, 
 attaining an elevation of 378 feet ; and they compose not only the hill, but 
 the flat valley beyond. From Indian Point, their transverse stretch up the 
 Great Cascapedia may be about four miles ; at the end of which distance, 
 they reach the base of the mountain slope running for the Peak of Traca- 
 digash. Westward from the Great Cascapedia, they skirt Cascapedia Bay, 
 up to the dividing line between the townships of Maria and Carleton ; where 
 they may have a breadth of a mile and upwards, though they are not seen 
 on the coast; being covered, along the water-line from Indian Point, by 
 the drift clays. 
 
 Mountain The mountain flank, which runs nearly parallel with the coast, from the 
 Cascapedia towards the Restigouche, is a part of the southern boundary of 
 the table-land which composes the general surface of the Gaspe* peninsula. 
 As far as the Peak of Tracadigash, it appears to run about southward, in 
 the strike of the measures, and to be composed of a coarse silicious con- 
 glomerate, standing in a vertical attitude, and presenting several remark- 
 Trap hiiis. able precipices. Between it, and the comparatively flat Bonaventure con- 
 
CHAP. XVL] DISTRIBUTION OF THE GASPfi SERIES. 449 
 
 glomerates in front, there occur several isolated hills of trap, with conical 
 summits, occasionally resting in part upon the mountain flank. The breadth 
 occupied by these, indicates that the range of trap with which they are con- 
 nected, is of some importance. 
 
 From the Peak of Tracadigash, the flank of the table-land changes its 
 direction, still running parallel with the coast, a little to the north of west, 
 and makes a partial section obliquely across the measures. These con- 
 sist of dark colored slates, with several masses of trap, and finally a great 
 calcareous formation ; which seems to run inland, to the north of the silicious 
 conglomerate. It is probable, however, that the strike ot the strata and 
 the mountain flank, again coincide, farther on ; for at the foot of the latter, 
 trap is found, associated with limestone beds, at the bridge, five miles up 
 from the mouth of the Nouvelle River ; and again, on the bridge over the 
 Scaumenac, a mile from its mouth. Trap also appears at the junction of scaumenac 
 the Little River with the Restigouche ; from which it is separated, between Rlver ' 
 the mouths of the Scaumenac and Little Rivers, by a margin of silicious 
 conglomerate, very like that of Tracadigash. This latter rock is seen in 
 vertical or highly tilted southward-dipping strata, below Mungo's Brook, 
 as well as at Points Lagarde and Bordeau ; comprehending a distance of 
 thirteen miles. 
 
 The valley of the Little River makes a section across the range of Little K**- 
 trappean hills. These, on the Kempt or Metis road, which runs along this 
 valley, have a breadth of more than two miles, extending to the bridge 
 across the river ; close by which, fossiliferous limestones appear, succeeded 
 by calcareo-argillaceous and arenaceous shales, and, farther back, by thin- 
 bedded limestones, with dark shales. Not far below the bridge, a tribu- 
 tary from the west joins the Little River, and, in the latter part of its 
 course, runs through a valley; which corresponds with that in which 
 another stream flows we'stward, joining the Restigouche, about five miles 
 below the mouth of the Matapedia. The fossiliferous limestones, which 
 probably extend along these valleys, here come upon the Restigouche. 
 
 Mountains of trap occupy the whole of the triangle between the valleys Trap Mils, 
 and the main river ; and just at the termination of the mountain, at the apex 
 of the triangle, the intrusive rock is seen interstratified with the limestones. 
 Some of the fossiliferous strata are exposed near the mill on Andrew's 
 Brook, a little over two miles below the Matapedia ; and again about half a 
 mile farther up, below the mouth of Seller's Brook. The thin bedded lime- 
 stones, in which no fossils have been observed, come upon the Restigouche 
 at and below the mouth of the Matapedia. 
 
 Returning down the Restigouche, on the opposite side y ih New Brunswick, 
 the trap range is again met with. The Sugar-loaf, near Campbelltown, 
 is a hill of trap ; and this rock occupies the greater part of the area between 
 the brook at its base, and the Restigouche. On the margin of the river, 
 
 DD 
 
450 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 Cape Bon 
 Ami. 
 
 Kestigouche 
 
 Bonaventure 
 rocks. 
 
 however, a silicious conglomerate appears ; and at Mission Point, just in 
 front, a greenish-grey sandstone, probably belonging to the same formation, 
 is met with. The strata in both localities dip northward. Lower down, 
 between Shaw's Brook and Point La Lime, intrusive rocks again appear. 
 They are composed of red feldspar and black mica, and are interstratified 
 with the conglomerate ; which is composed almost altogether of pebbles of 
 crystalline rocks, and runs along the beach for some distance, to Point 
 La Lime. 
 
 A little below the point, there occurs, associated with the conglomerate, 
 a thin seam of carbonaceous shale, with a bed of clay beneath it. The same 
 seam is again seen at Point Pin Sec, resting on the clay bed, and over- 
 laid by a mass of intrusive rock ; which has changed it to a hard black 
 stone. A conglomerate bed again occurs farther on, from beneath which, 
 towards Point Peuplier, there appears a red slate, employed by the 
 Indians for the manufacture of their calumets. The rocks seen along 
 the shore, between this and Dalhousie, are nearly all of trap. In a 
 beautiful transverse section of the trap series, which occurs in the vicinity 
 of Cape Bon Ami, and continues for a mile, the layers of igneous rock 
 are interstratified with limestones and calcareous shales, abounding in 
 fossils. Among the species are Favosites G-oihlandica, F. basaltica, F. 
 polymorpha, with two undetermined species of Zaphrentis, Strophomena 
 rhomboidalis, S. punctuliferaf two undetermined species of Orthis, and 
 two of Spirifera, Atrypa reticularis, an undetermined species each of 
 Athyris and Orthoceras, with Calymene Blumenbacliii. 
 
 The inference to be drawn from these details is, that the lower rocks in 
 the valley of the Restigouche, from the mouth of the Matapedia downwards, 
 constitute a trough, containing a calcareous and a silicious series. These 
 are probably contemporaneous with the Gaspe* limestones, and their over- 
 lying conglomerates and sandstones. The intrusive rocks, which are so 
 abundant in this basin, mark a period of disturbance, whose influence has 
 not unlikely been powerful in this part of the continent. 
 
 On this trough of lower rocks, the Bonaventure conglomerates repose 
 unconformably. Their northward limit is the mountain flank of the Gasp 
 table-land, which they follow in the line that has been described ; turning 
 sharply up to a nearly vertical attitude, for a short distance, as they approach 
 the intrusive rocks, and generally leaving a geographical depression between 
 . their basset edges and the mountain flank. Between Tracadigash and the 
 Nouvelle River, the strip occupied by the Bonaventure conglomerates on' 
 the coast, is flat and narrow, the width not being a mile ; but between the 
 Nouvelle and the Scaumenac, though their dip is gentle, these rocks rise 
 into hills, which occupy a breadth of four miles, and form the coast from 
 Maguasha Point to High Cape. This is their western limit in the district 
 which has come under the examination of the Survey. 
 
CHAP. XVI.] DISTRIBUTION OF THE GASPti SERIES. 451 
 
 On the New Brunswick side of the Restigouche, a small portion of the 
 Bonaventure formation is seen lying unconformably on the trap and lower 
 conglomerate of Point La Lime, on the south side of the Campbelltown road, 
 just in the rear of the point. None of it has been observed at Dalhousie ; Dainousie. 
 between which place and Jacket River, the coast has not been examined. 
 Huron Island is however supposed to belong to this formation ; and between 
 Jacket River and Bathurst, it is displayed, in many places, resting in a 
 nearly horizontal attitude upon fossiliferous limestones, trap, and silicious 
 conglomerates. These are repeated several times in the distance, through 
 the effect of undulations. 
 
 The flat red rocks in the vicinity of Bathurst belong to this formation ; Bathurst. 
 and on the left bank of the Nipisiguit, about a mile above the town, they 
 are found to contain fossil plants, which are partly converted into coal, 
 and partly replaced by vitreous sulphuret of copper, in a manner similar 
 to those at the Joggins in Nova Scotia, on the Bay of Fundy. At this 
 spot, on the Nipisiguit, an attempt was made about twenty years since, by 
 the Gloucester Mining Company, to work the deposit for copper ore ; but 
 the irregular distribution of the organic remains rendered the operations 
 uncertain, and induced the abandonment of the adventure. The strata 
 are very nearly horizontal; and they present the following section, in 
 descending order : 
 
 Ft. in. 
 
 Chocolate-red micaceo-arenaceous shale, with casts of shrinkage cracks, . . 30 
 
 White quartzose conglomerate, the thickest part of which is two feet, 
 diminishing in one direction to two inches, in the space of fifteen 
 yards. The bottom is very white, and contains quartz pebbles, some 
 of which are an inch in diameter, 1 
 
 Whitish-red argillo-arenaceous shale, forming a passage to the next bed 
 
 below, 6 
 
 Bluish-grey argillo-arenaceous shale in parallel layers ; the bed thins out 
 
 in about thirty yards up the stream. It is charged with the remains Copper ore. 
 
 of broken plants, some of which are replaced by vitreous sulphuret 
 
 of copper, coated with a thin covering of green carbonate. Some are 
 
 in part replaced by the copper ore, and partly converted into coal. 
 
 Small nodules of the sulphuret of copper also occur, chiefly in the 
 
 lower part, and traces of nickel are said to have been found in some 
 
 of them. The greatest thickness of the bed is four feet; its average,. . 2 
 
 White quartzose conglomerate, similar to that of the summit. This does 
 
 not thin out in the distance examined, about fifty yards, 4 
 
 Red sandstone conglomerate, with white quartz pebbles ; of which some 
 
 would weigh three ounces, 6 
 
 Red shale, 6 
 
 Red sandstone conglomerate, with quartz pebbles, some weighing a pound 
 
 and a half, 10 
 
 59 6 
 
 At Rough Waters, three miles up the Nipisiguit from Bathurst Harbour, 
 the Bonaventure rocks are found lying in a nearly horizontal attitude upon 
 
452 
 
 GEODOGY OF CANADA. 
 
 [CHAP. XVI. 
 
 
 Granite. 
 
 Age of the 
 granites. 
 
 a mass of granite, and filling the inequalities of its surface. The granite 
 is fine grained, and is composed of white feldspar, colorless translucent 
 quartz, and black mica. At the immediate junction of the two rocks, the 
 red sandstones seem slightly harder than in other parts, while the granite 
 is softer. The feldspar is very white and opaque ; and two or three feet of 
 the surface have a schistose structure, as if from the stratification and 
 solidification of a layer of disintegrated granite. In some places, the 
 lowest of the red strata terminate abruptly against a vertical granite 
 ledge, and present the semblance of a dislocation at the spot ; but the 
 even continuity of the overlying beds plainly shows this to be the result 
 of original deposit upon an uneven surface. 
 
 Where the junction of the sandstones and the granite is first seen, the 
 former are thirty feet thick ; but as the surface of the granite gradually rises, 
 up the river, while the sandstones maintain their nearly horizontal atti- 
 tude, these gradually thin out and disappear. At Rough Waters, there is 
 a porphyritic dyke, consisting of reddish compact feldspar inclosing red 
 crystals of the same mineral : it has an underlie S. < 60. Granite of the 
 same character as that of Rough Waters, is seen up the Middle River, 250 
 yards from its junction with Bathurst Harbour. The resemblance of this 
 granite to that of the Eastern Townships, and the distribution of a simi- 
 lar granite, from the state of Vermont, through Maine, to New Brunswick, 
 leave little doubt that they are all of the same age. The intruded masses 
 of this rock in the Eastern Townships, as we have seen, intersect the 
 Devonian strata, and those of Bathurst are here shown to underlie the 
 Bonaventure formation, which belongs to the Carboniferous period ; so that 
 the eruption of the white granites of this part of North America, appears 
 to have taken place, at or near the close of the Devonian period. 
 
 Proceeding along the coast of New Brunswick, to the north-east of Bath- 
 urst, after an interval concealed by sand, red sandstones again occur, at 
 Salmon Beach, four miles from the entrance to the Harbour. They are 
 exposed for 156 yards across the measures, and their dip appears to be N. 
 40 E. < 9. Five miles farther, after another interval of sand, a succes- 
 sion of greenish-grey or drab sandstones, no doubt overlying the former, 
 make their appearance, dipping N. 20 E. < l-2. These commence 
 at Ellis Brook, west of Cranberry Cape ; and the measures to the eastward 
 are not again concealed for a very considerable distance along the coast. 
 point Dumai. As far as Point Dumai, twelve miles from Cranberry Cape, the succession 
 of beds, that can be seen and followed in the cliffs, which vary from twenty 
 to a hundred feet in height, amounts to very nearly 400 feet. 
 
 In this section, two regular coal seams occur, within 132 feet of each 
 other, the upper one eight inches, and the lower six inches thick. Each 
 of these is underlaid by the argillaceous root-bed, or under-clay, which 
 supported the plants of whose ruins they are composed. These under-clays 
 
 Coal seams. 
 
CHAP. XVLJ DISTRIBUTION OP THE GASPfi SERIES. 453 
 
 are thickly penetrated by Stigmaria ficoides, and studded with occasional 
 nodules of argillaceous carbonate of iron. The roof of the upper coal 
 seam, consists of a dark bluish-grey argillaceous shale, and contains an 
 abundance of ferns and other plants. Among them are Pecopt&ris SerlU, 
 P. nervosa, an undetermined Sphenopteris, 8. latifolia, an undetermined 
 species of Aster opTiyllites, with A. galioides, Cordaites borassifolia, 
 Sphenophyllum Schlotheimi, Noeggerafhia flabellata, with undetermined 
 species of Bechera, Lepidodendron, Calamites, and Oyperites. 
 
 By thus tracing the Bonaventure conglomerates and sandstones round 
 the Bay of Chaleurs, to Bathurst, their relation to the nearest coal seams 
 of New Brunswick, is made out with a considerable degree of certainty. 
 The general dip of the Bonaventure formation in Canada accords with the 
 result thus arrived at. Its slope towards the bay, would carry it beneath 
 the coal-bearing strata on the south side ; where no rock of a similar char- 
 acter is seen to overlie the coal measures. The only fossils which have Bonaventure 
 been met with in this formation, are certain large plants, converted into formation< 
 coal, which occur in the vertical beds on the south side of Malbay ; and 
 although the external markings of these fossils give nothing by which 
 to determine their species, they offer no contradiction to the stratigraphical 
 evidence. 
 
 The Bonaventure formation appears to be the very base of the coal coal formation, 
 series, in so far as Gaspe* is concerned ; and its distribution in Canada 
 shows that a narrow margin on the north shore of the Bay of Chaleurs 
 may be considered as the limit, in that direction, of the great eastern 
 coal field of North America. 
 
 We here conclude the general description of the rock formations of 
 the province, and of their distribution, so far as yet examined ; with the 
 exception of the diluvium or drift formation, which is reserved for a subse- 
 quent chapter. The mineralogical and chemical history of these rocks will 
 now be given in successive chapters, on their mineral species, the compo- 
 sition of the stratified and unstratified rocks, and the mineral waters. 
 These will be followed by particular descriptions of the economic rocks 
 and minerals of the province ; reserving for the Appendix a complete list of 
 the organic remains, with a large number of figures in addition to those 
 already given. 
 
454 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 CHAPTER XVII. 
 
 MINERAL SPECIES. 
 
 ARRANGEMENT. CARBONATES. SULPHATES. PHOSPHATES. FLUORIDS. SILICATES. 
 METALLIC ORES AND METALS. CARBONACEOUS MINERALS. SULPHUR. 
 
 In the preceding chapters, we have, in describing the different rock 
 formations, made mention of the greater number of the mineral species 
 which these contain. It is now proposed, as preliminary to a chemical and 
 mineralogical description of these rocks, to notice in succession the various 
 minerals, which have, up to the present time, been observed in the 
 province. Under each species, will be given the most interesting facts in 
 its history, so far as regards its occurrence in Canada, its associations, and 
 Classification, its chemical composition. Without attempting to follow a rigidly scientific 
 classification, we shall first notice the carbonates, sulphates, phosphates, 
 and fluorids, and then proceed to the silicates ; reserving for the last, the 
 metallic ores and combustible minerals. The history of the mineral sub- 
 stances which are found dissolved in our natural waters, will be given in the 
 chapter on the mineral waters of Canada. 
 
 CARBONATES OF LIME AND MAGNESIA. 
 
 CALCITE. 
 
 calcareous Finely crystallized forms of calcareous spar are abundant in many of 
 8 P ar ' the mineral veins on Lake Superior, and on Lake Huron ; some of these 
 
 have afforded transparent cleavable varieties like Iceland spar. At Har- 
 rison's location on St. Ignace Island, a calcite of this kind is found, some 
 portions of which are filled with small brilliant crystals of native copper, 
 giving it the aspect of aventurine. At the Bruce Mines, large scaleno- 
 hedrons occur, with pearl-spar and quartz. Large semi-transparent very 
 obtuse rhombohedrons have been found in veins, in the Trenton limestone 
 
CHAP. XVIL] MINERAL SPECIES. 455 
 
 group, near Lachine ; and similar varieties are met with in various other 
 localities in the same formation. Huntingdon, in Hastings county, is 
 cited by Professor Chapman as affording remarkable crystals. Crystals 
 of the primary rhombohedron occur in the dolomites of Point Le*vis, on 
 the walls of fissures, which are filled with crystals of quartz and a bitu- 
 minous matter ; sometimes with pyrites. The variety known as dog-tooth 
 spar, is abundant, lining cavities in the dolomites of the Niagara formation : 
 the crystals are generally implanted on those of pearl-spar. Mention has 
 already been made of the concentric masses of carbonate of lime, with a 
 concretionary fibrous structure, which are found in the limestones of the 
 Quebec group, and are abundant at Point Le'vis, Orleans Island, and at 
 Acton. These masses have sometimes been mistaken for fossil corals, but Travertine, 
 resemble still more the travertines formed by certain mineral waters of the 
 present day ; with which they are probably identical. Masses of crystal- 
 line travertine occur in fissures in the gypsiferous rocks, at Oneida and 
 elsewhere. Recent deposits of a similar nature, from calcareous springs, 
 are abundant in many parts of Western Canada ; as at Dundas, Niagara, 
 Woodstock, and near Toronto. These travertines are sometimes solid and 
 crystalline, like alabaster ; and at others, porous and tufaceous. They 
 often enclose or incrust mosses, leaves, and branches of trees. In the 
 township of York, on a small tributary of the Don, beds of tufa occur, from 
 twelve to fifteen feet in thickness, and are overlaid by sand and clay. 
 Deposits of this substance are abundant in many places, along the base of 
 the escarpment formed by the Niagara formation, in the counties of Grey 
 and Simcoe. They are constantly in process of formation. We may also 
 in this connection mention the fresh-water marls, which are nearly pure 
 carbonate of lime : these are abundant in our lakes and marshes. 
 
 The particular history of the great masses of carbonate of lime which 
 constitute the various limestone formations, will be given in a subsequent 
 chapter. We may here, however, notice a peculiar variety of fetid 
 carbonate of lime, which forms a large bed in the Laurentian series, 
 in Grenville. It is a very coarse-grained cleavable, milk-white, and Fetid caicite. 
 apparently pure caicite, which, when struck or very slightly scratched, 
 evolves a most powerful and unpleasant odor, recalling somewhat that 
 of phosphuretted hydrogen. It dissolves without residue in dilute acids ; 
 and the carbonic acid gas evolved does not affect solutions of lead or 
 silver-salts, so that it is difficult to say to what the peculiar smell of this 
 singular rock can be due. It is entirely distinct from the bituminous odor, 
 which is evolved by percussion from a great many of the limestones of the 
 palaeozoic series, or from that produced by striking some silicious rocks. 
 
456 GEOLOGY OP CANADA. [CHAP. XVII. 
 
 ABRAGONITE. 
 
 Arragonite. This species has been observed forming stalactites and delicate fibrous 
 masses, in a calcareous rock, in the township of Tring. A similar variety, 
 according to Dr. Bigsby, was found in a vein in the limestone of Lachine. 
 
 DOLOMITE. 
 
 Dolomite. Crystallized dolomite, which is often known by the names of pearl-spar 
 and bitter-spar, is abundant in cavities and geodes in the dolomites of 
 the Niagara formation in Western Canada ; where it is generally asso- 
 ciated with calcite, in the form of dog-tooth spar, and with gypsum. Anhy- 
 drite, the sulphates of baryta and strontia, quartz, and fluor-spar, more 
 rarely occur crystallized in these geodes. The dolomites of the Calciferous 
 
 Pearl-spar, formation, which resemble those of the Niagara, in like manner contain 
 geodes of pearl-spar, with calcite, gypsum, heavy-spar, and quartz, in 
 many localities. 
 
 In the copper-bearing quartz veins at the Bruce mines, crystallized pearl- 
 spar is also found with calcite. In one instance, a crystalline massive 
 variety forms a veritable wall of dolomite, varying from a few inches to two 
 feet in thickness, and running through the middle of a metalliferous quartz 
 vein, which traverses diorite. 
 
 Among the altered rocks of the Quebec group, dolomite is often inti- 
 mately mixed with serpentine, forming a variety of ophiolite ; or, in the 
 form of crystals of bitter-spar, is disseminated in steatite, in which it some- 
 times forms veins, as at Leeds ; where a ferruginous bitter-spar is the 
 gangue of copper-glance, specular iron, and native gold. It is also abun- 
 dant in many of the quartz veins of this mineral region. 
 
 Magnesian Dolomites, or magnesian limestones, which consist of variable mixtures 
 
 limestones. O f (J } om ite with pure carbonate of lime, are developed to a very great 
 extent in Canada. Besides forming great beds among the Laurentian 
 limestones, and rendering those of the Huronian series more or less mag- 
 nesian, dolomites make up the chief part of the so-called Calciferous for- 
 mation, which was formerly known as the Calciferous sandrock ; and are 
 developed on a great scale in its geological equivalent, the Quebec group ; 
 where they present varieties remarkable for containing large portions of 
 carbonates of iron and manganese. The so-called limestones of the whole 
 Middle and Upper Silurian series in Western Canada, are, with few excep- 
 tions, dolomites ; including the Clinton, Niagara, Guelph, and Onondaga 
 formations. The Devonian limestones of that region are not generally 
 magnesian ; but in Eastern Canada, the fossiliferous limestones of that age, 
 at Duds well, are curiously penetrated by veins of dolomite, constituting a 
 
 congiom- sort of breccia. Conglomerates or breccias, with a magnesian cement, 
 also occur in the Quebec group, in many places, and in the Chazy formation 
 
CHAP. XVII.] MINERAL SPECIES. 457 
 
 at Montreal. A much more recent dolomitic conglomerate, which encloses 
 fragments of fossiliferous limestone of the Lower Helderberg formation, 
 occurs on the Island of St. Helen. Dolomite also occurs, replacing 
 the remains of great numbers of fossils in the Trenton limestone, at Ot- 
 tawa. Corals, brachiopods, gasteropods, cephalopods, and Crustacea, are FOSSHS replaced 
 alike replaced by a white, translucent, crystalline, reddish-weathering dolo- by dolomite - 
 mite. This also forms small seams in the bluish-grey compact limestone, 
 which contains 3' 9 per cent, of clay, with a little oxyd of iron, but no 
 magnesia. A fragment of an Orthoceras from this rock was nearly solid, 
 but had drusy cavities filled with pearl-spar and quartz. Its analysis gave : 
 carbonate of lime 56*00, carbonate of magnesia 37' 80, carbonate of iron 
 5.95 = 99' 75. Similar dolomitic casts of orthoceratites are found in a 
 grey earthy, non-magnesian limestone, of the Chazy formation, near Mont- 
 real, and at the Mingan Islands. We reserve for another, place some 
 inquiries into the origin of dolomite, and likewise a series of analyses of 
 dolomites and various limestones, from different formations. 
 
 HAGNB8ITB. 
 
 Carbonate of magnesia has hitherto but rarely been recognized as form- 
 ing rock masses ; but it is probably much more abundant than has been 
 supposed, and may have often been mistaken for dolomite, which it re- 
 sembles. Beds of a rock, consisting chiefly of carbonate of magnesia, 
 with variable proportions of carbonate of iron, occur in several places 
 among the strata of the Quebec group, associated with serpentine, dolo- 
 mite, and steatite. On the twelfth lot of the seventh range of Sutton, it sutton, 
 forms a bed a foot thick, associated with the latter two rocks, in grey 
 micaceous schists. 
 
 It is mingled with grains of a feldspathic mineral, and with small 
 scales of green mica; giving the whole the aspect of a bright green, very 
 micaceous gneiss, weathering rusty-red. The proportion of soluble car- 
 bonates in the rock is variable ; a pure, slightly colored fragment gave 
 carbonate of magnesia 83*35, carbonate of iron 9-02, insoluble 8'03 = 
 100-40. Another portion gave carbonate of magnesia 33-00, carbonate 
 of iron 19-35, alumina 0-50, insoluble 45-90 = 98-70. The specimens 
 contained small grains of nickeliferous pyrites ; but the insoluble residue, 
 after the action of nitric acid, still retains a portion of nickel as an insoluble 
 silicate, and has a bright green color, apparently due to a small amount 
 of oxyd of chromium, which it also contains. It is essentially a silicate of 
 alumina and alkalies, chiefly soda, with traces only of magnesia and of iron ; 
 and is apparently a mixture of feldspar with a green chromiferous mica. 
 
 The magnesite rock of the seventeenth lot of the ninth range of Bolton Boiton. 
 forms a bed many yards wide ; interstratified between steatite on one side, 
 and an impure serpentine, passing into diorite, on the other. It resembles 
 
458 GEOLOGY OP CANADA. [CHAP. XVII. 
 
 a crystalline limestone, and is made up of strongly coherent cleavable 
 grains of magnesian spar, whitish or bluish-grey in color, and weathering 
 rusty red ; with grains and small irregular veins of hyaline quartz. It is 
 stained here and there with a yellowish-green hydrocarbonate of nickel, 
 which incrusts the joints of the rock. It also contains small grains of 
 pyrites, small portions of some green chromiferous silicate, and occasionally 
 a little carbonate of lime. Analyses of two different portions gave carbo- 
 nate of magnesia 59-13, carbonate of iron 8-32, insoluble 32-20 = 99-65 ; 
 and carbonate of magnesia 59-72, carbonate of iron 10- 31, insoluble 29-90 
 = 99-93. The insoluble matter was nearly pure quartz, yielding 93-6 
 per cent, of silica, with a little alumina, alkali, and oxyd of chrome. 
 
 Magnesite also occurs on the twenty-fourth lot of the ninth range of 
 Bolton, where it forms beds in argillite. It here appears as a compact 
 rock, with a conchoidal fracture, bluish-grey within, but weathering reddish- 
 brown. It contains, like the others, a mixture of silicious matter, and a 
 portion of carbonate of iron. This variety can scarcely be distinguished, 
 by its external characters, from the magnesian limestones so common in the 
 same region. 
 
 SULPHATES, PHOSPHATES, AND FLUOEIDS. 
 
 HEAVY-SPAR. 
 
 Heavy-spar. Heavy-spar, or sulphate of baryta, is found in many localities in 
 Canada. In the Laurentian series several veins of this mineral have been 
 observed. One of these, on the second lot of the eighth concession of 
 Lansdowne, intersects the crystalline limestone, and is in some parts mixed 
 with calcite and galena. In other parts, the whole vein consists of nearly 
 pure heavy-spar, forming large tabular crystalline masses, which are semi- 
 transparent, and bluish or rarely reddish in color. Well denned crystals 
 are met with in cavities in the vein. The township of Dummer is also 
 cited as a locality by Prof. Chapman. 
 
 On the fourth lot of the sixth range of Bathurst, a vein of opaque white 
 lamellar heavy-spar, said to be about a foot wide, is found in gneiss. It 
 contains small grains of copper pyrites. Heavy-spar is also met with in 
 MacNab, at the mouth of the Dochart ; and a red variety is associated with 
 purple fluor-spar in cavities in the Laurentian limestone near the hematite 
 of Iron Island, Lake Nipissing. 
 
 Sulphate of baryta is abundant in many of the veins on the north shore 
 of Lake Superior, and sometimes makes up a great proportion of the vein. 
 An interesting locality, according to Dr. Bigsby, is on a large and lofty 
 
CHAP. XVII.] MINERAL SPECIES. 459 
 
 island, three miles east of Gravelly Point, and sixty-three east of Fort 
 William. Here the mineral occurs lining fissures in a porphyry, with green 
 octahedral fluor-spar. It is also occasionally met with in the copper veins of 
 the Bruce mines. Small veins of massive white heavy-spar are met with 
 intersecting the serpentines of the Bras, a tributary of the Chaudire. The 
 same mineral occurs crystallized in geodes, in the dolomites of the Calcif- 
 erous formation, and is said to be occasionally found in those of the 
 Niagara formation at Niagara Falls. Small almond-shaped masses of a 
 reddish cleavable variety of heavy-spar are found, with gypsum, imbedded 
 in shales of the Hudson River formation, at Cape Rich. 
 
 CELESTIKE. 
 
 Celestine, or sulphate of strontia, abounds in the limestones of the sulphate of 
 Trenton group, at Kingston, and in its vicinity. Dr. Thompson gave the 8t 
 name of baryto-celestine to specimens from this region, which, according 
 to him, contained thirty-five per cent, of sulphate of baryta. The speci- 
 mens from Kingston in the collection of the Geological Survey, were, 
 however, found to be pure sulphate of strontia, without a trace of baryta, 
 and to have a specific gravity of 3-96. It occurs in white translucent 
 crystalline foliated masses, which are sometimes radiated, and often several 
 inches in diameter. These are generally associated with calcite, blende, 
 and iron pyrites. Sulphate of strontia, according to Dr. Bigsby, occurs 
 in sky-blue prismatic crystals, in a similar limestone on the right bank of 
 the Ottawa, near the head of the Long Sault. A fibrous variety occurs 
 also in limestone, at the narrows of Lake Simcoe, near the Severn, with 
 selenite, on the Grand Manitoulin, and at Niagara Falls. 
 
 Gypsum, or hydrous sulphate of lime, has already been mentioned as Gypsum, 
 occurring with pearl-spar, in the dolomites of the Niagara formation. It is 
 abundant in these, not only in a lamellar form (selenite), but in compact 
 snow-white masses, sometimes several inches in diameter ; filling rounded 
 cavities in the dolomite, which are often lined with crystals of quartz. It is 
 met with in similar conditions in some of the dolomites of the Clinton and 
 the Calciferous formations. Cavities in the latter, at Beauharnois, and 
 elsewhere, are lined with calcite and quartz crystals, and filled with compact 
 and lamellar gypsum. Small almond-shaped masses of reddish gypsum 
 occur in the Hudson River shales at Point Rich, along with heavy-spar ; 
 and a bed of soft bluish shale in the Medina formation, at St. Vincent, 
 contains an abundance of isolated crystals of gypsum, an inch or more in 
 length. Large masses of transparent selenite, according to Dr. Bigsby, 
 occur in the limestones of Hudson's Bay. The great workable deposits of 
 gypsum in Canada, are interstratified with the magnesian limestones and 
 
460 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVII. 
 
 shales of the Onondaga formation, under which head they have already 
 been described. 
 
 ANHYDRITE. 
 
 Anhydrite. 
 
 This species is not yet known to occur in Canada; but the Niagara 
 formation in western New York has afforded a foliated transparent variety, 
 which occurs in the geodes, common to the dolomites of that series. 
 
 EPSOM SALT. 
 
 Sulphate of 
 magnesia. 
 
 Epsom salt, or sulphate of magnesia, besides predominating in the waters 
 of some mineral springs, is found upon the dolomites of the Clinton forma- 
 tion, at various points along their outcrop from Niagara Falls to Lake Huron. 
 It generally occurs as a crystalline incrustation upon sheltered surfaces of 
 the rock, and, in such cases, evidently results from the evaporation of 
 exuding waters. These crusts, at Dundas, are sometimes an inch in thick- 
 ness. Near Niagara, however, it is said to be found with gypsum, in geodes 
 in the rock. Sulphate of magnesia has been observed in other countries, 
 associated with gypsum, apparently as a contemporaneous deposit ; and it is 
 probable, that here in the Clinton formation, also, it is derived from an ori- 
 ginal impregnation of these gypsum-bearing dolomites with the salt ; instead 
 of being, as some have supposed, the result of a subsequent reaction 
 between the gypsum and the dolomite. 
 
 Sulphate of magnesia has also been observed as an efflorescence on a 
 serpentine rock, near the iron-ore bed of Crow Lake, in Marmora ; where it 
 may arise from the action of sulphuric acid from oxydizing pyrites, upon 
 the magnesian silicate. An abundant efflorescence of the same salt has 
 been observed in the black shales of the Utica formation, along the line of 
 the aqueduct, near Montreal, when these are first quarried and exposed 
 to the weather ; and it is also seen upon the black shales of Quebec. 
 
 APATITB. 
 
 Phosphate of Apatite, or phosphate of lime, is a common mineral in the limestones 
 Ume - of the Laurentian series, sometimes disseminated hi minute and rare blue 
 
 or green crystals ; but at other times so abundant, as to make up a great 
 proportion of the rock, and in some cases to form beds of a nearly pure 
 crystalline apatite. The most remarkable localities known in Canada, are 
 in North Elmsley and in South Burgess. In the former township, the 
 mineral has been traced across the lots twenty-four, twenty-five, and 
 twenty-six of the eighth range, for about a mile in a south-west direc- 
 tion ; and it appears to be continued into South Burgess, on the second 
 lot of the seventh, and from the seventh to the tenth lot of the fifth range. 
 It has been quarried to a small extent on the twenty-fifth lot of the eighth 
 range of North Elmsley, where it seems to form an irregular bed, having a 
 
CHAP. XVII.] MINERAL SPECIES. 461 
 
 breadth of about ten feet ; of which three feet are nearly pure crystalline 
 sea-green apatite, with only a small admixture of black mica. In the 
 remaining portion, it is mingled with the limestone, the phosphate largely 
 predominating, and sometimes forming prisms a foot or more in length, and 
 four inches in diameter. These are generally rough, but often terminated, and, 
 as well as the smaller ones, have always their angles rounded. Large prisms 
 of it are also found in a bed of quartzite near the limestone. The apatite is 
 sometimes associated with large crystals of pyroxene, and of phlogopite : in 
 one of the latter, about four inches in diameter, a crystal of apatite, a quar- 
 ter of an inch thick and two inches long, was found imbedded, the axis of 
 the prism being parallel with the cleavage of the mica. Rounded masses 
 of calcite are often enclosed in the apatite ; which, hi its turn, is frequently 
 in rounded pale-green crystalline masses, imbedded hi the coarse-grained 
 limestone. The phosphate of lime of Burgess belongs to the variety called Fiuor-apatite. 
 fluor-apatite, and contains only about 0-5 per cent, of chlorine. 
 
 A similar locality of apatite occurs in the township of Ross, where large 
 olive-green terminated crystals, with rounded angles, are imbedded in a 
 yellowish crystalline limestone, which at the same time contains a consider- 
 able proportion of cleavable grains of purple fluor-spar, and crystals of 
 black spinel. In some bands of this limestone, small crystals of the apatite, 
 with grains of fluor-spar, make up more than one half of the mass. Another 
 locality is at the foot of the Calumet Falls ; where crystals of blue apatite, 
 and of quartz, are imbedded in a coarsely cleavable sky-blue calcareous 
 spar. Apatite is also met with in some abundance, in crystalline limestone, 
 near Blaisdell's mill, on the Gatineau. 
 
 At St. Roch, on the Achigan River , there occurs an intrusive mass of 
 fine grained grey dolerite, in which, besides crystals of augite, small hexa- 
 gonal prisms of apatite are rather abundantly disseminated. These are 
 transparent, pink or purple in color, and sometimes an inch in length, and 
 one or two lines in diameter: their surfaces are often dull, and their 
 angles are rounded. 
 
 Nodules, composed in great part of phosphate of lime, occur in many coproiites. 
 localities in the Lower Silurian rocks, and appear to be coproiites. In 
 some cases, at least, they exhibit imbedded fragments of the shells of Lin- 
 gula, which was probably the source of the phosphate of lime. We have 
 shown that the horny translucent shells of Lingula and Orbicula, both of 8t 
 recent and fossil species, together with Oonularia and Serpulites, differ 
 entirely from those of other mollusks, and, like the bones of vertebrate 
 animals, consist for the greater part of phosphate of lime. The shell of 
 Lingula ovalis (Reeve), a recent species, left, by calcination, 61-00 per 
 cent, of fixed residue ; which consisted of phosphate of lime 85' TO, car- 
 bonate of lime 11-75, magnesia 2-80 = 100-34. 
 
462 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 Among the localities of these phosphatic nodules, we may mention the 
 Chazy formation at Allumette Island, where they are abundant in a coarse 
 grained sandstone. Not only does the phosphatic paste enclose fragments 
 of Linguta, but it is found filling the moulds of Pleurotomaria or Holopea. 
 These masses, which are sometimes an inch thick and two inches long, are 
 chocolate-colored, and contain imbedded grains of white silicious sand. 
 When heated, they disengage a strongly ammoniacal water, with an odor 
 of burnt horn. Smaller fragments of a similar phosphatic material are 
 found at Grenville, in sandstone beds, which belong to the same formation 
 as the last. The Chazy limestone at Hawkesbury and Lochiel also encloses 
 phosphatic nodules, from one fourth of an inch to an inch in diameter, 
 blackish-brown without, but yellowish-brown within, and giving off abun- 
 dance of ammonia when heated. Fine examples of similar coprolites have 
 been found in the graptolitic shales of Point LeVis, and at Riviere Ouelle 
 in a calcareous conglomerate, both of the Quebec group. At the latter 
 locality, the phosphatic masses are very abundant, and often assume curious 
 imitative shapes. 
 
 A specimen from Allumette Island had a specific gravity of 2-875, 
 and gave as follows : phosphate of lime (bone earth) 36-38, carbonate of 
 lime, with some fluorid, 5-00, magnesia and peroxyd of iron, by difference, 
 7-02, insoluble 49-90, volatile matter 1-70 = 100-00. The insoluble matter, 
 which consists of silicious sand, equalled 38*00 per cent, in another fragment. 
 A specimen from Hawkesbury gave phosphate of lime 44-70, carbonate of 
 lime 6*60, carbonate of magnesia 4-76, peroxyd of iron and a trace of 
 alumina 8-60, insoluble sand 27-90, volatile 5-00 = 97-56. 
 
 One from Riviere Ouelle, with a specific gravity of 3*15, afforded 
 phosphate of lime 40-34, carbonate of lime, with some fluorid, 5-14, carbo- 
 nate of magnesia 9-70, peroxyd of iron, with traces of manganese, and a 
 little alumina, 12-62, insoluble silicious residue 25*44, volatile 2-13 = 
 95*37. In the latter specimen, the microscope shows, besides grains 
 of quartz, small cylindrical bodies, resembling the spiculae of sponges. 
 The large amount of iron in the nodules from Riviere Ouelle, appears to 
 exist as a carbonate of the protoxyd ; and is evidently connected with the 
 presence of an abundance of iron pyrites, which surrounds the phosphatic 
 masses, and points to the action of organic matters on a solution of sulphate 
 of iron; whose reduction must yield an atom of protoxyd of iron for 
 each one of bisulphuret : 2 (FeO, S0 3 ) == FeS 2 + FeO + 7 . Small 
 hollow cylindrical masses, found in the sandstones in that locality, resemble 
 bones. They appear to be homogeneous under the microscope, and are only 
 serpuiitee. incrusted with silicious sand. These, which are supposed to be Serpulites, 
 differ in their composition from the soluble portion of the nodules, in con- 
 taining a much less proportion of iron. An analysis gave phosphate of 
 lime 67*53, carbonate of lime 4-35, magnesia 1-65, protoxyd of iron 2-95, 
 
CHAP. XVIL] MINERAL SPECIES. 463 
 
 volatile 2-15, adhering sand 21-10 = 99-73. All of these bodies give 
 evidences of the presence of fluorine ; and of azotized organic matters, which 
 evolve ammonia, with an animal odor, when heated. (American Journal 
 of Science, July 1854, [2,] xvn, 235.) 
 
 FLUOK-8PAB. 
 
 This mineral has been met with hi several localities in Canada, but is 
 rarely found in great abundance. Green and purple fluor-spar frequently 
 occur in the mineral veins on Lake Superior : a purple variety is found on 
 the main land opposite Pic Island, filling veins in syenite ; and also with cal- 
 cite in amygdaloid, three miles east of Point Gargantua. Another locality 
 of green octahedral crystals, with heavy-spar, in porphyry on an island 
 near Gravelly Point, has been mentioned under the latter species. The 
 above localities were long since described by Dr. Bigsby. Green cubes of 
 fluor-spar also occur at Prince's mine, associated with quartz and calcite. 
 
 In the Laurentian rocks, purple fluor occurs, both granular, and in small 
 cubic crystals with heavy-spar, in fissures in the limestone on Iron Island, 
 Lake Nipissing. . The same mineral is found disseminated in purple cleav- 
 able grains, associated with green apatite, in a yellowish crystalline lime- 
 stone in Ross : the fluor-spar makes up from five to ten per cent, of the rock. 
 A small vein of the mineral is also met with in the vicinity. A specimen 
 of galena, said to be brought from the Gatineau, is imbedded in a crystal- 
 line lilac-colored fluor-spar. A green compact variety occurs in considerable 
 proportion, in veins of milk-white calcite, with galena, cutting the Potsdam 
 sandstone at Bay St. Paul and Murray Bay ; and a dark purple cleavable 
 fluor-spar, with white calcite, forming very fine specimens, is found in veins, 
 among the black slates, near the citadel of Quebec. A small vein of com- 
 pact purple fluor-spar has been observed in the grey fossiliferous limestone 
 of Montreal : its color is at once destroyed by heat. This mineral is also 
 occasionally found crystallized, with various other spars, in the geodes of 
 the dolomites of the Niagara formation. 
 
 SILICATES. 
 
 In describing the silicated minerals, it will be convenient to group them 
 into two classes : 1st, Non-aluminous silicates, chiefly of protoxyds, such 
 as lime, magnesia, and ferrous oxyd. 2nd, Aluminous silicates, which, 
 with the exception of a limited number of simple silicates of alumina, may 
 be represented as double silicates of alumina, and an alkaline or earthy 
 protoxyd. These two classes are connected, through the aluminous 
 pyroxenes and hornblendes. 
 
464 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 OLIVINE, OB OHBY8OLITE. 
 
 oiivine. This species has hitherto been recognized in but few localities in North 
 America. A nearly colorless transparent variety, the boltonite of Prof. C. 
 U. Shepard, occurs in the crystalline magnesian limestone of Bolton, in 
 Massachusetts, with asbestus, mica, and magnetic iron. It has a density 
 of 3-21; and its analysis gave to Prof. Brush, silica 42-82, magnesia 54-44, 
 protoxyd of iron 1-47, lime 0-85, volatile 0*76 = 100-34. A curious gran- 
 itoid dolerite, which is found in boulders at Thetford, in Vermont, contains 
 masses of green oiivine, sometimes an inch in diameter. This gave by 
 analysis, according to Mr. Manice (Am. Jour, of Science [2,] xxxi, 359), 
 silica 40*75, magnesia 50-28, protoxyd of iron 9-36 = 100-36. Many of 
 the dolerites in the vicinity of Montreal abound in oiivine. At Rougemont, 
 dykes of a fine grained greenish-black basalt, enclose numerous well defined 
 crystals of green oiivine, which appear in strong relief on the weathered 
 surfaces. A granitoid dolerite, with a white feldspathic base, which forms 
 a large portion of the same mountain, contains, besides black augite, small 
 honey-yellow grains of oiivine in abundance ; and a similar rock is found 
 in Mounts Royal and Montarville. In a portion of the latter, oiivine is the 
 predominant mineral, and occurs in olive or amber-colored imperfect crys- 
 tals, some tunes half an inch in diameter, forming 45-0 per cent, of the 
 rock. The powdered oiivine gelatinizes with hydrochloric acid in the cold, 
 and is almost instantly decomposed when warmed with sulphuric acid 
 diluted with an equal volume of water ; the silica separating chiefly in a 
 flocculent form, and enclosing small grains of the undecomposed mineral, 
 which are left after dissolving the ignited silica. A little silica is how- 
 ever retained in solution, and is precipitated by ammonia, with the oxyd 
 of iron. Two analyses of separate portions of this oiivine gave as follows, 
 after deducting the undecomposed mineral : 
 
 Oxygen. 
 
 Silica, 37-13 37-17 = 19-82 
 
 Magnesia, 39-36 39-68 = 13-87 
 
 Protoxyd of iron, 22-57 22-54 = 5-10 
 
 99-06 99-39 
 
 Oiivine has not yet been noticed among the magnesian rocks of the 
 Silurian period in Eastern Canada; but it occurs in the same geological 
 formation in the United States. Dr. Genth has lately described it in 
 disseminated grains in a talc slate from Webster, Jackson county, North 
 Carolina ; where it is associated with serpentine, pyrosclerite, quartz, and 
 chromic iron. The oiivine from this locality, like the accompanying 
 magnesian minerals, contains traces of oxyd of nickel. Grains of oiivine 
 also occur with the chromic iron of Loudon county, Virginia. (Am. Jour, 
 of Science, [2,] XXXH, 199.) 
 
CHAP. XVII.] MINERAL SPECIES. 465 
 
 CHONDKODITE. 
 
 Tliis fluosilicate of magnesia is much more common than chrysolite in Chondrodite. 
 crystalline limestones, and is often met with in those of the Laurentian 
 series, in Canada. The grains of chondrodite are sometimes so arranged 
 as to mark the stratification of the rock. In a specimen, the locality of 
 which is unknown, the contact of two beds of limestone, one marked by 
 grains of chondrodite, and the other by those of serpentine, is distinctly 
 seen. A similar association occurs in the limestones of St. Jerome. Fine 
 specimens of chondrodite are found, with small scales of graphite, in a 
 white crystalline limestone, from near Newborough. 
 
 LIEVKITE OK YENITE. 
 
 To this rare species is to be referred a silicate of iron, which probably 
 forms a bed in the Laurentian series, since a boulder of it nearly a foot in 
 diameter, was found in the vicinity of Ottawa. It contains some black mica, 
 and portions of red granular garnet ; but it consists, for the greater part, of 
 a mineral having a hardness of 5-5 and a density of 4*15-4*16. It weathers 
 of a rusty red ; but within, its lustre is sub-metallic, shining, and sometimes 
 iridescent. Its color is velvet-black, but its powder is yellowish ash-grey. 
 The mineral is slightly translucent on the edges, and is strongly magnetic. 
 It is brittle, with an uneven fracture, and cleaves imperfectly in two directions, 
 oblique to one another. Before the blowpipe, it intumesces, and yields a 
 black magnetic slag. The mineral gelatinizes with hydrochloric acid, and is 
 completely decomposed. Its analysis gave, silica 27*80, protoxyd of iron 
 56-52, peroxyd of iron 10*80, magnesia 2*59, lime 0*64, oxyd of manga- 
 nese, a trace, volatile 1*20 = 99*55. Another trial gave 28*20 of silica, 
 and 9*93 of peroxyd of iron. From its composition, not less than its 
 physical characters, this substance is regarded as a variety of lievrite. The 
 rock from which the mass was derived, has not been observed in place. 
 
 WOLLA8TONITE OB TABULAR-SPAR. 
 
 This silicate of lime is often found with the Laurentian limestones, in woiiastonite. 
 which it sometimes forms beds, occasionally mingled with carbonate of lime 
 or with quartz. At Grenville, it is associated with a dark green pyroxene 
 and a white feldspar ; forming a rock in which garnet, idocrase, sphene, 
 pyroxene, and graphite occur. Beautifully white fibrous masses of woiias- 
 tonite, several inches in length, are obtained in this locality. Its specific 
 gravity is 2*89-2*92, and its analysis gave to Mr. Bunce: silica 53*05, 
 lime 45*74, protoxyd of iron 1*20 = 99*99. In Bastard, a pale green 
 variety also forms a rock, with quartz and small scales of brown mica. 
 Other localities of tabular-spar are St. Jerome and Morin. 
 
466 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 HOKNBLENDE OB AMPHIBOLB. 
 
 Horn- The variety of hornblende called tremolite is abundant in the Lauren- 
 
 b]ende - tian limestones at the Calumet Falls, and in Blythfield and Dalhousie. 
 Short thick and highly modified prisms of a white transparent tremolite, 
 with a density of 2-97, have been observed by Prof. Chapman, in a white 
 crystalline limestone from Algona. The raphilite of Dr. Thompson, from 
 Lanark, is nothing but a fibrous, radiating, grey hornblende, having a hard- 
 ness of 5-5, and a specific gravity, when in powder, of 2-845. According 
 to Dr. Thompson, it contains ten per cent, of potash ; but an analysis of an 
 authentic specimen gave silica 55-30, lime 13-36, magnesia 22*50, protoxyd 
 of iron 6-30, alumina 0-40, manganese, traces, potash 0-25, soda 0-80, 
 volatile 0*30 = 99-21. Another specimen, which had been purified by 
 diluted hydrochloric acid, gave 57-20 of silica. The mineral is associated 
 with carbonate of lime and phlogopite. The same vicinity furnishes a 
 greenish-brown variety of actinolite, crystallized in prisms, and said by Dr. 
 Thompson to be manganesian. A pale green or bluish-green variety, which 
 may be referred to actinolite, or to pargasite, is common in druses in the 
 Pargasite. Laurentian limestones. Finely terminated crystals of dark green pargasite, 
 sometimes an inch in diameter, are found implanted upon, or imbedded in, 
 a greenish-white pyroxene, at the High Falls, and at the Ragged Chute, 
 on the Madawaska. A specimen in thick dark green, nearly opaque 
 prisms, from the former locality, had a specific gravity of 3-050-3-058, 
 and gave by analysis, silica 55-05, alumina 4-50, lime 13-44, magnesia 
 20-95, protoxyd of iron 5-85, volatile 0-35 = 100-14. Radiated masses of 
 green actinolite also occur imbedded in the finely granular magnetic iron 
 ore of Madoc. 
 
 Actinolite. Actinolite, disseminated in talc, occurs in beds with the serpentines of 
 the Lower Silurian series ; and a finely fibrous variety, without admixture, 
 sometimes forms great beds of a very tough greenish rock. Such a mass 
 occurs in St. Francis, Beauce, and gives by analysis, silica 52-30, lime 
 15-00, magnesia 21-50, protoxyd of iron 6-75, oxyd of nickel, traces, 
 alumina 1-30, volatile 3-10 = 99-95. Mixtures of greenish hornblende 
 with triclinic feldspars, form abundant beds of diorite in the same region. 
 Black horn- Black or greenish hornblende is very commonly disseminated through the 
 blende. feldspathic rocks of the Laurentian series ; giving rise to syenite and 
 syenitic gneiss, and also forming beds of hornblende rock, often schistose, 
 as at Blythfield, and at Lake St. John. Similar beds of black hornblende, 
 holding garnets, are found with the Silurian serpentines of Mount Albert. 
 Crystallized black hornblende enters abundantly into the diorites of 
 Yamaska Mountain and Mount Johnson, and is found sparingly, with black 
 mica, in the granitoid trachytes of Brome and Shefford Mountains. 
 
CHAP. XVtt.j MINERAL SPECIES. 4(57 
 
 OK ATJGITE, 
 
 This species is found abundantly in the Laurentian limestones, where a pyroxene, 
 light greyish or greenish variety (diopside or sahlite), sometimes forms 
 beds, or large segregated veins. Such is the case in Kildare ; where a rock 
 made up of nearly white cleavable pyroxene, with a little brown mica, is 
 interstratified with limestone. At the High Falls, and at the Ragged Chute, 
 on the Madawaska, a similar variety is associated with crystals of green 
 hornblende, which have just been described, and with black tourmaline. 
 The crystals of pale greyish-green pyroxene, often replaced on their acute 
 lateral edges, are sometimes several inches in diameter. Those associated Diopside. 
 with the hornblende, whose analysis is given above, have a specific gravity 
 of 3*273-3-275, and are composed of silica 54-20, lime 25-65, magne- 
 sia 17*02, protoxyd of iron 3-24, volatile 0-45 = 100-56. At the Calu- 
 met Falls similar; but slender crystals, sometimes six inches in length, 
 occur, with large crystals of olive-green binaxial mica, imbedded in flesh- 
 red crystalline limestone. 
 
 An interesting variety of pyroxene, found by Dr. Wilson, in Bathurst, Aluminous 
 forms crystalline masses, mixed with a little mica, calcite, apatite, copper p y roxen< 
 pyrites, and a pink crystalline mineral, to which the name of wilsonite has 
 been given. This pyroxene is massive, cleavable, and sometimes exhibits 
 small crystals. Its hardness is 6-5, and its density 3-19 ; its lustre is 
 vitreous, and pearly on the cleavage surfaces. It is colorless or greyish- 
 white, translucent, with an uneven, sub-conchoidal fracture. It contains a 
 portion of alumina replacing silica, a composition rarely met with in white 
 non-ferruginous pyroxenes. One of two concordant analyses gave, silica 
 51-50, alumina 6-15, peroxyd of iron 0*35, lime 23-80, magnesia 17-69, 
 volatile 1-10 = 100-59. A second yielded, silica 50-90, alumina and 
 peroxyd of iron 6'77, lime 23-74, magnesia 18-14, volatile 0-90 = 100-45. 
 The oxygen of the silica, in the first analysis, equals 27*28, and that of the 
 alumina 2-87, the sum being 30-05; while the oxygen of the other constit- 
 uents, the water included, amounts to 14*95. The ratio of these two 
 numbers is very nearly 2 : 1, or that of pyroxene. 
 
 Large white semi-transparent prisms, often an inch in diameter, and 
 highly modified, were many years since obtained in the vicinity of Ottawa, 
 and are figured in Shepard's Mineralogy. They were imbedded in crys- 
 talline limestone, and probably from a boulder. The density of these crys- 
 tals is 3*26-3-27, and their analysis gave silica 54-50, lime 25-87, mag- 
 nesia 18-14, protoxyd of iron 1-98, volatile 0-40 = 100-89. A granular 
 pyroxene rock which occurs with the ophiolite of Orford, has furnished 
 beautiful tabular twin-crystals, which line geodes, associated with cinnamon- 
 colored garnets, oT are grouped in bladed masses of an opaque greenish- 
 white. The crystals from the geode were opaque, and seemed somewhat 
 
468 GEOLOGY OF CANADA. [CHAP. XVIT. 
 
 earthy in their fracture, from incipient decomposition. Their density was 
 3-13 -3*15, and they gave by analysis, silica 54-50, lime 25-20, magnesia 
 15-29, protoxyd of iron 4-86, volatile 0-55 = 100-40. 
 
 Grenviiie. The dark green pyroxene of Grenville sometimes offers cleavage surfaces 
 of several inches in breadth ; and it often occurs in large prisms, with pitted 
 surfaces and rounded angles. Mixtures of similar pyroxene with orthoclase 
 and quartz, generally including sphene, are often found, apparently forming 
 beds among the limestones, as at Lachute, the Calumet Falls, and Elmsley. 
 Beds of green granular pyroxene (coccolite), either alone, or with black 
 mica, are also met with ; and grains of green pyroxene are very often dis- 
 seminated through the crystalline limestones, and sometimes through beds 
 of quartzite. The peculiar forms from the Laurentian limestone of Calumet 
 Island, resembling Stromatopora rugosa, have been figured on page 49. 
 When the somewhat magnesian limestone is removed by an acid, the fossil 
 is found to consist of an aggregation of brilliant crystalline grains of white 
 pyroxene, whose analysis gave silica 54-90, lime 27*67, magnesia 16-76, 
 volatile 0-80 = 100-13. 
 
 Hypers- The anorthosite rocks of the Laurentian series often contain a green 
 
 thene. granular or cleavable pyroxene, which passes into well characterized hy- 
 persthene. A specimen of this, associated with the andesine and ilmenite 
 of Chateau Richer, had a hardness of 6-0, and a density of 3-41. Its color 
 was blackish-brown, but yellowish-brown in thin laminae ; its streak and 
 powder ash-grey. One of two analyses gave silica 51-35, alumina 3-70, 
 protoxyd of iron, 20-56, lime 1-68, magnesia 22-59, volatile 0-10 = 99-98. 
 The second yielded silica 51-85, alumina 3-90, protoxyd of iron 20-20, 
 lime 1-60, magnesia 21-91, manganese, traces, volatile 0-20 = 99-66. 
 
 The name of augite is generally restricted to the black or dark colored 
 varieties of pyroxene, which occur in dolerite and similar rocks. The 
 
 Augite. dolerites of the district of Montreal often enclose crystals of black augite, 
 as in Montreal, Rougemont, and Montarville Mountains. The crystals 
 imbedded in the olivinitic dolerite of the latter, are short, thick, terminated 
 prisms, readily detached from their matrix. They have a hardness of 6-0, 
 and a specific gravity of 3-341. Their analysis gave silica 49-40, 
 alumina 6-70, lime 21-88, magnesia 13-06, peroxyd of iron 7-83, soda and 
 traces of potash 0-74, volatile 0-50 = 100-11. 
 
 DIALLAGE. 
 
 Diallage is generally regarded as a variety of pyroxene, and is classed 
 with bronzite and hypersthene, with which many varieties of it agree in 
 composition. The hypersthene of the Laurentian anorthosites is sometimes 
 replaced by a greenish sub-translucent diallage, which is probably of this 
 nature. Much that is known as diallage among serpentine rocks, is 
 however a hydrated . mineral, which should perhaps constitute a new spe- 
 
CHAP. XVIL] MINERAL SPECIES. 469 
 
 cies. Diallage is often associated with the serpentines of the Silurian 
 series in Canada, and sometimes forms rock-masses. A coarsely cleavable 
 bronze-colored variety from the township of Ham, where it forms a rock, 
 gave silica 50-00, magnesia 27*17, protoxyd of iron 13*59, lime 3*80, 
 water 6-30 = 100-86. Another rock from Orford consists of small 
 masses of celandine-green diallage, translucent, and with a pearly lustre, 
 imbedded in an amorphous soft greenish base. The specific gravity of 
 carefully selected fragments of this diallage was 3-02-3-03, and its hard- 
 ness was 5-0. These still enclosed grains of magnetic iron, which were 
 separated from the powder by a magnet, and equalled 4-37 per cent. 
 Two analyses of different specimens of the mineral thus purified, were 
 made, and gave as follows : 
 
 I. II. Oxygen. 
 
 Silica, 4*7-20 47-10 = 24-90 
 
 Alumina, 3-40 3-50 = 1-63 
 
 Lime, 11-36 11-34 = 3-24 
 
 Magnesia, 24-53 24-58 = 10-01 
 
 Protoxyd of iron, 8-91 8-55 = 1-89 
 
 Water, 5-80 5-85 = 5'20 
 
 Oxyds of nickel and chrome, traces traces 
 
 101-20 100-92 
 
 Warm dilute nitric acid removed nothing from the pulverized diallage, 
 nor from the rock. This gave, as a whole, silica 41-80, magnesia 26-13, 
 protoxyd of iron 11-05, lime 7-00, alumina 6-80, oxyds of nickel and 
 chrome, traces, water 7*60 = 100-38. From a comparison of this with the 
 previous analyses, it would appear that the paste of the rock is a substance 
 allied to chlorite or to pyrosclerite in composition. 
 
 This mineral evidently differs from pyroxenic diallage, both in the great 
 excess of bases, and the large amount of water which it contains. 
 
 TALC. 
 
 This species is comparatively rare among the Laurentian rocks, where Taic. 
 it seems to be generally replaced by pyrallolite. A greyish steatite or 
 soapstone is however met with in this series, in the township of Elzivir. 
 It gave to dilute nitric acid about twenty-five per cent, of carbonates of 
 lime and magnesia, and left a soft flaky talc. This was freed by washing, 
 from four or five per cent, of magnetic iron, and, after drying at 212 F., 
 yielded to analysis, silica 59-10, magnesia 29-05, protoxyd of iron, with 
 traces of manganese, 3-51, volatile 5-56 = 97-32. Unlike the talcs of the 
 Silurian series, this mineral contained no traces of nickel. 
 
 Among the altered Silurian strata, talc is abundant, sometimes in crys- steatite, 
 talline foliated masses, but it more frequently forms beds of a compact or 
 schistose variety of steatite or soapstone, interstratified with serpentine, 
 
470 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 magnesite, or clay slate, and often enclosing actinolite, or bitter-spar. 
 A greenish-white translucent steatite from Potton, gave by analysis, silica 
 59-50, magnesia 29-15, protoxyd of iron 4-50, alumina 0-40, oxyd of 
 nickel, traces, volatile 4-40 = 97-95. A silvery-white flaky talc-schist, 
 also from Potton, afforded silica 51-50, magnesia 22-36, protoxyd of iron 
 7*38, lime 11-25, alumina 3-50, oxyd of nickel, traces, volatile 3-60 = 
 99*59. The talc is here apparently mixed with hornblende, or with some 
 other anhydrous silicate containing lime. 
 
 PYRALLOLITE OR RENSSELAERITE. 
 
 Under the name of rensselaerite, Dr. Emmons of New York described, 
 in 1837, a steatitic mineral, which forms beds or large masses among 
 the Laurentian rocks in the northern part of that State. It is gen- 
 erally massive or granular, but sometimes appears in regular crystals, 
 which have the external form and the cleavage of pyroxene. Dr. Beck, 
 who submitted to analysis an impure specimen of it from Canton, New 
 York, declared it to be a mixture of steatite with pyroxene. He found it 
 to contain silica 59-75, magnesia 32-90, lime 1-00, peroxyd of iron 3-04, 
 water 2-85. This composition agrees closely with that assigned by Beudant 
 to the so-called steatitic pyroxene of Sahla in Sweden, and with the pyrallo- 
 lite of Nordenskiold, from Pargas in Finland, where it occurs in crystal- 
 line limestone with apatite, sphene, and green pyroxene ; being, according 
 to Nordenskiold, often incrusted with the latter mineral. Dana, in his 
 Mineralogy, has pointed out the resemblance between the two minerals 
 pyrallolite and rensselaerite, which are probably identical, so that the older 
 name of pyrallolite should take precedence. (See Schwieger's Journal, 
 xxxi, 386 ; and for rensselaerite, Reports by Emmons and Beck on the 
 Geology and Mineralogy of New York, passim.^) 
 
 A bed of pyrallolite occurs in crystalline limestone at Grenville. It is 
 granular, and made up of strongly coherent cleavable grains, but druses of 
 small crystals are occasionally met with in the mass. Its hardness is from 
 2-5 to 3-0. The density of the mineral from Grenville, is 2-757 ; that of 
 a coarsely columnar radiating variety from Charleston Lake, 2-644. A 
 specimen from an unknown locality, in the vicinity of Brockville, exhibits 
 cleavage surfaces one fourth of an inch broad. The color of the mineral is 
 generally greenish-white or sea-green, sometimes pearl-white. Very dark 
 colored, nearly black varieties are also described by Dr. Emmons. It is 
 translucent, with a vitreous lustre on the cleavage surfaces, elsewhere 
 waxy. The mineral is sectile and unctuous like steatite. Impure massive 
 varieties of it sometimes occur, as in Rawdon ; where a rock, which is 
 associated with crystalline limestones, and has the aspect of pyrallolite, 
 holds scales of silvery mica, and of graphite. A bed of pyrallolite also 
 occurs in Ramsay. Unlike talc, the pyrallolite from Grenville is attacked 
 
CHAP. XVII.] MINERAL SPECIES. 
 
 and partially decomposed by boiling in concentrated sulphuric acid. A 
 portion thus treated, gave up 3-89 per cent, of magnesia. It loses no 
 water at 300 F., and only 3*80 per cent, by a long continued red heat; 
 but when heated to whiteness, the loss is greater. Neither lime, manga- 
 nese, nor nickel, were detected in the specimens analyzed, which were 
 three in number. I is the granular variety from Grrenville, carefully freed 
 from adhering calcite ; II, a columnar specimen from Charleston Lake ; 
 and III, crystals from Canton, New York, obtained from Dr. Emmons. 
 
 I. 
 
 Silica; 61-60 
 
 Magnesia, 31-06 
 
 Protoxyd of iron, 1-53 
 
 Water, 5-60 
 
 99-79 100-31 100-05 
 
 The specimen analyzed by Beck was doubtless impure, as was probably 
 that of Nordenskiold. The mineral seems to be identical with the steatitic 
 substance from China, which has been mistaken for agalmatolite, and 
 like this is wrought into small vases and other objects of use and orna- 
 ment. It is evidently, as maintained by Dr. Emmons, a distinct species ; 
 and as a rock, it replaces, for the most part, in the Laurentian system, the 
 talcs, which are frequent in other series of metamorphic rocks. It 
 differs but little from talc in composition, except in a somewhat greater 
 amount of water; and the two specimens may perhaps be regarded as 
 dimorphous conditions of the same silicate of magnesia. 
 
 SERPENTINE . 
 
 This species, either alone or with various admixtures, is found in large 
 beds, both in the Laurentian and Silurian series, and constitutes the rocks 
 to be described in a subsequent chapter by the name of ophiolites. 
 
 Among the massive and nearly pure Laurentian serpentines, may be 
 mentioned those of Grenville and of Burgess, which are generally pale- serpentines 
 yellowish, or greyish-green; unless, as in the latter locality, they are 
 penetrated in parts by red peroxyd of iron. They also occur in this 
 series intermingled with carbonates of lime and magnesia, and disseminated 
 in grains, or forming veins, both in limestones and dolomites. The serpen- 
 tines of the Laurentian series have a lower specific gravity, and contain 
 less oxyd of iron and more water than ordinary serpentines. The analyses 
 of some of them are subjoined. I is the retinalite of Dr. Thompson, from 
 Grenville, where it is imbedded in a white limestone. Its color varies 
 from honey-yellow to oil-green, and its density is 2-47-2-52. II is a 
 similar serpentine, of a pale wax-yellow, from the Calumet Island ; density 
 2-36 - 2-38. Ill, grams of honey-yellow serpentine, separated by dilute 
 
472 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 nitric acid from a white lamellar dolomite from Grenville. IV is the 
 reddish-brown serpentine-rock or ophiolite of Burgess, from which a portion 
 of carbonates of lime and magnesia was first removed by acetic acid : 
 
 I. n. in. iv. 
 
 Silica, 39-34 41-20 44-10 39-80 
 
 Magnesia,. 43-02 43-52 40-05 38-40 
 
 Peroxyd ofiron, 1-80 -80 1-15 7-92 
 
 Water, 15-09 15-40 14-70 13-80 
 
 99-25 100-92 100-00 100-00 
 
 A pale greenish-grey opaque and earthy serpentine, or pipe-stone, from 
 Calumet Island, contains a mixture of argillaceous matter, and gave by 
 analysis, silica 37-50, magnesia 37-58, alumina and a little oxyd of iron 
 9-00, water 15-00 = 99-08. 
 
 Huroman No serpentine has yet been observed in the rocks of the Huronian 
 ine> series in Canada; but Mr. Whitney has described an ophiolite belonging to 
 them, which forms the headland of Presqu'ile, near Marquette, in northern 
 Michigan, and may be noticed in this connection. It is blackish-green, and 
 contains an admixture of octahedral crystals of magnetic iron, besides from 
 two to six per cent, of an insoluble silicate, probably hornblende. The 
 remaining portion is a serpentine, containing a large proportion of protoxyd 
 of iron. (American Journal of Science [2], xxviii, 18.) 
 
 Silurian The serpentines of the altered Silurian rocks in Eastern Canada, often 
 
 s ' form vast masses, almost without admixture. At other times, they enclose 
 diallage, actinolite, garnet, and chromic iron, or are intermingled with 
 carbonate of lime, with dolomite, and sometimes with ferruginous magne- 
 site ; forming varieties of ophiolite rock, into which talc sometimes enters. 
 The almost constant presence of small portions of oxyds of chrome and 
 nickel, is to be remarked in the analyses, not only of these serpentines, 
 but of the other magnesian rocks of the region ; while these two metals 
 appear to be altogether wanting in similar rocks of the Laurentian series. 
 The analyses of a few specimens of these serpentines are subjoined. I, 
 a finely granular olive-green massive serpentine, from Orford, enclosing 
 grains of magnetic and chromic iron-ores ; density 2-597. II, a fragment 
 of blackish-green serpentine, from a conglomerate ophiolite in Orford. 
 Ill, a massive greenish-white serpentine, near to a bed of ehromic iron in 
 Ham; density, 2-546. IV, a fibrous serpentine (picrolite), from Bolton ; 
 density 2-607. 
 
 I. n. in. iv. 
 
 Silica, 40-30 42-90 43-40 43-70 
 
 Magnesia, 39-07 36-28 40-00 40-68 . 
 
 Protoxyd of iron, 7-02 7-47 3-60 3-51 
 
 Oxyd of nickel, -26 -15 .... undet. 
 
 " chrome, traces -25 .... '" 
 
 Water, 13-35 13-14 13-00 12-45 
 
 100-00 100-19 100-00 100-34 
 
CHAP. XVII.] MINERAL SPECIES. 473 
 
 Foliated and fibrous varieties of serpentine are common in veins in the 
 ophiolites of the Silurian series ; and they constitute the varieties which 
 have heen described under the names of baltimorite, marmolite, picrolite, 
 and chrysotile. The latter occurs in silky flexible fibres, whose direction 
 is transverse to the walls of the vein ; and it constitutes much of the so- 
 called asbestus or amianthus of serpentine rocks. The true asbestus is, 
 however, a fibrous tremolite or hornblende. 
 
 A yellowish-white compact earthy mineral is found filling fissures in the 
 massive pyrallolite of Grenville. It is very soft and sectile, polishes 
 under the nail, acquiring a waxy lustre, and adheres strongly to the 
 tongue. Some portions of the mass contain disseminated scales of silvery 
 mica. The mineral in powder is decomposed, like serpentine, by boiling 
 sulphuric acid, and gave, silica 46 '66, magnesia (by difference) 38-05, 
 protoxyd of iron 1 33, volatile 13 96 = 100 00. The physical charac- 
 ters of this substance separate it from- serpentine, and ally it to meer- 
 schaum and aphrodite, which latter mineral it resembles in composition. 
 
 ALUMINOUS SILICATES. 
 
 Having described the principal silicates of protoxyds hitherto observed Aluminous 
 hi Canada, next in order may be noticed those minerals which contain s 
 alumina, and are for the most part double silicates of this base, and a 
 protoxyd, such as potash, soda, lime, magnesia or protoxyd of iron, either 
 with or without water. Of the simple aluminous silicates, only andalusite 
 and pholerite have been met with in the province. Kyanite is found in 
 the adjacent state of Vermont and farther southward, and might be 
 expected in south-eastern Canada, but has not yet been detected. The 
 same thing may be said of pyrophyllite, which occurs in North Carolina, 
 in rocks supposed to be of the same age with those of Vermont and the 
 Eastern Townships, both crystallized with quartz, and massive, giving rise 
 to a kind of aluminous steatite. 
 
 The minerals of the feldspar group, including scapolite, orthoclase, and 
 the triclinic feldspars, will now be described, and will be followed by the 
 zeolites,, agalmatolite, glauconite, chlorite, and some related alumino-mag- 
 nesian silicates. To these will succeed beryl, tourmaline, the micas, and 
 the denser double silicates, garnet, epidote, chloritoid, and staurotide, 
 together with andalusite. After these will be noticed zircon, spinel, 
 corundum, and quartz. 
 
 SCAPOLITE. 
 
 This species is abundant in the Laurentian rocks of northern New York, 
 where it is generally associated with pyroxene and sphene. Large crys- 
 tals of scapolite are met with in a similar association hi Hunterstown. It 
 
474 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 scapoiite. has also been observed in Grenville ; and a lilac-colored scapolite in irreg- 
 ularly aggregated crystals, forms masses in limestone at Calumet Island. 
 An interesting variety was found associated with black mica in a boulder, 
 near Perth. It has a hardness of 5-5, and a density of 2-640-2-667, is 
 greenish-grey in color, very tough and subtranslucent, with a waxy lustre, 
 pearly upon the cleavage surfaces, which are very distinct in two direc- 
 tions at right angles. Its analysis gave silica 46*30, alumina 26-20, lime 
 12-88, magnesia 3-63, protoxyd of iron 0-60, potash 2-88, soda 4-30, 
 volatile 2-80 = 99-59. This mineral is remarkable for the considerable 
 amounts of potash and magnesia which it contains. 
 
 OKTHOCLASE. 
 
 orthociase. This species of feldspar, which enters largely into the composition of 
 granite, syenite, gneiss, trachyte, and many porphyries, is very abundant 
 among the rocks of the Laurentian system. A reddish colored variety is 
 the predominant mineral in the coarse-grained gneiss, which is character- 
 istic of this series of rocks. A beautiful white porphyroid gneiss from the 
 Kivi^re Rouge, in Argenteuil, consists of a fine-grained base of orthoclase, 
 with a little quartz, containing besides red garnets, and small quantities of 
 silvery-mica, large cleavable masses of white semi-transparent orthociase, 
 having a density of 2-56. From its analysis, I, given below, it will be seen 
 to contain potash, with but little soda : the same is true of the gran- 
 ular base of the rock, II. A fragment of reddish feldspathic gneiss from 
 Grenville, in which orthociase was the predominant mineral, contained 
 however a larger proportion of soda, as is shown by its analysis, III. 
 t 
 
 I. n. ill. 
 
 Silica, 65-75 70-10 69-00 
 
 Alumina, 19-40 16-40 17-90 
 
 Peroxyd of iron, .... 
 
 Lime, 0-45 1-42 2*80 
 
 Potash, 13-60 10-96 3-86 
 
 Soda, , 0-69 0-59 3-70 
 
 Volatile, 0-25 0-40 TOO 
 
 100-14 100-07 98-26 
 
 Eertiute. The perthite of Dr. Thompson is a reddish orthociase, which, with 
 white quartz, forms a coarse granite in Burgess. In this rock, cleavage sur- 
 faces, several inches broad, are sometimes met with, which are barred with 
 lighter and darker bands. These are flesh-red and reddish-brown in color ; 
 and they exhibit, in certain lights, golden reflections like aventurine, which 
 are very beautiful in some polished specimens. The density of this feldspar 
 is 2-57-2-58. One of two concordant analyses gave silica 66-44, alumina 
 18-35, peroxyd of iron 1-00, lime 0-67, magnesia 0-24, potash 6-37, soda 
 
CHAP. XVII.J MINERAL SPECIES. 475 
 
 5-56, volatile 040 = 99-03. A second determination gave silica 66-50, 
 alumina and peroxyd of iron 19-25, lime 0-56, and potash 6-18. 
 
 Dr. Bigsby has noticed, under the name of aventurine, a largely crys- Aventurine 
 tallized flesh-red feldspar, which, like the perthite, shines with golden felds P ar - 
 points, and, according to him, forms part of a great granitic vein traver- 
 sing gneiss, on the north-east shore of Lake Huron, twenty miles east of 
 the French River. 
 
 Masses of a rock, brought from the Labrador coast, consist of a pale 
 reddish-brown cleavable feldspar, mixed only with a small quantity of dark 
 green hornblende. This feldspar, which is seemingly orthoclase, sometimes 
 offers cleavages half an inch broad, which exhibit golden-bronze reflections 
 of great beauty, resembling those of some varieties of labradorite. A fine 
 green orthoclase in a granitic vein has also been brought from the same region. 
 
 Associated with the Laurentian limestones there are frequently found 
 beds of a coarse-grained rock, made up of white feldspar and dark green 
 pyroxene, with brown sphene, and occasionally with quartz. This peculiar 
 rock has been observed at Lachute, where it contains brown tourmaline, 
 plumbago, and magnetic pyrites ; at the Calumet Falls ; and in Grenville, 
 Elmsley, and Burgess. The feldspar has generally the cleavages and other 
 characters of orthoclase. A specimen, probably from Chatham, with brown 
 sphene and quartz, had a specific gravity of 2-55-2-57, and gave by 
 analysis, silica 65-20, alumina 18-30, lime 0-34. A partial determination 
 of the alkalies, gave potash 8-57, soda 1*75 ; showing it to be a nearly pure 
 potash orthoclase. 
 
 The feldspar which occurs with pyroxene in the Laurentian rocks of 
 Hammond, St. Lawrence County, New York, and closely resembles those 
 just described, was by Breithaupt distinguished by the name of loxoclase ; 
 but according to Smith and Brush it has the cleavage and density of 
 orthoclase, with which it agrees in composition. It is however remarkable 
 for the large amount of soda which it contains. A pure crystal of this 
 feldspar gave to these chemists, soda 7-81, potash 4-35, lime 1*09 ; and 
 another specimen, soda 7-98, potash 2.36, and lime 2-36. (American 
 Journal of Science [2], xvi, 43.) 
 
 A white feldspar, which is found with sphene and pyroxene, at Wills- 
 borough, New York, in a rock similar to that of Chatham, is triclinic, 
 beautifully striated, and has the aspect of oligoclase. The mineral associ- 
 ations of these various feldspars are similar to those of the scapolite men- 
 tioned above. 
 
 The orthoclase from trachytic rocks often contains a large amount of 
 soda. The following are analyses of feldspars from the trachytes of of trachytes, 
 Canada. IV, orthoclase, from the porphyritic trachyte of Chambly ; V, 
 orthoclase of the granitoid trachyte of Brome Mountain, density 2-575 ; 
 VI, orthoclase from Shefford Mountain, density 2-561 ; VII, feldspar of 
 compact white trachyte from Mount Royal; VIII, feldspathic residue 
 
476 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 from a phonolite from Lachine, which contained a large proportion of 
 natrolite, and of carbonates of lime, magnesia, and iron. 
 
 Silica, 
 
 IV. 
 66-15 
 
 V. 
 
 65-70 
 
 VI. 
 65-15 
 
 VII. 
 
 63-25 
 
 VIII. 
 59-70 
 
 Alumina ...... 
 
 19-75 
 
 20-80 
 
 20-55 
 
 22-12 
 
 23-25 
 
 
 -95 
 
 84 
 
 73 
 
 56 
 
 99 
 
 Potash, 
 
 7-53 
 
 6-43 
 
 6-39 
 
 5-92 
 
 9-16 
 
 Soda, . . 
 
 5-19 
 
 6-52 
 
 6-67 
 
 6'29 
 
 2-97 
 
 Volatile, 
 
 -55 
 
 50 
 
 50 
 
 93 
 
 2-23 
 
 
 
 
 
 
 
 100-12 100-79 99-99 99*07 98-30 
 
 orthociase of ^- r ^' ^' Whitney has called attention to the frequent occurrence of ortho- 
 mineral veins, clase in the mineral veins of Lake Superior, where it is associated with 
 Lake Superior, native copper, epidote, calcite, natrolite, analcime, quartz, and saponite. It is 
 sometimes found incrusting the latter two species, and at others is covered 
 by calcite or natrolite ; the minerals, according to Mr. Whitney, being asso- 
 ciated in such a manner as to show the contemporaneous crystallization of 
 the copper, natrolite, calcite, and orthociase. The latter species, from its 
 associations and peculiar aspect, was at first mistaken for stilbite. It forms 
 crystalline lamellar masses, small geodes, or groups of implanted crystals, 
 which are pale or bright red in color. The crystals are seldom more than 
 one tenth of an inch in length, but are sometimes distinct enough for meas- 
 urement. This orthociase gave to Mr. Whitney's analysis, silica 65-45, 
 alumina 18-26, potash 15-21, soda 0-65, oxyd of iron 0-57, manganese, a 
 trace, = 100-14. (American Journal of Science [2], xxviii, 16.) 
 
 A particular interest is attached to the existence of orthociase in veins, 
 associated with minerals which are evidently of aqueous origin, for the 
 reason that hitherto there were but few examples of the occurrence of 
 feldspar under conditions which could leave no doubt of its aqueous origin. 
 Eastern Other instances of a similar kind are however met with in veins in the slates 
 
 of the Eastern Townships, where a flesh-red orthociase occurs so intermin- 
 gled with white quartz and chlorite, as to show the contemporaneous form- 
 ation of the three species. The orthociase generally predominates, often 
 reposing upon or surrounded by chlorite ; and at other times it is imbedded 
 in quartz, which covers the latter. Drusy cavities are also lined with small 
 crystals of the feldspar, and have been subsequently filled with a cleavable 
 bitter-spar, containing more or less of the carbonates of iron and manganese, 
 and sometimes associated with specular iron, rutile, and sulphurets of cop- 
 per. These veins are found cutting both the nacreous argillaceous slates, 
 and the chloritic slates of the Eastern Townships, and are well seen in 
 Leeds, Inverness, and Sutton. A study of them will show a transition from 
 veins containing quartz and bitter-spar, with a little chlorite or talc, through 
 others in which feldspar gradually predominates, until we arrive at veins 
 made up of orthociase and quartz, sometimes including mica, and having 
 
CHAP. XVII.] MINERAL SPECIES, 477 
 
 the characters of a coarse-grained granite ; the occasional presence of sul- 
 phurets of copper and specular iron characterizing all of them alike. It 
 is probable that these, and indeed a great proportion of quartzo-feldspathic 
 veins are of aqueous origin, and have been deposited from solutions in Granitic veins, 
 or fissures in the strata, precisely like metalliferous lodes. This remark 
 applies especially to those granitic veins which include minerals con- 
 taining the rarer elements. Among these are boron, phosphorus, fluorine, 
 lithium, rubidium, glucinum, zirconium, cerium, tin, and columbium, 
 which characterize the mineral species apatite, tourmaline, lepidolite, 
 spodumene, beryl, zircon, allanite, cassiterite, columbite, and many others. 
 
 A coarse-grained granite, which is probably intrusive, occurs in the 
 township of Bathurst, the feldspar of which was described by Dr. Thomp- 
 son under the name of peristerite, in allusion to its bluish opalescence, but 
 is found to be albite. In some portions of the rock the quartz is dissemi- 
 nated through the feldspar, so as to give rise to what is called a graphic 
 granite, but large cleavable masses are free from this admixture, and exhibit 
 the usual striation of the crystals of the triclinic feldspars. The color is 
 white, passing into pearl-grey and reddish, and the mineral shows an opales- 
 cence, in which blue predominates, mingled however with pale green and 
 yellow. Its hardness is 6-0, and its density 2-625. Analysis gave silica 
 66-80, alumina 21-80, potash 0-58, soda 7-00, lime 2-52, magnesia 0-20, 
 peroxyd of iron 0-30, volatile 0-60 = 99*80. Another specimen yielded 
 silica 67-25, lime 2-03. 
 
 A similar granite, consisting of large cleavable masses of white albite, 
 with quartz and mica, is found at the lake of Three Mountains, on the 
 Riviere Rouge ; and some of the garnet-bearing gneiss of that vicinity is 
 also albitic. Mingled with the opalescent albite of Burgess are found 
 portions of pale reddish orthoclase, an association not uncommon in granites. 
 A white feldspar, which is sometimes found with flesh-red orthoclase in 
 boulders of granitoid Laurentian gneiss, is probably albite or oligoclase. 
 
 OLIGOCLASE. 
 
 A feldspar having the composition of oligoclase forms, with black horn- 
 blende, the intrusive diorite of Mount Johnson. It often occurs in crys- 
 tals half an inch in diameter, which weather to an opaque white. The 
 color of this feldspar is white, rarely greenish or greyish. Its lustre is 
 vitreous, inclining to pearly. The specific gravity of a fragment was 2-631, 
 of the mineral in powder 2-659. Its analysis gave silica 62-05, alumina 
 22-60, peroxyd of iron 0-75, lime 3-96, potash 1-80, soda 7-95, volatile 
 0-80 = 99-91. Another specimen yielded silica 62-10, and lime 3-69. 
 
478 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVII. 
 
 ANDESINE AND LABBADORITE. 
 
 Andesine. 
 
 Labradorite. 
 
 The triclinic feldspars, containing lime and soda, which make up the 
 great anorthosite formation of the Laurentian series, offer considerable 
 variations in their composition. Some of them have that assigned to ande- 
 sine, others that of labradorite, or are intermediate between the two, while 
 others are near to anorthite. The following analyses will give some notion 
 of the variable composition of these feldspars. I and II are of a reddish 
 cleavable feldspar, which occurs in large striated cleavable masses, with 
 hypersthene and ilmenite, at Chateau Richer, and has a density of 2-66- 
 2*67. Ill is the greenish granular base in which the preceding is im- 
 bedded. It has a specific gravity of 2-67, and was treated, previous to 
 analysis, with acetic acid, which removed a few thousandths of carbonate of 
 lime. IV, a pale lavender-blue vitreous, semi-transparent feldspar in 
 large cleavable striated masses, the surfaces of which are often curved. 
 It occurs in a boulder at Chateau Richer, and has a density of 2.68- 
 2-69. V, a specimen similar to the last, from a larger boulder, in the adja- 
 cent parish of St. Joachim. These two are imbedded in a reddish granu- 
 lar base, with grains of ilmenite, and a little brown mica. VI, a similar 
 feldspar from Lachute, where it occurs in large finely striated cleavable 
 masses, in a greenish granular base. It is semi-transparent, and of a 
 lavender-blue, passing into sapphire-blue. This feldspar has a density of 
 
 2-687. 
 
 I. II. 
 
 59-80 
 25-89 
 
 0-60 
 
 7-78 
 
 0-11 
 
 1-00 
 
 5-14 
 
 Silica, 59-55 
 
 Alumina, 25-62 
 
 Peroxyd of iron, 0-75 
 
 Lime, 7-73 
 
 Magnesia, traces 
 
 Potash, 0-96 
 
 Soda, 5-09 
 
 Volatile, 0-45 
 
 III. 
 
 IV. 
 
 V. 
 
 VI. 
 
 58-50 
 
 57-20 
 
 57-55 
 
 58-15 
 
 25-80 
 1-00 
 
 26-40 > 
 0-40 > 
 
 27-10 
 
 ( 26-09 
 i 0-50 
 
 8-06 
 
 8-34 
 
 8-73 
 
 7-78 
 
 0-20 
 
 .... 
 
 .... 
 
 0-16 
 
 1-16 
 
 0-84 
 
 0-79 
 
 1-21 
 
 5-45 
 
 5-83 
 
 5-38 
 
 5-55 
 
 0-40 
 
 0-20 
 
 0-20 
 
 0-45 
 
 100-15 
 
 99-82 100-57 99-66 . 99'75 99-89 
 
 To these may be added the following : VII, a bluish-white granular 
 homogeneous translucent rock from Rawdon, with a density of 2-69. VIII, 
 a similar rock from Chateau Richer, pale bluish or greenish grey, with 
 red spots. The lustre on the cleavage surfaces of the grains is vitreous, 
 but elsewhere waxy. The rock contains small scattered flakes of black 
 mica, and has a density of 2-68. IX, a bluish opalescent cleavable feld- 
 spar from Morin, with a density of 2- 684 -2' 695. X, a lavender-blue 
 cleavable feldspar, with a grey opalescence, from a boulder in Drummond. 
 Canada West, and having a density of 2-697. XI, a pale sea-green 
 translucent cleavable feldspar, with a density of 2-695-2-703, from a 
 granular mass of a similar character, forming a boulder at Hunterstown. 
 XII, a greenish-white granular variety of anorthosite rock, from a boulder 
 
CHAP. XVII.] 
 
 MINERAL SPECIES, 
 
 479 
 
 near Ottawa, having a density of 2-73. 
 upon which Dr. Thompson founded the 
 
 VII. 
 Silica, .............. 54-45 
 
 Alumina, ............ 28-05 
 
 Peroxyd of iron, ..... 0-45 
 
 Lime, .............. 9-68 
 
 Magnesia, ............... 
 
 Potash, ............. 1-06 
 
 Soda, ............... 6-25 
 
 Volatile, ............ 0-55 
 
 This is a portion of the specimen 
 species named by him bytownite. 
 
 VIII. 
 
 IX. 
 
 X. 
 
 XI. 
 
 XII. 
 
 55-80 
 
 54-20 
 
 54-70 
 
 49-10 
 
 47-40 
 
 26-90 
 
 29-10 
 
 29-80 
 
 26-80 
 
 30-45 
 
 1-53 
 
 1-10 
 
 0-36 
 
 0-80 
 
 0-80 
 
 9-01 
 
 11-25 
 
 11-42 
 
 14-67 
 
 14-24 
 
 0-27 
 
 0-15 
 
 traces 
 
 traces 
 
 0-87 
 
 0-86 
 
 undet. 
 
 0-23 
 
 undet. 
 
 0-38 
 
 4-77 
 
 it 
 
 2-44 
 
 
 
 2-82 
 
 0-45 
 
 0-40 
 
 0-40 
 
 1-30 
 
 2-00 
 
 99-35 
 
 98-96 
 
 100-49 99-59 
 
 The analyses I and II have the composition ascribed to andesine, 
 while VII, VIII, IX, and X have that of labradorite. The beautifully 
 pure and crystalline feldspars IV, V, and VI have a composition 
 intermediate between these two, while XI, and the bytownite, XII, 
 approach to anorthite. 
 
 The bytownite gives by analysis nearly the same results as the feldspar 
 from the intrusive diorite of Yamaska Mountain. This rock is coarsely 
 crystalline, and made up of black hornblende, with a little yellow sphene, 
 and a white triclinic feldspar, the cleavage surfaces of which are sometimes 
 half an inch broad, and beautifully striated. The density of the powdered 
 feldspar was 2-756 - 2-763. Its analysis gave silica 46-90, alumina 31-10, 
 peroxyd of iron 1-35, lime 16-07, magnesia 0-65, potash 0-58, soda 1-77, 
 volatile 1-00 = 99-42. Another specimen gave silica 47*00, alumina and 
 iron oxyd 32-65, lime 15*90. Both of these feldspars may be looked 
 upon as impure anorthite. 
 
 The following also are analyses of feldspars from intrusive rocks. XIII, Feldspar* of 
 grams separated by crushing and washing from a granitoid micaceous 
 trachyte of Yamaska Mountain, and having a density of 2-563. XIV, 
 selected grains from another portion of the same rock. XV, cleavable 
 grains of white vitreous feldspar, separated by washing from the micaceous 
 diorite of Beloeil, and still holding a little mica. XVI, grains of a yellow- 
 ish vitreous feldspar from the peridotic dolerite of Montarville, and having 
 a density of 2-73-2*74. XVII, feldspar of a similar peridotic dolerite 
 from Mount Royal, with a small admixture of augite. 
 
 XIII. 
 
 Silica, 61-10 
 
 Alumina, 20-10 
 
 Peroxyd of iron, 2-90 
 
 Lime, 3-65 
 
 Magnesia, 0-79 
 
 Potash, 3-54 
 
 Soda, 5-93 
 
 Volatile, 0-40 
 
 98-41 
 
 iutrusivs rocks. 
 
 XIV. 
 
 XV. 
 
 XVI.' 
 
 XVII. 
 
 58-60 
 
 58-30 
 
 53-10 
 
 53-60 
 
 21-60 > 
 2-88 > 
 
 24-72 
 
 C 26-80 
 < 1-35 
 
 25-40 
 4-60 
 
 5-40 
 
 5-42 
 
 11-48 
 
 3-62 
 
 1-84 
 
 0-91 
 
 0-72 
 
 0-86 
 
 3-08 
 
 2-74 
 
 9-71 
 
 undet. 
 
 5-51 
 
 6-73 
 
 4-24 
 
 
 
 0-80 
 
 0-50 
 
 0-60 
 
 0-80 
 
 99-71 
 
 99-32 
 
 99-00 
 
480 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVII. 
 
 Constitution 
 of feldspars. 
 
 Opalescent 
 feldspars. 
 
 Nepheline 
 
 Sodalite. 
 
 The analysis XVI gives nearly the composition of labradorite, while 
 XIII, XIV, and XV are unlike any recognized variety. The vari- 
 ations in the composition of feldspathic minerals are well known to he very 
 great, and seem to countenance the view that the homoeomorphous species 
 albite, anorthite, and orthoclase, may crystallize together in variable and 
 indefinite proportions. The so-called species oligoclase, andesine, and 
 labradorite are connected by feldspars intermediate in composition, of 
 which we have examples in IV, V, and VI. All of these triclinic feld- 
 spars may be regarded as admixtures of albite and anorthite ; while the 
 soda-bearing feldspars of the trachytes, and th6 feldspars like perthite, and 
 like XIII and XIV, would appear to be mixtures of orthoclase with 
 albite, or some other triclinic feldspar. 
 
 It is worthy of note that in all the triclinic feldspars whose analyses are 
 given above, the specific gravity is greater as the silica and alkalies dimi- 
 nish, and the alumina and lime increase, in amount. All of the triclinic 
 feldspars have thus a common atomic volume, in which they agree with 
 the lithia-feldspar, petalite. (Am. Jour, of Science [2], xviii, 270.) 
 
 The most important localities of these feldspars have already been men- 
 tioned in describing their different varieties, and in mentioning the distribu- 
 tion of the anorthosite rocks in Chapter III. The brilliant play of colors 
 which makes the labradorite prized as an ornamental stone, is by no means 
 a constant character. It has not been observed in the beautiful varieties of 
 these feldspars from Chateau Richer ; but it is frequent in large cleavable 
 masses, imbedded in the anorthosites of Morin and Mille-Iles, and also in 
 boulders scattered along the valley of the Ottawa, and to the southward of 
 it. The most western exposure of these feldspars known, is that noticed 
 by Dr. Bigsby, who has described a breadth of five miles, occupied by 
 anorthosite on the coast of Lake Huron, about sixty miles west from 
 Penetanguishene, and ninety miles east from the French River. Here it 
 forms the main-land and numerous small islands, among which are found 
 coarse-grained varieties of bluish and grey feldspar, with purple, green, and 
 flame-colored opalescence. These colored reflections are not confined to 
 those triclinic feldspars which have the composition of labradorite, but are 
 seen in some which approach to andesine in composition, and even in albite, 
 the white variety called peristerite, which is described above, being 
 beautifully opalescent. 
 
 NEPHELINE AND 8ODALITE. 
 
 Crystals of white nepheline, with a fine blue variety of sodalite in small 
 grains, have been found sparingly in the granitoid trachyte of Brome. 
 Grams of orange-red nepheline or elaeolite are abundant, with black 
 hornblende, in a white feldspathic rock, which is found in boulders on Pic 
 Island, in Lake Superior. 
 
CHAP. XVII.] MINERAL SPECIES. 481 
 
 PETALITE AND SPODUMENE. 
 
 Petalite is here mentioned among the minerals of Canada, upon the Petaiite. 
 authority of Dr. Bigsby, according to whom this mineral was found with 
 tremolite, in a large boulder on the lake shore, at Toronto. Its only known 
 locality in situ, on this continent, is at Bolton, in Massachusetts, where it 
 occurs with scapolite in crystalline limestone. Spodumene, which is found spodumene. 
 in several localities in New England, in granitic veins with tourmaline and 
 beryl, has been observed, in a single instance, in a small rolled mass of 
 granite, near Perth. 
 
 ZEOLITES. 
 
 The true zeolites, which are hydrous silicates of alumina with a silicate zeolites, 
 of a protoxyd, may be mentioned in this connection. Several minerals 
 of this class have been observed in the amygdaloidal traps of Lake Supe- 
 rior, and more sparingly about Montreal. Among these, a fibrous zeolite, 
 described by Prof. Chapman as thomsonite, is found, according to Dr. 
 Bigsby, of a red color at Gargantua, and both red and green at Point 
 Maimainse, where it is associated with calcite. Prehnite, laumontite, and 
 analcime are also common among the minerals of the amygdaloid of the 
 north shore of Lake Superior, generally associated with native copper, and 
 often forming its gangue. Analcime abounds with the native copper of 
 Michipicoten Island. 
 
 A radiated zeolitic mineral, probably natrolite, occurs in small quantities N 
 in druses in the traps near Montreal, associated wijbh heulandite, chabazite, 
 and analcime. The latter two minerals have been observed with quartz 
 and calcite in druses in a porphyritic trachyte on the Chambly canal. A 
 zeolitic mineral forms an integral part of many of the trachytic rocks 
 about Montreal, which, through this admixture, pass into phonolites, to 
 be described in their proper place. The zeolite in these, which is inter- 
 mingled with orthoclase and with carbonates, readily gelatinizes with acids, 
 and has apparently the composition of natrolite. It sometimes forms thirty 
 or forty per cent, of the rock. 
 
 Prehnite is one of the most common vein-stones of the native copper on Prehnite. 
 Lake Superior ; and in the mines of the southern shore, it has been found in 
 radiating masses, imbedded in the blocks of copper. A mineral to which cniorastroiito. 
 the name of chlorastrolite has been given, is found imbedded hi the amyg- 
 daloid of Isle Royale, and in worn pebbles along the shore. As it is 
 somewhat prized as an ornamental stone, it may be mentioned in this con- 
 nection, although it has not yet been found on the northern shore of the 
 lake. It forms small masses of a radiated or stellated structure, and is 
 opaque, with a rich bluish-green color, and a pearly, somewhat chatoyant 
 
 FF 
 
482 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 lustre. It had been separated from prehnite, which it closely resembles in 
 composition, on account of its somewhat higher specific gravity, and also 
 because it contains more oxyd of iron and more water than prehnite. 
 According to Prof. Chapman, however, its specific gravity varies from 
 2-98 to 3-20, from the presence of more or less magnetic oxyd of iron, 
 which often forms the nucleus of the fibrous masses of chlorastrolite. 
 The amount of water he also found to vary, in different specimens, from 
 4-11 and 4-18 to 5*51 per cent. 
 
 Apophyiiite. Apophyllite, although not a proper zeolite, may be here mentioned as 
 occurring in foliated masses or plates, often of a red color, associated with 
 calcite in Prince's vein on Spar Island. The related species, pectolite, 
 has been observed on Isle Roy ale. Here also finely crystallized datholite 
 has been found, and a white massive porcelain-like variety of the same 
 mineral is met with at some of the mines on the southern shore. 
 
 AGALMATOLITE OB GIESECKITE. 
 
 Agalmatolite. Under this head it is proposed to notice a peculiar mineral which, 
 under different forms, occurs both in the Laurentian and Silurian series, 
 and sometimes forms rock-masses among them. The name of agalmatolite, 
 or figure-stone, was originally given to a soft unctuous mineral, which is 
 carved by the Chinese into ornaments. The researches of Scheerer and 
 of Brush have however shown that these figure-stones are not all alike, but 
 may be referred to three species, very distinct in chemical composition, 
 though closely resembling each other in specific gravity, hardness, and 
 general aspect. Of these, the first is a hydrous silicate of alumina and 
 potash, having the composition of gieseckite. The second is a hydrous 
 silicate of alumina, and is apparently a compact pyrophyllite. The 
 third is a silicate of magnesia, having the composition of talc or pyrallolite, 
 to which last species it belongs (see page 470). Of these three figure- 
 stones, the second and third are nearly infusible before the blow-pipe, and 
 are scarcely attacked by acids ; while the first fuses to a white enamel, 
 and is readily decomposed by hydrochloric acid, the silica separating in a 
 pulverulent form. 
 
 The minerals known by the names of gieseckite, liebnerite, and pinite, 
 all of which appear to crystallize in the hexagonal system, agree in compo- 
 sition, being hydrous silicates of alumina and potash, like the first menr 
 tioned kind of figure-stone, which seems to be only a massive variety of 
 gieseckite. So long, therefore, as the crystalline form of agalmatolite is 
 unknown, it may be provisionally united with gieseckite. 
 
 Gieseckite. The crystallized gieseckite which occurs in the Laurentian limestones of 
 Diana, Lewis County, New York, associated with a dark brown pyroxene, 
 and with magnetic pyrites, has been described by Prof. Brush. It forms 
 large and thick hexagonal prisms, sometimes two inches or more in diam- 
 
CBAP. XVII.] MINERAL SPECIES. 483 
 
 eter, and often exhibiting pyramidal planes. Considerable variations 
 are observed in the angles of these crystals, whose cleavage is sometimes 
 very distinct with the sides of the prisms, and at others scarcely percep- 
 tible. Its colors are pea-green and leek-green, and its lustre vitreous or 
 greasy. Thin fragments are translucent. The specific gravity of the min- 
 eral is from 2-73 to 2*75, and its hardness about that of calcite, or from 
 3*0 to 3*5, Its composition is very constant : one of three closely agree- 
 ing analysis gave to Brush, silica 45*70, alumina 31-65, protoxyd of 
 iron 1-10, lime 2-21, magnesia 3-46, soda 0-90, potash 8-06, water 7-01 
 = 100-09. (Am. Jour, of Science [2], xxvi. 64.) 
 
 The name of wilsonite has been given to a mineral discovered in the 
 township of Bathurst, by Dr. Wilson of Perth. It is associated with a 
 white aluminous pyroxene, described on page 467, together with calcite, 
 inica, and prisms of blue apatite. The wilsonite is in rose-red prismatic 
 masses, which have two perfect parallel cleavages, apparently nearly at 
 right angles, giving to the mineral a somewhat fibrous aspect, besides two 
 distinct diagonal cleavages.. The mineral has a hardness of 3-5, or a 
 little greater than that of calcite, on the planes of easy cleavage, but attains 
 5-5 at the extremities of the. prisms. Its specific gravity equals 2-76- 
 2-77. The lustre of the mineral is vitreous, shining, and somewhat pearly 
 on the cleavage surfaces : thin fragments of it are translucent. Its reac- 
 tions with the blow-pipe, and with strong acids, are like those of agalmato- 
 lite. Dilute hydrochloric acid removes from the powdered mineral a 
 portion of carbonate of lime, without however attacking the silicate, or 
 changing its color. Two analyses of the wilsonite thus purified, gave the 
 following results : 
 
 I. H. 
 
 Silica, 47-50 47-70 
 
 Alumina, 31-17 31-22 
 
 Magnesia, 4-25 4-14 
 
 Lime, 1-51 0-39 
 
 Potash, 9-22 9-38 
 
 Soda, 0-82 0-95 
 
 Water, 5-50 6-35 
 
 99-97 99-13 
 
 It contains, in addition, traces of maganese, to which its color is probably 
 due. As gieseckite has, by some mineralogists, been looked upon as the 
 result of an alteration of nepheline or some other hexagonal species, so 
 wilsonite has been called an altered scapolite. The notion of such alter- 
 ations or pseudomorphism is, however, rejected by many of the best P niMn 
 authorities at the present day, and there is no good reason for supposing 
 that these minerals ever had a different composition from their present one. 
 The crystalline form and cleavages of wilsonite are obscure ; but its other 
 
484 GEOLOGY OF CANADA. [CHAP, XVII. 
 
 characters, and its composition approach so closely to those of gieseckite, 
 that it may with propriety be considered as a variety of this mineral species 
 for the present. 
 
 Dysyntribite. Associated with the iron ores of the Laurentian system, at Rossie and 
 at Diana, in New York, occurs a rock which had been regarded as ser- 
 pentine until 1849, when Prof. C. U. Shepard described it as a hydrous 
 silicate of alumina, to which, from its toughness, he gave the name of 
 dysyntribite. He, however, overlooked the presence of potash in the 
 mineral; and in'1853, Profs. Smith and Brush, by their analyses, showed 
 that it contained a large proportion of this alkali, and was closely allied to 
 agalmatolite and to pinite in composition. It has a hardness of 3-0 - 3-5, 
 and a specific gravity of 2*76-2-81, is of a dull greyish-green color, 
 sometimes mottled with red, and is somewhat translucent on the angles. 
 This rock has not yet been found in the Laurentian system in Canada, but 
 is represented in the Silurian series. 
 
 I n 1852, before the true composition of dysyntribite was known, a simi- 
 lar rock, from St. Nicholas, which had at first been taken for serpentine, was 
 described by the name of parophite. It occurs in the vicinity of an intru- 
 sive mass of trap, which traverses shales belonging to the Quebec group, 
 apparently converting portions of them into a pale green translucent unc- 
 tuous substance, which sometimes forms layers an inch in thickness, and is 
 seen coating interstratified beds of sandstone, and also filling up small 
 fissures in an indurated red argillite. In one instance, a layer of the shale 
 several inches in thickness, was found to be earthy within, but translucent 
 at its contact with the overlying rock. In a continuation of 'the layer, 
 where it became thinner, the transformation of the shale into the green 
 translucent mineral was complete. Comparative analyses showed that this 
 does not differ in composition from the earthy shale, the change from the 
 one to the other being only molecular. This parophite, or rather agalma- 
 tolite, is massive and granular, or schistose in texture. Sometimes it is 
 botryoidal, with a concentric structure and a conchoidal fracture. Its 
 hardness varies from 2-5 to 3-0, and its specific gravity from 2-68 to 2-78. 
 The lustre of the mineral is waxy and shining, and its color varies from 
 greenish-white to olive-green. It is sub-translucent, and unctuous to the 
 touch, like steatite. The accompanying slate, which passes in a little dis- 
 tance into the agalmatolite, is dark ash-grey, marked with red. Its laminae 
 are somewhat curved, the surfaces feebly shining and slightly unctuous. 
 It is completely earthy and opaque, even on the edges, very soft, so as to 
 be scratched by the nail, and not at all gritty. 
 
 A layer of agalmatolite, which had in like manner been taken for ser- 
 pentine, forms a thin bed in clay slate, near the Famine River, in the 
 parish of St. Francis, Beauce. It is honey-yellow, translucent, granular 
 in texture, with a waxy lustre, and is readily cut with a knife, giving an 
 
CHAP. XVII.] 
 
 MINERAL SPECIES. 
 
 485 
 
 unctuous powder. The same mineral occurs with chloritic slates on the Agaimatoiite. 
 east shore of Lake Memphramagog, on the fifteenth lot of the first range 
 of Stanstead, forming a belt one hundred and fifty feet wide. In some 
 portions the agalmatolite is granular and nearly free from admixture ; 
 in others, it holds a good deal of quartz, and becomes very schistose. A 
 thin layer of the pure agalmatolite, at this locality, has a banded structure 
 and a ligneous aspect, with a shiny satiny lustre. It is translucent, of a 
 wax or amber-yellow color, and, being very unctuous to the touch, resem- 
 bles steatite. The analyses of some of the above substances are subjoined. 
 I and II are the greenish translucent agalmatolite of St. Nicholas ; 
 III is the dark ash-grey earthy schist, passing in a short distance into the 
 preceding ; IV, the granular agalmatolite 6f St. Francis ; V, the ligneous 
 agalmatolite of Stanstead. 
 
 I. II. III. IV. V. 
 
 Silica, 48-42 48'50 48-10 50-50 50-30 
 
 Alumina, 27-60 27-50 28-70 33-40 32-60 
 
 Protoxyd of iron, 4-50 5-67 4-80 traces traces 
 
 Lime, 2-80 1-30 2-10 " 
 
 Magnesia 1'80 2'24 1-41 1-00 1-20 
 
 Potash, 5-02 5-30 4-49 8-10 nndet. 
 
 Soda, 2-78 1-91 1-53 '63 " 
 
 Water, 6-88 7'40 8-40 5-36 6-50 
 
 99-80 99-82 99-53 98'99 
 
 Similar rocks to the above occur in the continuation of the same series 
 southward into Vermont. In the recent Report on the Geology of that 
 State, page 505, is an analysis, by Mr. G. F. Barker, of what had been 
 called a magnesian slate, from Pownal, Vermont. It was bluish-grey, 
 unctuous, and had a specific gravity of 2-90 : its composition is given in the 
 analysis VI below. VII, VIII, and IX are analyses by Smith and Brush, 
 of different specimens of the dysyntribite of Shepard, from northern New 
 York. (Am. Jour, of Science [2], xvi, 50.] 
 
 VI. VII. VIII. IX. 
 
 Silica, 42-90 44-80 46-70 44-74 
 
 Alumina, 42-20 34-90 31-01 20-98 
 
 Protoxyd of iron, 3-01 3-69 4-27 
 
 " manganese, 0-30 traces traces 
 
 Lime, 0-78 0-66 " 12-90 
 
 Magnesia, 1-98 0-42 0-50 8-48 
 
 Potash, 5-24 6'87 11-68 3-73 
 
 Soda, 1-33 3-60 traces traces 
 
 Volatile (water), 5-60 5-38 5-30 4'86 
 
 100-03 
 
 99-94 
 
 99-88 
 
 99-96 
 
486 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 In VI, an undetermined portion of peroxyd of iron is included with the 
 alumina. VII and VIII, as will be seen, approach near to pure agalmat- 
 olite in composition ; while in IX the smaller amounts of alumina and 
 alkalies, and the large proportions of lime, and magnesia as silicates, 
 indicates an admixture of something like pyroxene. The onkosine of 
 Kobell, which occurs at Salzburg, in masses in a micaceous dolomite, is a 
 substance similar to the above. 
 
 The conclusion from all these analyses is, that there exists a hydrous 
 silicate of alumina and potash, remarkable for the small proportion of silica 
 that it contains, which occurs crystallized, and in a nearly pure state, in 
 gieseckite, wilsonite, liebnerite, and pinite. In a massive form, and often 
 more or less impure, it forms a stratified rock, which has been described 
 under the various names of dysyntribite, parophite, magnesian slate, and 
 agalmatolite, which latter name it will be convenient to retain. The anal- 
 yses of the specimens from St. Nicholas appear to show that this mineral 
 exists there as an earthy sedimentary deposit, which has been converted 
 into green translucent agalmatolite by the action of an intrusive rock. 
 The local metamorphism from this cause has here produced, within a limited 
 space, similar changes to that wide-spread action which has altered the 
 whole series of strata farther south, and given rise to the agalmatolites of 
 St. Francis and of Stanstead. 
 
 GLAUCONITE OK GREEN-SAND. 
 
 The glauconite or green-sand of the Cretaceous formation in Europe 
 and the United States, is a hydrous silicate of protoxyd of iron and potash, 
 with a variable amount of alumina. It appears to be related to the agal- 
 matolite just described, by the small proportion of silica and the large 
 amount of potash which it contains. Glauconite occurs in rounded grains, 
 which are sometimes disseminated through limestone, and at others form 
 layers, nearly pure, or mingled only with portions of clay or of quartz sand. 
 These grains, according to the observations of Ehrenberg and Bailey, often 
 occur filling the shells of polythalamia, small spiral mollusks and tubuli, 
 and even the cavities of corals and the spines of echini. With these casts 
 are however other rounded and irregular grains of green-sand, which do 
 not appear to have been formed in any such moulds. This substance is not 
 only abundant in Cretaceous and Tertiary deposits, but is now forming in 
 the ocean, and fills the shells of recent species of polythalamia, obtained 
 from deep-sea soundings along the coast of North America. (Amer. Jour, 
 of Science [2], xxii, 281.) 
 
 The grains of glauconite have about the hardness of gypsum, and are 
 blackish-green: when crushed upon white paper they give an olive-green 
 stain. A portion of the glauconite from the Cretaceous formation of New 
 Jersey, was freed from clay by washing, and then submitted to analysis by 
 digestion in hydrochloric acid. From the residue, about twenty-five per 
 
CHAP. XVII.] -MINERAL SPECIES. 487 
 
 cent, of quartz sand was separated. The soluble portion consisted of silica 
 50-70, alumina 8-03, peroxyd of iron 22-50, lime 1-11, magnesia 2-16, 
 potash 5-80, soda 0-75, volatile 8-95 = 100.00. Other analyses by Rogers 
 and by Fisher, of glauconite from the same region, agree closely with this, 
 but give from 3-85 to 6-50 of alumina. Mallet found the latter amount in 
 the same mineral from Alabama ; while the glauconite of Westphalia, 
 according to Von Dechen, contains ten per cent, of alumina. This base, 
 in variable proportions, seems, then, to enter into the composition of 
 glauconite, replacing a part of the protoxyd of iron. 
 
 The rocks of the Quebec group are, in some localities, characterized tiy Green-sand 
 grains of a soft green mineral, which closely resembles the glauconite o 
 more recent formations, and sometimes constitutes a considerable propor- 
 tion of beds of sandstone or shale. A sandstone of this kind from Point point Le>is. 
 Levis, which was free from calcareous matter, and abounded in these 
 grains, was reduced to powder, and digested with hydrochloric acid until 
 the green mineral was decomposed. The separated silica was removed by 
 carbonate of soda from the residual quartzose sand, and the soluble mat- 
 ters, from two different specimens of the rock, were as follows for 100 parts: 
 
 Silica, 11-40 12-26 
 
 Alumina, 5-66 6-84 
 
 Protoxyd of iron, 7-56 6'38 
 
 Lime, 0-20 0-18 
 
 Magnesia, 0-44 0-86 
 
 Potash, 1-60 1-48 
 
 2686 28-00 
 
 On the Island of Orleans, between beds of a dolomitic conglomerate, are Orleans 
 thin layers of a friable sandstone, made up of grains of quartz, with others Island> 
 a soft green mineral resembling that just described, and giving a bright 
 bluish-green powder. By crushing the rock and sifting, the coarser grains 
 of quartz were removed, and dilute nitric acid then dissolved a portion of 
 carbonate of lime which formed the cement of the rock. The analysis of 
 the green mineral was effected by hydrochloric acid, and the liberated 
 silica was separated from the insoluble quartz sand. I and II give the 
 results of two analyses of the substance, while III represents its 
 composition as calculated after deducting the quartz. 
 
 I. II. ill. 
 
 Silica, 31-32 31-30 50-7 
 
 Alumina, 12-20 12-15 19-8 
 
 Protoxyd of iron, 5-29 5-27 8-6 
 
 Magnesia, * 2-26 3-7 
 
 Potash 5-05 5-6p 8-2 
 
 Soda, - 0-33 0-5 
 
 Water (by ignition) 5-25 8-5 
 
 Quartz,...., 35-96 .... 
 
 97-66 100-0 
 
488 GEOLOGY OF CANADA. [CHAP. XVII, 
 
 This substance evidently differs from the glauconite of more recent for- 
 mations in the smaller amount of iron, and the great proportion of alumina, 
 which it contains. Green grains, apparently similar to those of the Quebec 
 group, are found in the fossiliferous magnesian limestones of the same age 
 in Texas ; and layers of a green mineral, described by Dr. Owen as a 
 silicate of iron, are abundant in the Lower Magnesian limestones of 
 Minnesota, where they are used by the Indians as a pigment. A speci- 
 men of this from Ked Bird, on the Mississippi, was interstratified and 
 intermingled with a magnesian limestone, which was removed by dilute 
 nitric acid. A mixture of the green mineral with angular grains of quartz, 
 was thus obtained, and gave by an analysis of 3-420 grams, as follows: 
 insoluble sand 1-590, silica -804, protoxyd of iron -356, alumina -198, 
 lime -043, magnesia -022, potash '120, soda -017, volatile -167, loss 
 103 = 3-420. The 'Soluble portion, calculated for 100 parts, is as fol- 
 lows : silica 46*58, protoxyd of iron 20-61, alumina 11-45, lime 2-49, 
 magnesia 1-27, potash 6-96, soda 0-98, volatile 9-66 = 100-00. Another 
 portion gave protoxyd of iron 19-73, alumina 11-03. The analyses of 
 the glauconite from New Jersey and from Minnesota show that a variable 
 proportion of alumina may enter into the composition of this silicate, and 
 serve to connect the more ferruginous mineral of the former locality with 
 the green-sand of Orleans Island. In this connection, it may be mentioned 
 that beds of a similar green-sand or glauconite occur near the base of the 
 Lower Silurian series in Russia. 
 
 Prof. E. J. Chapman has described bright green streaks and markings 
 in beds of a silicious limestone of the Black River formation, in the town- 
 ship of Rama. The green matter is said, in some cases at least, to be 
 collected around minute crystals of decomposed iron pyrites. It was 
 supposed, from its color, to be a compound of copper, but, according to 
 Prof. Chapman, it contains no traces of this metal. Silica, oxyd of iron, 
 and water were however detected in its composition, so that it is probably 
 related to glauconite. (Canadian Journal, iv, 493.) 
 
 CHLORITE, PYROSCLERITE, AND CLINTONITE. 
 
 chlorite. Chlorite has not yet been observed in the Laurentian series ; but it is 
 occasionally found disseminated in the diorites of the Huronian series, 
 which pass into a soft green schistose rock, that appears to be a chloritic 
 slate. Among the altered Silurian strata, chlorite is of frequent occurrence. 
 A pure massive variety, made up of a confused aggregation of small scales, 
 occurs with quartz, and sometimes with bitter-spar and feldspar, in what 
 appear to be veins among these schistose rocks. Chlorite also occurs dis- 
 seminated in 'dark green scales in limestones and in dolomites of this 
 series, or mixed with grains of quartz and feldspar, and sometimes with 
 specular iron, giving rise to chloritic sandstones and slates. Green scales 
 
CHAP. XVII.] MINERAL SPECIES. 489 
 
 of what seems to be chlorite, are also seen in the reddish talcoid argilla- 
 ceous slates, whose analysis gives a little magnesia, which may probably 
 be due to an intermixture of this mineral. 
 
 Dr. Bigsby has described the occurrence of chlorite among the crystal- 
 line rocks to the north of Lake Superior, on Rainy Lake, and also on the 
 Lake of the Woods, where a bed of slaty chlorite occurs in greenstone, 
 and holds octahedral iron ore and cubic pyrites. 
 
 The chlorite of the older authorities includes several closely related Foliated 
 species, now regarded as distinct. Among these are chlorite proper ^c"^, 1 ** 
 (including pennine andleuchtenbergite), clinochlore, and ripidolite, which 
 differ in optical and crystallographic characters, and offer, moreover, some 
 variations in chemical composition. They are all, however, basic hydrous 
 silicates of alumina, with magnesia; a variable portion of which is 
 replaced by protoxyd of iron. The same metal, in the state of peroxyd, 
 according to Rammelsberg, sometimes replaces a part of the alumina. 
 All of these chloritic minerals have an eminently foliated structure, and 
 resemble talc on the one hand and the micas on the other. Closely related py r08C ie- 
 to the chlorites, both in structure and in composition, is pyrosclerite, to rite - 
 which vermiculite, rhodochrome, and kammererite belong. These latter 
 varieties contain small portions of oxyd of chrome, to which they owe a 
 purplish color. They are generally found in serpentine, with chromic iron, 
 and the localities of this ore in Melbourne and Bolton present small 
 portions of what appears to be kammererite. 
 
 Clintonite is the name which has been given to a foliated hydrous ciintonite, 
 silicate of alumina and magnesia, containing some lime, which constitutes 
 a very distinct species, and includes the holmesite of Dr. Thompson, and 
 the xanthophyllite and disterrite of other authors. Clintonite occurs with 
 blue spinel in a crystalline limestone in Daillebout. 
 
 LOGANITE AND SOME ALLIED MINERALS. 
 
 an 
 silicates. 
 
 Related to the foliated or mica-like group of magnesian species, which sparry 
 includes talc, the chlorites, pyrosclerite, ciintonite, and the magnesian 
 micas, is a series of minerals, closely resembling these in composition, 
 density, and hardness, but entirely different in structure. They are 
 prismatic, and may be described as spar-like, with the form and the 
 cleavage of pyroxene, or of hornblende. Having generally been regarded 
 as results of the alteration of one or other of these two minerals, the rank 
 of distinct species has been refused to them, while the specific distinct- 
 ness of the corresponding foliated minerals is not disputed. 
 
 First among these sparry magnesian minerals, is the one which corres- 
 ponds to talc, and has already been described by the name of pyrallolite, 
 or rensselaerite (page 470). To this series also belong the following 
 alumino-magnesian minerals, which havb been described by Dr. Beck as 
 
490 GEOLOGY OF CANADA. [CHAP. XVIt 
 
 occurring among the crystalline limestones of Orange County, New York 
 They are grey or greenish-grey in color, somewhat translucent, soft 
 readily cut with a knife, and unctuous to the touch. Both of thes< 
 minerals are crystallized in long rhomboidal prisms, having the cleavagi 
 and the angles of hornblende. Their specific gravity is not given ; bu 
 their composition, as found by Dr. Beck, is subjoined in the analyses ' 
 and II. (Trans. Am. Assoc. Geologists 1840-42, 244.) Ill is tin 
 analysis, by Delesse, of a closely related mineral, which occurs in th 
 crystalline limestone of the Vosges, in France, and resembles serpentici 
 in its external characters. It is uncrystalline, soft, of a waxy lustre, i 
 greenish color, has a specific gravity of 2 '622, and contains traces o 
 chrome and of manganese. (Ann. des Mines [4], xx, 155.) 
 
 I. ir. m. 
 
 Silica, 35-00 34-66 38-39 
 
 Alumina, 32-30 25-33 26-54 
 
 Peroxyd of iron, .... -59 
 
 Lime, 10-80 5-09 -67 
 
 Magnesia, 20-70 25-22 22-16 (by diff.) 
 
 Water, 1-17 9-09 11-65 
 
 99-77 99-39 100-00 
 
 Hydrated aluminous magnesian minerals, sparry in crystallization, m 
 related to the above, are met with in several localities among the Laurentia 
 calumet limestones in Canada. The first one to be mentioned occurs at the Calume 
 Falls - Falls. It is associated with pale green serpentine, brown phlogopitc 
 and apatite, in a white crystalline limestone, and has been described b; 
 the name of loganite. It occurs in short thick oblique rhombic prisms 
 replaced on the edges, or on the acute solid angles. The crystals ar 
 generally rounded, but present a prism of 124, or near to that c 
 hornblende. There is a distinct cleavage with the sides and the base c 
 the prism, and an imperfect one with the longer diagonal. The hardnes 
 of the mineral is about that of calcareous spar, and its specific gravity i 
 from 2 60 to 2 64. The surface of the crystals is dull, but the lustre ( 
 the cleavages is vitreous and shining. The color is clove-brown c 
 chocolate-brown, often pale, and the mineral is sub-translucent, britth 
 and with an uneven fracture. The crystals, which are seldom more tha 
 one fourth of an inch in diameter, are penetrated by carbonate of lim< 
 from which they are with difficulty freed. The mineral is infusible befoi 
 the blowpipe, and partially decomposed by acids. 
 
 In the following analyses, a portion of carbonic acid, combined with th 
 lime, is included hi IV and V. In VI, the composition is calculated fc 
 100 parts, excluding the carbonate of lime. 
 
CHAP. XVIL] MINERAL SPECIES. 491 
 
 IV. V. VI. 
 
 Silica, 32-84 32-14 33-28 
 
 Alumina, 13-37 13-00 13-30 
 
 Magnesia, 35-12 36-43 35-50 
 
 Peroxyd of iron, 2-00 2-28 1-92 
 
 Volatile, 17-02 16-83 16-00 
 
 Lime, *96 -93 
 
 101-31 101-61 100-00 
 
 Associated with the extensive deposit of crystalline phosphate of lime North 
 in North Elmsley, is a mineral closely resembling the loganite in its char- Elmsley - 
 acters. It exists as a small bed in the limestone, and forms with it a 
 granular mixture, inclosing masses of the pure mineral, which closely re- 
 sembles pyroxene in appearance. The prismatic cleavages are perfect, 
 the basal cleavage indistinct. The hardness is not greater than calcareous 
 spar, and the specific gravity from 2-538 to 2-539. The color of the 
 mineral is greenish-grey ; its powder is white and unctuous to the touch. 
 The lustre is resinous, shining ; the mineral is brittle and somewhat trans- 
 lucent on the edges. Crystals of hard unaltered dark-brown sphene, and 
 small masses of flesh-colored calcite, are imbedded in it. The analyses of 
 two pure specimens of this sparry silicate gave VII and VIII. 
 
 A mineral almost identical with this occurs in North Burgess, in a pyrox- North 
 enic rock, with large crystals of a magnesian mica, which last has been Bur s e88 - 
 wrought to a considerable extent. The mineral in question is found in 
 imbedded cleavable masses, sometimes several inches in diameter. It has 
 the cleavage of pyroxene, a hardness between gypsum and calcite, and a 
 specific gravity of 2-32-2-35. It is pale greyish-green in color, very unc- 
 tuous to the touch, translucent on the edges, and has a waxy lustre. The 
 results of two analyses of this mineral are given under IX and X. 
 
 VII. VIII. IX. X. 
 
 Silica 36-90 36-50 39-70 38-90 
 
 Alumina 11-13 10-80 14-20 14-30 
 
 Magnesia 28-11 28-26 25-84 25-62 
 
 Protoxyd of iron 9-18 9-54 4-50 4-32 
 
 Water 14-00 14-62 16*20 17-66 
 
 99-32 99-72 100-44 100-80 
 
 The two minerals last described approach nearly in composition and in 
 general character to loganite. This latter was by Dana referred to pyro- 
 sclerite, with which it closely agrees in composition ; but it differs completely 
 in the absence of the micaceous or foliated structure, and also in contain- 
 ing more water. The low specific gravity of the mineral IX and X 
 is worthy of notice. The variations in the composition of this sparry sili- 
 cate from different localities are not more considerable than those of the 
 different varieties of chlorite and of serpentine ; and although they may here- 
 
492 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 after constitute grounds for specific distinctions, it will be well, for the 
 present, to include the silicates from North Burgess and North Elmsley, 
 with that from the Calumet, under the name of loganite. This mineral 
 is to be distinguished from pyrosclerite or kammererite, not only by its 
 greater amount of water, but by a crystalline form resembling that 
 of pyroxene or hornblende, and a sparry structure very distinct from the 
 micaceous one of pyrosclerite, which is due to the perfect basal cleavage 
 possessed by this latter species in common with the micas, chlorites, and 
 talc. The sparry minerals pyrallolite and loganite are thus represented 
 in the latter group by talc and pyrosclerite, while the sparry silicates 
 described by Beck and Delesse (I, II, and III), have no known foliaceous 
 representatives. Gieseckite represents in composition a hydrous potash mica. 
 The pyroxenic rock from North Burgess, which encloses the loganite, 
 closely resembles it in cleavage and in color, but has a greater hardness, 
 and a specific gravity of 3.003. It is mingled with a portion of car- 
 bonate of lime ; after removing which by a dilute acid, the mineral gave, 
 by analysis, as follows: silica 54*30, alumina 3-70, protoxide of iron 2-07, 
 lime 10-39, magnesia 23-61, volatile 5.43 = 99-63. 
 
 Beryl. This species is frequently met with in granitic veins, associated with 
 garnet, tourmaline, and chrysoberyl among the crystalline strata of Maine, 
 New Hampshire, Massachusetts, and Connecticut, which are supposed to 
 be of palaeozoic age. It has not, however, been noticed among the rocks 
 of Vermont, or of south-eastern Canada. In the Laurentian system, 
 granitic veins with tourmaline, zircon, and mica, the associates of beryl, are 
 met with ; and in one of these in Saratoga County, New York, chrysoberyl 
 occurs in some abundance. According to Dr. Bigsby, beryl is found 
 in well-defined pale green crystals, with black mica, in a porphyritic 
 granite, associated with gneiss and mica schist on the east side of Rainy 
 Lake, two hundred and thirty miles to the north of Lake Superior. 
 
 TOURMALINE AND AXINITE. 
 
 Tourma- Black tourmaline is abundant in many places among the Laurentian 
 rocks. A remarkable locality is described by Dr. Bigsby as occurring 
 among the Thousand Islands, on the south side of the English channel, 
 and near the upper end of Tar Island, on Yeo's Island, which is about 
 three hundred yards long, and divided by a ravine into two unequal parts ; 
 on the south-western of which, and on the face of a shelving mound of whitish 
 granite, is a bed twelve paces in diameter, consisting of large crystals of 
 black tourmaline, with greenish-yellow mica, quartz, and feldspar. In 
 other parts of the same island, black tourmaline abounds, in granitic veins 
 
OHAP. XVII.] MINERAL SPECIES. 493 
 
 which traverse a fine-grained gneiss. Other localities mentioned by 
 Dr. Bigsby are Murray Bay, and Cape Tourmente. Finely terminated 
 crystals of black tourmaline, an inch in diameter, occur in white quartz on 
 the eighteenth lot of the fourth range of Bathurst, and in quartz veins in 
 Eardley. Granitic veins, holding the same mineral, are met with in the 
 township of Ross, on the Roche-Fendue Channel, in Carrying-Place Bay, 
 on Charleston Lake, on Stoney Lake in Dummer, and on the west side of 
 the North River at St. Jdrfane. Here the tourmaline is associated with 
 small crystals of zircon. Black tourmaline also occurs associated with 
 pyroxene and hornblende on the Madawaska (see pages 35 and 467). 
 Other localities are Elmsley, Lachute, St. Felix, and the Calumet Falls. 
 
 A peculiar variety of black tourmaline is found in white quartz near 
 Madoc, and in Elzivir. It forms veins of an inch or more in width, made 
 up of very fine fibres transverse to the sides of the vein, velvet black 
 in color, and with a silky lustre resembling masses of what is called mineral 
 charcoal, for which it had been mistaken. The powder of the mineral 
 from Madoc is bluish-black, becoming pale by ignition. A partial analysis 
 of it gave silica 36-50, alumina 27 '45, peroxyd of iron 14 '90, magnesia 
 6'05, and lime 1-12. This shows the mineral to be an iron-magnesia tour- 
 maline, which, in parts, may be observed in the form of black acicular 
 crystals penetrating the quartz. 
 
 Brown tourmaline is frequently met with in the limestone of the Lau- Brown 
 rentian series. At the Calumet Falls, crystals of this mineral, an inch 
 in diameter, have been found imbedded in flesh-red limestone, with ido- 
 crase. They are somewhat translucent, of a rich yellowish-brown color, 
 highly modified, and with brilliant planes. The specific gravity of the 
 these crystals is 3 '03. Similar crystals, almost equal in beauty, have 
 been found with pyroxene in limestone, in the township of Ross, and also 
 in Clarendon ; and a single transparent crystal, remarkable for its modifi- 
 cations, was obtained near Hunterstown. This, together with a crystal 
 from Ross, is figured in Dana's Manual of Mineralogy, 4th edition, page 
 270, figures 457 and 460. Slender delicate prisms of hair-brown tourma- 
 line occur in white quartz, in Fitzroy, and at the Island Portage, Lac des 
 Chats. At McGregor's quarry at Lachute, grains and imperfect crystals 
 of brown tourmaline are disseminated in the limestone, of which they 
 seem to mark the lines of stratification. 
 
 The rare species axinite is said by Dr. Bigsby to have been found in Axinite 
 fine crystals, lining a cavity in a boulder of primitive rock at Hawkesbury. 
 
 MICAS, MUSCOVITE AOT) PHLOGOPITE. 
 
 The group of the micas includes two principal divisions : those which are 
 essentially silicates of alumina and alkalies, chiefly potash, often with lithia 
 and fluorine, including muscovite and lepidolite ; and the magnesian micas 
 
494 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 phlogopite and biotite ; the former group generally belonging to granitic 
 rocks, and the latter to limestones. The magnesian micas often present 
 some variations in their composition, and the hydrated ones offer a natural 
 transition to the foliaceous magnesian species, chlorite and pyrosclerite. 
 Muscovite. . Among the localities of muscovite may be noticed the tourmaline locality 
 on Yeo's Island, described above, and many of the granitic veins already 
 mentioned. Large crystals are also found in an immense vein of graphic 
 granite on Allumette Lake (page 36). A porphyritic granite on Cape 
 Tourmente, according to Dr. Bigsby, holds great crystals of mica a foot 
 in diameter. Mica enters, to a small extent only, into the composition of 
 the gneiss of the Laurentian system ; and a dark brown mica is sparingly 
 met with in the anorthosites of the same series. In the altered rocks of 
 the Eastern Townships, micaceous schists are abundant, generally mingled 
 with quartz ; but in some cases, a rock is found which is almost entirely 
 made up of a mineral approaching in composition to a hydrous mica. In 
 Shipton, a mineral of this sort has been mistaken for a compact chlorite or 
 potstone, and wrought to some extent. It consists of an aggregation of 
 small greenish-grey scales, and contains silica 51-50, alumina 29*20, 
 protoxyd of iron 9*27, magnesia 1-08, potash 1*54, soda 1*59, water 5-10 
 = 99*28. Crystals of silvery mica occur in a quartz vein in Barford, 
 with white apatite, copper pyrites, and magnetic pyrites. 
 
 chromiferous A bright green colored mica, which contains in combination a portion of 
 oxyd of chromium, is found in several localities in the Eastern Townships. 
 Minute scales of it occur in the magnesite of Sutton ; and it is met with, in 
 larger plates and imperfect crystals, in a dolomite from Bolton. This 
 mica is probably allied to the chromiferous mica from the Tyrol, which has 
 been named fuchsite. 
 
 phlogopite Phlogopite is very common among the Laurentian limestones, sometimes 
 both in more or less abundantly disseminated in small scales or crystals, 
 pure limestones and dolomites. The colors of these small crystals are gen- 
 erally some shade of yellow or brown ; but in rare cases, they are of a deep 
 olive-green or silver-white. At the Calumet Falls, delicate olive-green 
 prisms of phlogopite, sometimes an inch in diameter and several inches 
 in length, are found imbedded with crystals of pyroxene in a pink, lamellar 
 limestone. In Burgess, large tables of a steel-grey mica, with a somewhat 
 metallic lustre, are found in a similar limestone, with crystallized apatite; a 
 prism of which was in one case found imbedded in a crystal of mica. 
 
 The largest specimens of phlogopite are generally found in beds near 
 to bands of quartzite or pyroxenic gneiss, which often limit the crys- 
 talline limestones, or are interstratified with them. The mica occurs in 
 large tabular crystals with pyroxene and calcite, and often with quartz, 
 orthoclase, and rarer minerals. Examples of this are met with in Grenville 
 and in North and South Burgess ; in all of which, the mica is obtained in 
 
 mica. 
 
CHAP. XVII.] MINERAL SPECIES. 495 
 
 large sheets, which, being transparent and free from flaws, are wrought and 
 employed for the same purposes as the muscovite or potash mica of granites. 
 In North Burgess, the phlogopite is imbedded in a pyroxenic rock, with 
 loganite (page 490), and affords plates which sometimes measure twenty 
 by thirty inches. 
 
 This mica was submitted to analysis, and gave as follows : silica 40-97, 
 alumina 18-56, magnesia 25-80, potash 8-26, soda 1-08, volatile 1-00, 
 loss, probably fluorine, 4-33 = 100-00. Another specimen gave silica 
 40-55, alumina 18-10, volatile 0-66. In one of these analyses the mica 
 was decomposed by heated sulphuric acid, and in the other by fusion with 
 carbonate of soda. The alumina contained no trace of oxyd of iron. 
 
 PHOLERITE. 
 
 This mineral is identical in composition with the kaolin which arises from 
 the decomposition of feldspars, and it may be regarded as that substance in 
 a crystalline condition. From its foliated or micaceous structure, it may 
 be considered as a hydrated mica, bearing to muscovite a relation anal- 
 ogous to that which the chlorites and pyrosclerite sustain to phlogopite. 
 Phoierite occurs in the form of white unctuous films in the joints of many 
 quartzose sandstones of the Huronian series ; and what appears to be the 
 same mineral is occasionally met with in small botryoidal masses, lining 
 cavities in the jasper conglomerate of the same series. In a sandstone 
 of the Quebec group, just below the ChaudiSre Falls, pholerite is met with 
 filling fissures, and sometimes forms masses half an inch thick, composed of 
 minute soft scales, very unctuous and slightly coherent. The masses have 
 a greenish or yellowish-white color. Before the blowpipe, the mineral ex- 
 foliates in white cauliflower-like shapes, but is infusible. It gives off an 
 abundance of water when heated in a glass tube, and assumes a fine blue 
 color when ignited after having been moistened with nitrate of cobalt. The 
 mineral was separated as much as possible from intermingled grains of 
 quartz, by crushing it and suspending it in water. It was then levigated 
 and dried at 212 F., when its analysis gave silica 46*05, alumina 38-37, 
 lime 0-61, magnesia 0-63, water 14-00 == 99-66. Another analysis yielded 
 silica 45-55, and water 13-90. 
 
 GARNET AND IDOCRA8E. 
 
 Garnet forms with epidote and idocrase a group of double silicates of 
 alumina and protoxyd bases, distinguished from the feldspars by their much 
 greater specific gravity and hardness, and by the fact that sesquioxyds of 
 iron and manganese sometimes replace wholely or in part the alumina, while 
 magnesia, or the protoxyds of these same metals, may take the place of the 
 lime and alkalies which form the protoxyd bases of the feldspar series. 
 
496 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 Chloritoid may be looked upon as a hydrated species belonging to the 
 same group of silicates. 
 
 Garnet. Garnet is frequently met with in the Laurentian rocks. It is often dis- 
 seminated in grains or imperfect crystals through the gneiss, and charac- 
 terizes great masses of quartzite. Beds of nearly pure red garnetoock 
 are sometimes met with, as in gneiss in St. Je*r6me, in quartzite in Rawdon, 
 Marmora, and at Bay St. Paul. Imperfect crystals, several inches in 
 diameter, occur in the gneiss of Murray Bay. A rose-red garnet, dissemi- 
 nated in small masses through a white orthoclase gneiss at Lake Simon, 
 on the river Rouge, gave by analysis, silica 37*80, alumina 21-00, lime 
 1-81, magnesia 8-85, protoxyd of iron 29-03, volatile 0-18 = 98-67. 
 
 idocrase. Small crystals of cinnamon-colored garnet have been observed with 
 crystals of wax-yellow idocrase, pyroxene, and zircon, in calcareous spar 
 at Grenville, and also imbedded in limestone with brown tourmaline and 
 idocrase, in a boulder ; the three species being nearly alike in color. Large 
 crystals of brown idocrase occur with brown tourmaline, at the Calumet 
 
 wwte Falls. 
 
 M3k ' A remarkable variety of white lime-alumina garnet occurs with the 
 serpentines of the Eastern Townships. In Orford it is found in small 
 rounded masses, which, with a little intermingled serpentine, make up a 
 rock. This garnet is compact, very tough, and has a conchoidal fracture. 
 It is sub-translucent, with a waxy lustre, greenish or yellowish-white in 
 color, and has the hardness of quartz, and a specific gravity of 3-52-3-53. 
 Its analysis gave silica 38-60, alumina 22-71, lime 34-83, magnesia 0-49, 
 oxyds of iron and manganese 1-60, soda and a trace of potash 047, 
 volatile 1-10 = 99-80. After intense ignition, which did not effect its 
 fusion, the mineral gelatinized with hydrochloric acid. 
 
 An apparently homogeneous rock, composed in great part of a similar 
 garnet, occurs in contact with serpentine, in St. Erancis. It is extremely 
 tough, and so hard as to scratch deeply the surface of agate. Its specific 
 gravity is 3*33-3-36. This rock has a sub-conchoidal fracture, a feebly 
 shining lustre, is yellowish-white and somewhat translucent. Another 
 variety in the same vicinity is greenish-white, somewhat granular, and 
 exhibits imperfect crystals in drusy cavities. It has a specific gravity of 
 3*39-3-43. Grains of native gold have been observed in this white 
 garnet-rock. Another rock, near by, was found to consist of a similar white 
 garnet, with a density of 3-49, mingled with a softer white feldspathic 
 mineral, of density 2*73-2*83, and with a greenish and greyish horn- 
 blende, having a specific gravity of 3 * 046 ; the whole forming a coarse- 
 grained aggregate. 
 
 The compact garnet-rock, of density 3 33, did not effervesce with heated 
 nitric acid ; and it gave on analysis, silica 44 85, alumina 10 * 76, peroxyd of 
 iron 3*20, lime 34*38, magnesia 5 -24, volatile 1-10 = 99*53. The 
 alumina and oxyd of iron, with 22*69 of silica and 21*07 of lime, make 
 
CHAP. XVII.] MINERAL SPECIES. 497 
 
 up 57 " 72 of garnet, and the remaining elements form 40 71 per cent, of 
 a bi-silicate of lime and magnesia, approaching to pyroxene in composition. 
 A white massive garnet-rock, similar to that from Orford, and associated 
 with serpentine, comes from Beyrouth, in Bavaria. 
 
 A beautiful green garnet occurs in the sixth lot of the twelfth range of Green 
 Orford. It forms granular masses, or is disseminated with millerite (sul- chrome - 
 phuret of nickel), in a white crystalline calcite. The largest crystals are 
 found in druses in the massive portions, but do not exceed a line in diam- 
 eter, and are dodecahedrons, sometimes with their edges replaced. The 
 mineral is transparent, with an emerald-green color, which is not altered 
 by a red heat. This garnet resembles closely the ouvarovite from the Urals, 
 but differs in containing a much larger proportion of alumina and less 
 oxyd of chrome. Its analysis gave silica 36-65, alumina 17*50, oxyd of 
 chrome 6-20, protoxyd of iron 4-97, lime 33-20, magnesia 0-81, volatile 
 0-30 = 99-63. Another analysis gave oxyd of chrome 6-93, protoxyd of 
 iron 4-80, lime 33-29. This beautiful garnet, if obtained in sufficiently 
 large crystals, would constitute a gem equal in beauty to the emerald. 
 
 Large dodecahedrons of cinnamon-colored garnet, and others which are 
 yellowish or nearly white, occur with crystals of pyroxene (page 467), 
 in the immediate vicinity of this chrome-garnet. 
 
 A compact yellowish-green mineral, which resembles epidote in specific Epidote. 
 gravity and hardness, is occasionally met with in a reddish feldspathic 
 gneiss of the Laurentian series. Good examples of this occur near 
 Carleton Place. Crystalline epidote is also frequently found in amygdal- 
 oidal traps on Lake Superior, and is associated with native copper. At 
 Mamainse, crystals of epidote are met with, implanted upon mesolite, and 
 rarely associated with small brown garnets. 
 
 Epidote characterizes large portions of the altered Silurian rocks. It is 
 there generally associated with quartz, often forming veins or kernels, with 
 imperfect crystals, in a granular quartz-rock, which passes into mica-schist: 
 chlorite is a frequent accompaniment. In many parts occur beds which 
 are entirely made up of quartz and epidote ; sometimes in distinct grains, 
 at others forming a homogeneous rock, generally pale green, very tough 
 and sonorous. This rock is met with in beds among the chloritic schists 
 from St. Armand to Gaspe*. A specimen from the Grand Matanne Kiver, 
 having a hardness of 7-0, and a density of 3-04, gave by analysis, silica 
 62-60, alumina 12-30, peroxyd of iron 9-40, lime 14-10, magnesia 0-72, 
 soda 0-43, volatile 0-16 = 99-71 ; which corresponds to a mixture of 61 33 
 parts of epidote and 38 22 parts of quartz. This rock, which is the epido- 
 site of some lithologists, is also found in characteristic specimens in Mel- 
 
 GQ 
 
498 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 bourne. Well crystallized greenish epidote is found in the concretionary 
 argillaceous rock of St. Joseph, which is described on page 255. 
 
 CHLORITOID. 
 
 chioritoid. This mineral species is of common occurrence in the micaceous schists 
 of the Quebec group, in Eastern Canada, in which it is disseminated in 
 small grains and crystalline plates. It is abundant in a fine-grained 
 greyish wrinkled micaceous slate from Brome ; and in larger specimens, 
 from Leeds, where it occurs in a schistose rock, which is pearl-grey in 
 color, passing into greenish-grey, and is made up of quartz, with a mineral 
 having a talcose aspect, but aluminous in composition, and apparently a 
 mica. The chioritoid is imbedded in this rock, in small lamellar masses, 
 rarely more than one fourth of an inch broad, and one eighth of an inch 
 thick. Spherical masses, half an inch or more in diameter, are sometimes 
 found, composed of plates of the mineral radiating from a centre, and 
 often making up one half of the volume of the rock. The chioritoid has a 
 perfect cleavage in one direction, and two less distinct transverse 
 cleavages. The lamellae are often curved, and are not easily separable. 
 The hardness of this mineral is equal to that of feldspar, and its specific 
 gravity is 3 '513. Its color is dark-greenish grey, passing into black. 
 The planes of perfect cleavage have a brilliant vitreous lustre, but the 
 fracture presents a feeble waxy lustre. The powder of the mineral is 
 greenish-grey, becoming reddish by ignition. Its analysis gave, silica 
 26 30, alumina 37 10, protoxyd of iron 25 92, protoxyd of manganese 
 93, magnesia 3 66, water 6 10 = 100 01. 
 
 This species is identical with what has been described by the names of 
 barytophyllite, chlorite spar, sismondine, and masonite. The mineral from 
 Massachusetts, to which Dr. Thompson gave the name of phyllite, is per- 
 haps the same species, inasmuch as a specimen obtained from Mr. Heu; 
 land in London, and designated as " phyllite from North America" is chior- 
 itoid, closely resembling that from Leeds. The ottrelite of Hauy, from 
 Ottrez in Luxembourg, cannot be distinguished from the same species. 
 
 STAITKOTIDE. 
 
 staurotide Staurotide is found in mica schists in Vermont, but has not yet been 
 met with in Eastern Canada. According to Dr. Bigsby, however, it 
 occurs in the gneiss to the north of Lake Superior, (see page 65,) where 
 it is abundant in very small crystals on Rainy Lake, and in much larger 
 crystals on the river Lacroix, at the second portage from the lake of the 
 same name. 
 
CHAP. XVII.] MINERAL SPECIES. 499 
 
 ANDALU8ITE OB CHIASTOLITE. 
 
 This species occurs in somewhat micaceous argillites of Upper Silurian 
 or Devonian age, on Lake St. Francis. In some cases the mineral 
 forms slender flesh-red prisms, not more than one tenth of an inch in 
 diameter. In other portions of the rock, larger crystals inclose a black chiastoiite. 
 material, giving rise to that variety of andalusite which exhibits a cross in 
 its transverse section, and is known as chiastoiite (pages 430 and 433). 
 
 ZIRCON. 
 
 This mineral is found in some abundance associated with pyroxene, zircon, 
 tabular-spar, calcite, orthoclase, sphene, and plumbago, at Grenville, where 
 terminated prismatic crystals half an inch in diameter are sometimes met. 
 These are reddish-brown and opaque ; but smaller crystals from the same 
 locality are cherry-red and transparent. The specific gravity of this zircon 
 is 4-60-4-62 ; and it gave on analysis, silica 33*7, zirconia, with a trace of 
 oxyd of iron, 67-3 = 101-0. 
 
 Small brownish crystals of zircon have been found in St. Jdr6me, with 
 black tourmaline, in granitic veins which traverse gneiss. At Pic Island, 
 in Lake Superior, a mass of unstratified rock, composed of red somewhat 
 opalescent feldspar and black hornblende, contains small crystals of zircon. 
 
 SPINEL. 
 
 On the tenth lot of the first range of Burgess, the flesh-red Laurentian spinel, 
 limestone abounds in crystals of black spinel, which may be traced over 
 an extent of a mile or more. The crystals are sometimes an inch, or even 
 two inches in diameter, and are occasionally coated with mica, though 
 often brilliant, and exhibiting a replacement of the edges of the octa- 
 hedron. Fine groups of crystals, detached from the limestone, have here 
 been found loose in the soil. Black spinel in imperfect crystals occurs 
 with apatite and fluor-spar, in crystalline limestone in the township of 
 Ross. Small crystals of it have also been found with chondrodite in a 
 boulder of crystalline limestone near Ottawa ; and in a bed of micaceous 
 limestone in the seigniory of Daillebout, small translucent octahedrons of 
 blue spinel are met with. 
 
 CORUNDUM:. 
 
 Corundum has been observed on the second lot of the ninth range of Corundum, 
 Burgess, and in the immediate vicinity of a deposit of copper pyrites. 
 Here, in contact with the crystalline limestone, occurs a rock made'up of 
 feldspar, quartz, calcite, silvery white mica, and sphene. Disseminated 
 throughout- this aggregate were small grains of a mineral whose color 
 
500 GEOLOGY OF CANADA. [CHAP. XVII, 
 
 varied from light rose-red to sapphire blue, while its hardness, which was 
 greater than that of topaz, showed the mineral to be corundum. Small 
 crystals of light-blue corundum have been found elsewhere in the limestone 
 of the vicinity. 
 
 QTJABTZ. 
 
 Quartz. Notwithstanding the abundance of this mineral in the form of quartzite 
 among the different geological formations of the province, interesting min~ 
 eralogical varieties of quartz are rare. The trappean rocks along the 
 north shore of Lake Superior, however, yield amethysts in great abun- 
 dance, which are sometimes of a fine color. The small crystals of quartz 
 known as Quebec diamonds, occur in fissures in the limestones of the 
 Quebec group, and are occasionally an inch or more in diameter, and ter- 
 minated at both ends. The crystals from this locality offer some unusual 
 modifications in their form: Mr. Dana has figured one of them in his 
 Manual of Mineralogy, 4th edition, p. 146. These crystals are generally 
 colorless, but sometimes of a smoky brown, and in some rare instances, 
 according to Dr. Bigsby, contain a drop of pale bituminous liquid. Fine 
 transparent crystals are also found in the soil in Lacolle, and in drusy 
 cavities in the dolomites of the Calciferous formation in many places. 
 
 Large prismatic crystals of transparent quartz have been found in drusy 
 cavities of the quartz veins of the Bruce Mines. They are generally 
 incrusted with small crystals of copper pyrites. In the quartz veins at 
 Harvey's Hill Mine also, large transparent prismatic crystals several inches 
 in length occur, and sometimes hold regular crystals of copper pyrites., 
 which are completely encased in the quartz. 
 
 Agate. Agates are found in great abundance in the amygdaloids of Lake 
 Superior, and sometimes of considerable size and beauty. They abound 
 in rolled masses on the beaches of Michipicoten and St. Ignace Islands, at 
 Thunder Bay, and elsewhere along the coast. Agate or chalcedony is 
 here sometimes met with filling veins in a kind of pitchstone porphyry. 
 Small agates of delicate colors are also found, together with pebbles of 
 jasper, among the conglomerates of the Bonaventure formation, and are 
 known to collectors by the name of Gaspe* pebbles (page 404). 
 
 jasper. Beds of a red ferruginous jasper, often finely clouded, occur near Sher- 
 brooke and also at Riviere Ouelle. The jasper of the latter locality is trav- 
 ersed by veins of chalcedony. Jasper pebbles of various colors abound 
 in the conglomerates of the Huronian series. Beds of chert or hornstone 
 occur alike among the limestone of the Huronian series (p. 57), the Upper 
 Copper-bearing rocks of Lake Superior (p. 67), and their equivalents of 
 the Quebec group. Hornstone is also occasionally met with in nodules or in 
 layers among the limestones of the Trenton and Niagara groups, and in 
 great abundance in the Corniferous formation, to which it has given its 
 
CHAP. XVII.] MINERAL SPECIES. 501 
 
 name. In various formations and localities chalcedonic quartz is found in 
 limestone, replacing organic remains, in which the cavities are sometimes 
 filled or lined with quartz crystals. This is well seen in the Trenton forma- 
 tion on the Ottawa (page 176), and in the Corniferous formation in 
 various parts of Western Canada. The remarkable veins of chert in the 
 syenite of Grenville are described on page 41. 
 
 METALS AND METALLIC MINERALS. 
 
 Under this head may be noticed the various metals which are found in Metaia. 
 Canada in a native state, together with their ores, including oxyds and 
 sulphurets. They will be arranged as follows, beginning with the less 
 perfect metals : titanium, tungsten, molybdenum, chromium, uranium, 
 cerium, arsenic, nickel, cobalt, manganese, iron, zinc, copper, lead, mercury, 
 silver, gold, platinum, and iridium. 
 
 TITATUUM, ILMENITE AND KUTILE. 
 
 In the form of titaniferous iron ore or ilmenite this element is very Titanium, 
 abundant in the Laurentian series, where it appears to belong to the anor- Ilmenite - 
 thosites or triclinic feldspar rocks. In St. Je'rOme, Rawdon, and Chateau 
 Richer it occurs disseminated in grains, or in thin plates, which seem to 
 mark the lines of stratification. In the latter locality it forms masses 
 of several ounces weight, in a rock made up of andesine with a little 
 hypersthene. In the parish of St. Urban, at Bay St. Paul, great masses Bay st 
 of ilmenite are intercalated in the stratification. One of these, with a Paul 
 thickness of ninety feet, was traced for a distance of three hundred feet, 
 and is said to be continued, with perhaps slight interruptions, for the 
 -distance of a mile. Several smaller masses of the ore are also seen in the 
 neighborhood. The ilmenite is sometimes penetrated by grains of a 
 greenish triclinic feldspar, which forms the surrounding rock, and it con- 
 tains in many parts, orange-red transparent grains of pure titanic acid. This 
 ilmenite is coarsely granular or crystalline, and has a density of 4-56 -4- 66. 
 Its analysis gives titanic acid 48-60, protoxyd of iron 37*06, peroxyd of 
 iron 10-42, magnesia 3-60 = 99-68. The ilmenite of Chateau Richer has a 
 density of 4*65, and gives titanic acid 39-86, peroxyd of iron (in part as 
 peroxyd) 56-64, magnesia 1-44, insoluble quartz, 4-90 = 102-84. 
 
 The iron ores of the altered Silurian strata are very often titaniferous. 
 Such is the case with many of those of Brome and Sutton, which contain 
 one or two hundredths of titanic acid, probably as ilmenite, and are moreover 
 sometimes associated with sphene and rutile. In the seigniory of St. st. Francis. 
 Francis, Beauce, there is a bed of granular iron ore, forty-five feet wide, 
 in serpentine. When crushed and washed, to free it from a small portion 
 of earthy matters, it may be separated by the magnet into two portions. 
 
502 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVII. 
 
 Rutile. 
 
 Titanic 
 acid. 
 
 About two thirds of the whole is common magnetic oxyd of iron ; while the 
 remaining non-magnetic portion is ilmenite, which gave titanic acid 48-60, 
 peroxyd of iron 40-70, magnesia 2-44, insoluble 4-20, water and loss 
 4-06 = 100-00. A bed of magnetic iron occurring in serpentine at West 
 Troy in the state of Vermont, contains in like manner four per cent, of 
 titanic acid, probably in the form of ilmenite. 
 
 In the auriferous sands of Canada the black residue left after washing, 
 contains a large quantity of ilmenite, mixed with chromic iron, rutile, and 
 magnetic and specular oxyds of iron. In Sutton, small red flattened crys- 
 tals . of titanic acid are found with chlorite, specular iron, and orthoclase 
 feldspar. It is difficult to determine whether they belong to the species 
 rutile, or to brookite, both of which are pure titanic acid. The same doubt 
 applies to the red grains of titanic acid in the ilmenite from St. Urban, 
 which sometimes make up as much as one tenth of the mass of ore. It is, 
 however, probably rutile, which is the more common species, and is met 
 with crystallized in chlorite slate, in New England, in conditions similar 
 to that of Sutton. Rutile, in delicate acicular crystals, has been observed 
 in drusy cavities, with quartz, at the Wallace mine, on Lake Huron. 
 Connected with the presence of titanium in the metamorphic strata of the 
 Eastern Townships, may be mentioned its occurence in the red ferruginous 
 slates of Granby, which yield small portions of it on analysis. It is 
 probable, however, that this element is very often present in argillaceous 
 rocks. Titanic acid was also found in an impure greenish earthy limestone 
 from Granby, which, besides thirty per cent, of carbonate of lime, contains 
 small portions of manganese, chrome, and nickel, together with about six 
 per cent, of titanic acid. In like manner, the insoluble residue (amounting 
 to forty-six per cent.) from a ferruginous dolomite from Rougemont, gave 
 by analysis seven per cent, of titanic acid, which, as in the previous case, 
 is in an unknown state of combination. 
 
 sphene. Small veins of opaque yellowish sphene, sometimes stained green by 
 copper, have been found in the iron slates of Sutton. Minute amber- 
 yellow crystals of sphene are also met with in the granitoid trachytes of 
 Brome, Shefforii, and Yamaska, and in the diorite of Mount Johnson. 
 The crystals, which are brilliant and transparent, are seldom larger than a 
 grain of rice, and generally much smaller. Some of them, however, 
 admit of crystallographic measurement, and give the angles of sphene. 
 The partial analysis of a small portion of this mineral, from Yamaska 
 Mountain, gave silica 31 '5, titanic acid 40 -0, the remainder being lime. 
 In addition to sphene, these intrusive rocks often contain titanium in the 
 form of ihnenite. 
 
CHAP. XVII.] MINERAL SPECIES. 503 
 
 Sphene is often met with in the Laurentian limestones, generally 
 associated with those aggregates of quartz, pyroxene, and orthoclase 
 feldspar, which have been repeatedly noticed. The crystals, which are 
 often of considerable size, are generally clove-brown or chocolate-brown, 
 but sometimes yellowish or amber colored. Among other localities of 
 crystallized sphene, may be mentioned Lachute, Calumet Falls, and 
 Burgess, where a honey-yellow variety occurs with green pyroxene and 
 corundum. In North Elmsley, brown sphene is found imbedded in 
 loganite, at the quarry of phosphate of lime, and also, near by, with 
 pyroxene. Crystallized sphene occurs imbedded in calcareous spar, with Lederite, 
 pyroxene, tabular-spar, and zircon, on the tenth lot of the fifth range of Grenville - 
 Grenville. The plumbago mine formerly wrought by Mr. Harwood, on 
 the same lot, affords a remarkable massive variety of sphene, well known 
 to mineralogists, which, from its peculiar cleavages, was, by Sheperd, 
 distinguished as a subtspecies, with the name of lederite. Dana has 
 however shown that, although the same abnormal cleavage exists in 
 crystals of lederite from other localities, these have nevertheless the 
 crystalline forms of ordinary sphene, with which the Grenville mineral 
 agrees completely in composition. It is found with pyroxene, tabular- 
 spar, and calcite, in masses several inches in diameter ; and perfect 
 cleavage-forms measuring one or two inches may be obtained. It has the 
 usual hardness of sphene, and a specific gravity of 3 '49-3 -50. It is of 
 a light chocolate-brown in color, and is somewhat translucent. Its analysis 
 gave silica 31 83, titanic acid, with a trace of oxyd of iron, 40 * 00, lime 
 28-31, volatile 0- 40 = 100 -54. The titanic acid extracted from this 
 mineral exhibits all the characters of that from other sources. 
 
 TUNGSTEN. 
 
 The only example of an ore of tungsten yet known in Canada was found wolfram, 
 by Prof. Chapman, in a boulder of Laurentian gneiss, on Lake Couchi- 
 ching, which contained crystals of wolfram, or tungstate of iron and man- 
 ganese, with magnetic iron ore. The specific gravity of this wolfram was 
 6*938, and its analysis yielded tungstic acid 73.45, a substance having' 
 the characters of niobic acid 1.95, protoxyd of iron 9-05, protoxyd of 
 manganese, by difference, 15-35, silica 0-20 = 100*00. A particular 
 interest is attached to this mineral species, inasmuch as it is frequently 
 associated with the oxyd of tin, an ore which has not yet been found in 
 the Laurentian rocks. 
 
 MOLYBDENUM. 
 
 Molybdenite, or sulphuret of molybdenum, has been observed in small 
 quantities in a quartz vein at Terrace Cove on Lake Superior. It has 
 also been several times met with associated with pyroxene on Mud Lake, 
 
504 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 Moiyb- in the vicinity of Balsam Lake, in one case accompanied with copper 
 pyrites in quartz. It also occurs sparingly in flakes in a reddish gneiss at 
 St. Jerfone. The only locality hi which this mineral has been observed in 
 considerable quantity is at the mouth of the Quetachoo River, in Mani- 
 couagan Bay, on the north shore of the Gulf of St. Lawrence. Here, 
 in a bed of quartz six inches thick, in gneiss, molybdenite occurs in nodules 
 of from one to three niches in diameter, and in flakes, which are sometimes 
 twelve inches broad, and one fourth of an inch thick. 
 
 uranium. An ore of this rare metal is said to occur at Maimanse, where it 
 forms a vein about two niches in width, at the junction of the trap and 
 syenite. It was first described in 1847 by Dr. J. L. Leconte as a new 
 ore of uranium, under the name of coracite. It is amorphous, pitch-black 
 in color, with a grey streak, a resinous lustre, and a conchoidal fracture. 
 Its hardness is 3-0, and its density 4-38. According to Mr. J. D. Whit- 
 ney, who subsequently analysed it, it is distinguished from pitchblende 
 by its ready solubility in cold hydrochloric, acid, and contains oxyd of 
 uranium 59-30, lime 14-44, oxyd of lead 5-36, oxyd of iron 2-24, alu- 
 mina 0-90, silica 4-35, carbonic acid 7-47, water 4-64, with traces of 
 magnesia and manganese = 98-70. Mr. Whitney, with much probability, 
 suggests that the oxyd of lead, and a portion of the lime, are to be regarded 
 as combined with the sesquioxyd of uranium. 
 
 Uran-ochre, in the form of a sulphur-yellow crystalline crust, has been 
 observed lining fissures in the magnetic iron ore of Madoc. 
 
 CHROMIUM. 
 
 chromic The presence of oxyd of chromium has not yet been recognized in 
 the Laurentian or Huronian series, but it is very widely diffused among 
 the magnesian rocks of the Quebec group, the serpentines of which every- 
 where contain disseminated grains, nodules, and sometimes beds of chromic 
 ore. Grains and crystals of it are also met with in the dolomites and stea- 
 tites of this group. Workable beds of this ore are found in the townships of 
 Bolton, Ham, Melbourne, and at Mount Albert, in Gaspe*. The ore from 
 Bolton gave by analysis, oxyd of chromium 45-90, protoxyd of iron 35-68, 
 alumina 3-20, magnesia 15-03 = 99-81. Another specimen, from a 
 large boulder of chromic iron ore found near Lake Memphramagog, 
 yielded oxyd of chrome 49*75, protoxyd of iron 21-28, alumina 11*30, 
 magnesia 18-13 = 100-46. 
 
 Both of these specimens are remarkable for the large amount of mag- 
 nesia which they contain, since this element is sometimes entirely wanting 
 in chromic iron. The difference in the amount of alumina in the two ores 
 is another instance of the extremely variable composition of this mineral. 
 
CHAP. XVII.] MINERAL SPECIES. 505 
 
 When the chromiferous serpentines are decomposed by sulphuric acid, a cnromifer- 
 portion of oxyd of chromium is dissolved, while the separated silica gene- OU88ilicate8 - 
 rally contains grains of chromic iron, mixed with others of magnetite. In 
 some cases, however, the whole of the chromium in the mineral appears to 
 be in the state of a silicate. Traces of chromium are found not only in 
 the serpentines, but in the diallage, actinolite, and chlorite of the Quebec 
 group ; and the same element in larger quantity gives an emerald-green 
 color to a mica which is found in the magnesite of Sutton, and in crystals in 
 dolomite fromBolton and other localities (page 494). It also enters into 
 the composition of a purple kammererite or pyrosclerite, which is sometimes 
 mingled with the chromic iron ore of Bolton. The green chrome-garnet 
 from Orford has already been described (page 497). Oxyd of chromium, 
 in small amount, is found in an unknown state of combination in an impure 
 earthy unaltered limestone from Granby. 
 
 CERIUM. 
 
 Some small crystals of a mineral having the aspect of allanite cerium, 
 were found in a feldspathic rock near Bay St. Paul, and gave by analysis 
 a portion of oxyd of cerium with lanthanum. Minute crystals of a similar 
 mineral have been observed in a rock composed of labradorite and hyper- 
 sthene, from Lake St. John. 
 
 Ores containing arsenic are found in small quantities in several localities. Arsenic. 
 An arsenical ore from Michipicoten Island containing, besides nickel and 
 copper, from forty-seven to fifty-three per cent, of arsenic, is found by 
 several analyses to consist of a mixture, in variable proportions, of the 
 arseniurets of copper and nickel. Another ore from the Wallace Mine on 
 Lake Huron, contains, besides iron, nickel, and sulphur, six per cent, of 
 arsenic. Both of these will be described among the ores of nickel. 
 Arsenic, in the form of arseniate of cobalt, also occurs in rose-red incrusta- 
 tions on calcareous spar at Prince's Mine on Lake Superior. 
 
 Arsenical sulphuret of iron, or mispickel, which contains about forty-five Mispickei. 
 per cent, of arsenic, is found well crystallized with argentiferous galena 
 in a quartz vein on the Chaudidre in St. Francis ; and still more abund- 
 antly in small crystals, also with argentiferous galena, in a large vein of 
 quartz on Moulton Hill near Lennoxville. It is also said to occur at 
 Harvey's Hill in Leeds. 
 
 NICKEL AND COBALT. 
 
 These two metals are mentioned together because they are generally 
 associated in nature. They have been met with in many localities in ous py rite8 ' 
 Canada. A bed of quartz six or eight inches wide in the Laurentian 
 
506 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVII. 
 
 Cobalt. 
 
 gneiss on the eleventh concession of the seigniory of Daillebout, on the 
 river Assumption, contains a considerable amount of iron pyrites, which 
 yields to analysis 0.55 per cent, of oxyd of nickel, mixed with cobalt. A 
 similar iron pyrites, which occurs with pyritous copper in Escott, contains 
 small portions of cobalt and nickel ; but a more remarkable locality of 
 cobaltiferous iron pyrites is found in Elizabethtown near Brockville. 
 The pyrites, which is massive, brilliant, and in great abundance, yields to 
 analysis from 0*5 to 0-6 per cent, of oxyd of cobalt. Further details of 
 this deposit, and of the modes of extracting the cobalt, will be given in a 
 subsequent chapter. 
 
 Nickel. An ore of nickel from the Wallace Mine on Lake Huron consists in 
 
 great part of sulphur ets of iron and nickel, with a little arsenic, and is a 
 fine-grained steel-grey mixture, whose analysis, after deducting earthy 
 matters derived from the gangue, gave as follows for 100 parts : iron 41-79, 
 nickel 13-93, arsenic 6-02, sulphur 38-16, copper 0-10 = 100-00. A por- 
 tion of the iron is probably contained as oxyd in the gangue. The 
 nickel contains a few thousandths of cobalt. When exposed to moist 
 air, this ore becomes covered with an efflorescence of minute acicular 
 greenish-white crystals, which consist of nickel-vitriol, or hydrated 
 sulphate of nickel. 
 
 Two ores of nickel were discovered a few years since in a vein cutting 
 a bed of amygdaloid on Michipicoten Island. The first of these is a 
 
 Arseniuret brittle massive ore, associated with quartz, and having a brilliant metallic 
 lustre, and a color varying from tin-white to bronze yellow. Its hardness 
 is 5'0, and its specific gravity from 7 '35 to 7 '40. This mineral is 
 variable in composition. The results of four analyses were as follows : 
 
 I. 
 
 Arsenic, 31 -36 
 
 Copper, 44-70 
 
 Nickel,... 17-03 
 
 Silver, 
 
 99-09 100.28 
 
 Nickel 
 vitriol. 
 
 of nickel. 
 
 II. 
 
 III. 
 
 IV. 
 
 44-67 
 
 ..... 
 
 ... . 
 
 30-81 
 
 27-60 
 
 10-28 
 
 24-55 
 
 27-29 
 
 36-39 
 
 0-25 
 
 0-21 
 
 
 
 It would appear from calculation that these varying results are due to 
 mixtures of copper-nickel or nickeline, which consists of 44 '1 of nickel 
 and 55 9 of arsenic, with the arseniuret of copper, domeykite, which 
 contains 71 '7 of copper and 28-3 of arsenic. The nickel from this ore 
 contains traces of cobalt. 
 
 The second ore, said to be from the same mine as the preceding, occurs 
 as the gangue of native copper and native silver, which are scattered 
 through it in grains. The mineral is amorphous, greenish-yellow or apple- 
 green in color, with a waxy lustre and a conchoidal fracture. It is very 
 soft, polishing under the nail, and falling to pieces when immersed in 
 
CHAP. XVII.] MINERAL SPECIES. 507 
 
 water. It is decomposed by acids, and is found to be essentially a Silicate of 
 hydrated silicate of nickel. The analysis of one specimen dried at 212 P. nickel> 
 gave silica 33-60, oxyd of nickel 30-40, protoxyd of iron 2-25, lime 4-09, 
 magnesia 3-55, alumina 8-40, water 17*10 = 99-39. Another specimen 
 dried at a higher temperature, yielded silica 35 80, oxyd of nickel 32 20, . 
 water 12-20. It contains, besides, traces of cobalt and copper, and 
 appears to be identical with the nickel-gymnite of* Dr. Genth. A third 
 specimen, which contained small grains of the native metals disseminated, 
 gave silver 2 '55, copper 18 '51, and oxyd of nickel 20 '85. 
 
 The frequent occurrence of nickel in small quantities among the mag- 
 nesian rocks of the Quebec group has been already noticed. It is seldom 
 or never absent from the serpentines, steatites, diallages, and actinolites 
 of this series, but rarely forms more than two or three thousandths of 
 the mineral, in which it generally appears to be combined as a silicate. 
 With the chrome-garnet of Orford, the sulphuret of nickel (millerite) occurs smpimret 
 in small grains and prismatic crystals, disseminated through the mixture of ofnickel - 
 garnet and calcite in quantities which may become available. In the 
 magnesite of Sutton, it exists in very small quantities as a nickeliferous 
 pyrites ; and in that of Bolton it incrusts the fissures of the rock with a 
 green stain of what appears to be a hydrocarbonate. The proportion of 
 oxyd of nickel determined upon a large portion of the magnesite of Bolton 
 was found to be one thousandth. It was free from cobalt. The chromic 
 iron ore from Ham, however, gave on analysis 22 per cent, of oxyd of 
 nickel, hi which cobalt could be detected. The dolomites which are 
 associated with the serpentines of this altered series of rocks, often give 
 traces of nickel on analysis ; and it was found associated with oxyd of 
 chrome, in the earthy limestone from Granby already noticed. 
 
 MANGANESE. 
 
 The ores of manganese have as yet been met with only in small Earthy 
 quantities in Canada, and in the form of earthy hydrated peroxyd ox y dof 
 or wad, which occurs in various localities in alluvial deposits, often asso- 
 ciated with bog iron ore. Specimens of the bog manganese from Bolton 
 were much mingled with sand and pebbles, and contained but 26-5 per cent, 
 of pure peroxyd of manganese. An ore in reniform masses from Stanstead, 
 was more free from earthy matters than the last, but contained a large 
 amount of oxyd of iron, and gave 37-0 per cent, of peroxyd of manganese. 
 The bog iron ores from near St. Maurice sometimes contain several 
 hundredths of peroxyd of manganese, and the two ores occasionally 
 pass into each other by varying mixtures. The association of these 
 two metals in superficial deposits shows that oxyd of manganese is 
 capable of being dissolved and again precipitated, under conditions simi- 
 lar to the oxyd of iron, and probably by the intervention of organic matters. 
 
508 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 A film of peroxyd of manganese is often found incrnsting and cementing 
 sand and pebbles in alluvial deposits ; and the native gold in the valley of 
 the ChaudiSre is frequently discolored by a coating of the same oxyd. 
 carbonate In many of the rocks of the Eastern Townships, manganese exists in the 
 ^ orm f a protosalt, generally as carbonate. These rocks are distinguished 
 by weathering to a brownish-black. A ferruginous dolomite from Button, 
 contains more than seven per cent, of carbonate of manganese. The 
 bitter-spar which is met with in the quartz veins among the altered 
 slates of this region is sometimes manganesian, and some beds of the 
 green Sillery sandstones blacken exteriorly from the peroxydation of 
 a portion of manganese which they contain. It is doubtless from the 
 partial decomposition of such rocks that has been derived the manganese 
 to form the earthy ores already noticed. 
 
 In connection with the manganesian character of the rocks of the Eastern 
 Townships, it may be mentioned that beds of silicate of manganese, some- 
 tunes with the peroxyd, occur among the crystalline rocks of Vermont, and 
 that workable deposits of manganese ore are found with the hydrous iron 
 ores of that state. 
 
 IRON AND ITS OKES. 
 
 The native silicate of iron, lievrite, has already been noticed on page 
 465. Under the present head are included the carbonate of iron, the 
 magnetic oxyd, the anhydrous peroxyd, and the combinations of this last 
 with water and organic matters, constituting limonite and iron ochre : to 
 these must be added the sulphurets of iron. The native nickeliferous iron 
 fr m Madoc is also to be mentioned here ; although there is little doubt that, 
 like similar masses in other parts of the world, it is of extra-terrestrial origin, 
 and an aerolite. The specimen here noticed was found, in 1854, upon the 
 surface of a field, and weighed 370 pounds. Its shape is rudely rectangu- 
 lar, and flattened on one side. The surface is irregularly pitted, as is gener- 
 ally the case with meteoric masses, and coated with a film of oxyd of iron. 
 This iron is malleable, and highly crystalline in texture, and when etched 
 by an acid exhibits beautifully the peculiar markings which are known as 
 the Widmannstattian figures. Its analysis shows it to be an alloy of iron, 
 with 6-35 per cent, of nickel. Small portions of the phosphuret of nickel 
 and iron are disseminated through the iron, and, in making a section of it, 
 rounded masses of magnetic iron pyrites were met with. 
 
 CARBONATE OB 1 IRON. 
 
 The crystalline carbonate of iron, or spathic iron ore, is said to occur 
 with copper pyrites in quartz, on Echo Lake. A brownish cleavable spar 
 from Leeds, which has been called spathic iron, is a double carbonate of 
 lime and magnesia, with only a few hundredths of carbonate of iron. A 
 
CHAP. XVHJ MINERAL SPECIES. 509 
 
 similar admixture of iron characterizes most of the hitter-spar found in the carbonate 
 metalliferous veins of that region, as well as the dolomites and magnesites of iron - 
 of the Eastern Townships. An example of the occurrence of a large 
 proportion of carbonate of iron, is seen in the magnesite of Sutton (page 
 457), which thus exhibits a transition to spathic iron. This ore occurs in 
 beds, in the schistose rocks of Plymouth in Vermont. 
 
 The earthy argillaceous variety of carbonate of iron, which is known 
 as clay iron-stone, is found in considerable abundance in layers and nodules, 
 among the shales which are interstratified with the Gaspe* sandstones. 
 (See the section given on page 394.) 
 
 MAGNETIC OXYD OP IRO2T 
 
 This ore, to which the names of oxydulated iron, and magnetite, are Magnetic 
 often given, forms great beds among the Laurentian rocks, in Hull, iron ore - 
 Orenville, South Sherbrooke, South Crosby, Madoc, Belmont, and many 
 other localities. The occurrence of these has already been alluded to on 
 page 26, but a detailed description of these important deposits will be 
 reserved for a future chapter. The ore is sometimes disseminated in 
 grains through the Laurentian gneiss, but the great masses are generally 
 associated with the crystalline limestones. The magnetite of this region is 
 sometimes fine grained and compact, and at other times coarsely crystalline 
 and granular, but is rarely in crystals. Well defined cubes of magnetite, 
 with replaced edges, have, however, been found at the contact of the iron 
 ore with limestone, near Portage du Fort. The finely granular ore of Madoc 
 sometimes exhibits polarity, constituting a natural lodestone. The mag- 
 netite of the Laurentian rocks is generally very free from foreign matters. 
 Small portions of carbonate of lime, of mica, and more rarely of actinolite,, 
 are however occasionally disseminated through it, and, in some cases, 
 scales of graphite. 
 
 Magnetic ore is of frequent occurrence among the crystalline rocks of 
 the Eastern Townships, sometimes in octahedral crystals, which are 
 disseminated in chloritic slates ; or, as in Sutton, in a chloritic dolomite, 
 which contains large quantities of the carbonates of iron and manganese. 
 Beds of massive magnetic ore have been found in the same series, in 
 .Leeds, and in St, Francis, Beauce, where a large bed of ore in serpentine is 
 found to be a granular mixture of magnetite and ilmenite (p. 501). 
 
 SPEKOXYD OP IKON, OK RED HEMATITE. 
 
 This mineral, which is sometimes called oligist iron ore, and, in its p e roxyd of 
 different varieties, constitutes the specular, micaceous, and earthy red iron - 
 iron ores, is frequently found in the Laurentian system, though less 
 abundant than magnetite. It forms beds, as in McNab, or large irregular 
 masses arranged in the planes of stratification, as on Lake Nipissing. It 
 
510 GEOLOGY OF CANADA. [CHAP. XVII 
 
 Red is also found at Hudson's Wharf, on the Lac des Chats/ The ore in 
 
 tlte> these localities is compact or finely crystalline. Ore of a similar character 
 occurs in small beds in the Potsdam sandstone, in Bastard and Ramsay ; 
 and in little layers and nodules in the sandstone of the Sillery formation 
 near St. Nicholas. The peroxyd of iron is intermingled in considerable 
 proportion with the shales of this series, and gives to them their deep red 
 color. Beds of an impure fossiliferous peroxyd of iron occur among the 
 shales of the Clinton formation, near Hamilton; but, as in the Sillery 
 formation, the oxyd is mingled with the argillaceous sediments, and only 
 here and there accumulated in a comparatively pure state. 
 
 Among the altered rocks of the Eastern Townships, red hematite is of 
 frequent occurrence. Scales and crystalline plates of it are often dissemi- 
 nated in chloritic and epidotic rocks ; and a micaceous or foliated or mica- 
 ceous variety of the ore is sometimes found in veins of quartz, cutting 
 these rocks, as in the Pinnacle Mountain in St. Armand. Elsewhere it 
 occurs in tabular crystals, or thick plates, sometimes with feldspar, and at 
 others with copper-glance in bitter-spar, as in Leeds. 
 
 Micaceous Micaceous peroxyd of iron, mingled with variable quantities of quartz 
 and chlorite, form great beds of a schistose rock in this region. This rock 
 is what has else where, been named itabirite, or specular schist, and is in 
 some parts a rich ore of iron, while in other parts it passes into the ordi- 
 nary chloritic slates of the country. 
 
 HYDROUS PEROXYD OP IRON, OR HMONITE. 
 
 Brown This ore of iron, which is also known by the name of brown hematite, 
 
 includes the so-called bog-iron ore, and a large proportion of the iron 
 ochres which are found in great abundance in many localities, but espe- 
 cially in the St. Lawrence valley in Lower Canada, where it overlies the 
 superficial deposits of clay and sand, and generally holds a portion of these 
 ma tters in admixture. These bog ores or limonites moreover often contain 
 portions of oxyd of manganese and phosphoric acid ; besides a variable 
 amount of organic matter, which is still more abundant in the iron ochres. 
 The composition of the purer varieties of limonite corresponds to 85*6 
 of peroxyd of iron and 14- 4 of water, but the following analyses will show 
 the variations to be met with among the bog ores. The volatile portion 
 includes water and organic matter. I is an ore from Petite Cote, Vau- 
 dreuil ; II, a and 6, from Cote St. Charles, Vaudreuil ; III, from Upper 
 Rocky Point, Eardley ; IV, from Bastard, twentieth lot, second conces- 
 sion ; V, an ore used at the St. Maurice forges, and considered of the 
 best quality, with a bright reddish-brown color externally, and a brilliant 
 black fracture ; VI, from the same region, called by the workmen a rotten 
 ore ; VII, from the same vicinity as the last two, but dark colored from 
 the presence of manganese, and evolving chlorine when dissolved in hydro- 
 
CHAP. XVII.] 
 
 MINERAL SPECIES. 
 
 511 
 
 chloric acid. A portion of the silica in this last ore is chemically combined Bog iron 
 with the oxyd of iron, and separates in a gelatinous form from the hydro- ore- 
 chloric solution. 
 
 
 1 
 
 74 
 
 r. 
 
 50 
 
 Il'tf. 
 76-95 
 
 116. 
 
 III. 
 
 57-15 
 
 IV. 
 
 77-80 
 
 V. 
 77-60 
 30 
 
 VI. 
 
 74-30 
 traces. 
 
 VII. 
 
 64-80 
 5-50 
 
 Sesquioxyd of mangai 
 
 
 
 30 
 10 
 
 80 
 1-50 
 
 
 
 1-60 
 
 
 
 Silica 
 
 .... 7 
 
 5 
 1 
 19 
 
 43 
 52 
 
 70 
 
 21-60 
 
 1- 
 16- 
 
 76 
 61 
 50 
 
 5-40 
 
 1-81 
 17-25 
 
 3-60 
 
 1-80 
 22-20 
 
 4-80 
 undet. 
 23-65 
 
 
 
 
 ....18 
 
 95 
 
 19-80 
 
 18-85 
 
 
 
 100-85 99-05 
 
 99-20 96.67 102-36 101-90 98-75 
 
 It will be observed that in all of these ores the amount of volatile matter origin of 
 exceeds that of the water which the hydrated peroxyd should contain. 
 The iron in some of them exists in part as protoxyd, giving rise to an 
 excess in the analysis. This is evidently connected with the presence 
 of organic matters, whose power to reduce peroxyd of iron to the 
 condition of protoxyd is well known. . Waters charged with these 
 matters, the results of the decay of vegetable substances, permeate ferru- 
 ginous sediments and reduce the peroxyd of iron to the state of protoxyd ; 
 which is thus rendered soluble in water, and is brought to the surface 
 either as a carbonate of protoxyd, or, when organic matter is abundant, as a 
 combination of protoxyd of iron with some one of those organic matters 
 which have received the names of crenic, geic, and humic acids. These 
 protosalts of iron absorbing oxygen from the air, the metal is rendered 
 insoluble, and is precipitated from the solution of the carbonate as a hydra- 
 ted sesquioxyd, or, from the organic solution, as a compound of this oxyd 
 the vegetable acid. While the purer limonites are nothing more than 
 the hydrous sesquioxyd of iron, the bog ores consist of variable mixtures 
 of this with the organic compound, and some of the ochres about to be 
 described are probably this combination in a nearly pure state. 
 
 Extensive deposits of these ochres are found along the north side of the iron 
 river St. Lawrence, in the vicinity of the beds of bog ore, and also in achres - 
 Middlesex County. Pointe du Lac near Three Rivers, and Ste. Anne, steAnne. 
 Montmorenci, are remarkable localities of the ochre, and at the latter 
 place it is easy to observe it in the process of formation. Here, over 
 an area of four acres, is a deposit of ochre varying from four to seven- 
 teen feet in thickness, which is yellowish-brown at the surface, becoming 
 reddish or purplish-brown in those parts which are most exposed to air 
 and light. At a little distance below the surface, however, the ochre is 
 greenish in color ; and when recently dug up it is greenish-white, indica- 
 ting a compound of protoxyd of iron, which however grows yellowish, 
 from peroxydation, as the mass dries. Water oozes in a great many 
 places from the surface of the ochre, and collects in depressions. It is 
 
512 GEOLOGY OF CANADA, [CHAP. XVII, 
 
 at first colorless, transparent, and ferruginous to the taste, but by expo- 
 sure to the air soon lets fall a reddish-brown precipitate of ochre, and 
 becomes tasteless. As this precipitate is buried by subsequent accumula- 
 tions of the ochre, it is again reduced to a protoxyd, either by the reaction 
 of the organic matter which it contains, or by that derived from the 
 decaying roots and trees, which are abundant hi the deposit, and it 
 
 tion ofth ^ us assumes *he greenish c l r already noticed. A specimen of this 
 ochre. ochre was submitted to a chemical examination. It was pulverulent, 
 earthy, and of a light brownish-yellow. After being dried at 212 F., 
 it was gently crushed and sifted, to separate some few vegetable remains. 
 The ochre thus purified, when closely pressed into a crucible, covered, 
 and heated to redness, evolves inflammable gases, and leaves a black 
 mixture of metallic iron, with charcoal, which, when exposed to the air, 
 even after cooling, takes fire spontaneously, and is changed into red 
 oxyd of iron. When ignited in an open vessel, and carefully stirred to 
 promote oxydation, it lost in three experiments from 36-10 to 36-20 per cent. 
 of its weight. Hydrochloric acid dissolved the ochre, leaving 3- 6 per cent. 
 of silicious sand ; and on evaporating the solution, a farther portion of silica, 
 equalling 1-15 per cent, separated in a gelatinous state. The solution now 
 contained only traces of phosphates, and no other mineral impurities. 
 After adding tartaric acid and ammonia, the iron was thrown down as 
 sulphuret, and gave 59-10 per cent, of peroxyd. 100 parts of the ochre 
 thus yield peroxyd of iron 59-10, silica 4*75, water and organic matters 
 36-10 = 99-95. In order to ascertain the nature and the proportion of 
 the organic matters combined with the iron-oxyd, a portion of the ochre 
 organic was boiled, for half an hour, in a platinum vessel, with one half its weight 
 acids. O f hy(j ra te of potash and two or three parts of water. By this means the 
 organic matter Was dissolved, giving a deep brown liquid, from which acetic 
 acid threw down no precipitate. Acetate of copper now separated a dark 
 brown matter, which was regarded as apocrenate of copper, and equalled 
 2-21 per cent, of apocrenic acid. Carbonate of ammonia then gave a 
 slight white precipitate of crenate of copper ; but it was evident that the 
 greater part of the organic matter was present in some other form. It was 
 found that neutral acetate of lead precipitated it almost entirely from the 
 acetic solution as a dark brown compound with oxyd of lead ; a small ad- 
 ditional portion only being subsequently separated on the addition of 
 ammonia. The mixed lead precipitates, dried at 212 F., contained 36-6 
 per cent, of oxyd of lead, and indicated an amount of organic matter equal 
 to 16-16 per cent, the weight of the ochre. 
 
 The dried ochre, by exhaustion with a solution of caustic potash, lost 
 20-47 per cent, of its weight: another experiment gave 20-8. Deducting 
 from the mean of these, 1-15 of soluble silica, there remains 19-48 ; and as 
 this dissolved silica would also be mingled with the lead precipitate, it 
 
CHAP. XVII.] MINERAL SPECIES. 513 
 
 must be deducted from 16-16, leaving 15-01 per cent, for the organic 
 acids combined with the oxyd of lead. As these were wholly precipitated 
 with the oxyd of lead, it would appear that they exist in the ochre in a 
 higher state of hydratation than in the lead precipitate, so that the portion 
 dissolved out by potash consists of 15*01 of organic acids, as they exist in 
 the compound with oxyd of lead, and 4-47 of water = 19*48 ; giving for 
 the whole amount of water 21*14 per cent. The composition of the ochre 
 is therefore, peroxyd of iron 59*10, organic acids 15*01, water, by dif- 
 ference, 21*14, soluble silica 1*15, sand 3*60 = 100*00. 
 
 This compound of peroxyd of iron with water and organic acids is evi- 
 dently different from the hitherto described ores of iron, and should, 
 probably, constitute a distinct species. The bog iron ores containing 
 organic matter, may be regarded as variable mixtures of this organic salt 
 of peroxyd of iron with limonite. 
 
 The oxalate of iron, or oxalite, has been observed upon the black schists Oxaiite. 
 at Kettle Point in Bosanquet. It appears as a sulphur-yellow incrusta- 
 tion, which when heated on charcoal, before the blow-pipe, blackens and 
 becomes magnetic. 
 
 IRON PTRITES, 
 
 Under this head may be noticed the ordinary cubic sulphuret of iron, suiphureta 
 and the magnetic pyrites or pyrrhotine. The species marcasite, or white of iron - 
 iron pyrites, has not yet been recognized in Canada. 
 
 Cubic pyrites is often found in the Laurentian gneiss and limestones, cubic iron 
 but seldom in finely crystallized varieties. It is not unfrequently met 
 with in quartz veins in these rocks, often with massive foliated pyrrhotine, 
 and sometimes contains small portions of nickel and cobalt, as the pyrites 
 of Daillebout, of Escott, and that of Elizabethtown. The latter mass is 
 of great and unknown extent, forming apparently an irregular bed in the 
 crystalline rocks, and consists in part of a porous cellular variety with a 
 greenish tinge, and in part of a pure massive pyrites, almost tin-white 
 when recently fractured, but assuming a golden tarnish in the air. It is 
 the latter form of the pyrites from this locality, which, according to Mr. 
 Macfarlane's experiments, contains the greatest proportion of cobalt. 
 Localities of pyrites of some importance are indicated in the second lot of 
 the seventh range of Clarendon, also in the seigniory of Terrebonne, 
 where there is a vein four feet in width. Another vein, said to be forty 
 feet wide, occurs hi the Augmentation of Lanoraie. 
 
 Iron pyrites is of common occurrence in the rocks of the Huronian 
 series, and in the metalliferous veins of Lake Superior. It is also occa- 
 sionally found lining fissures hi the Lower Silurian limestones, and replacing 
 fossils, in the Utica formation. In the Quebec group, it forms concretionary 
 masses, often several inches in diameter, among the schists near Cape Rouge 
 
 HH 
 
514 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 and on the island of Orleans. In the Eastern Townships, iron pyrites is 
 sometimes associated with the ores of copper, as in Garthby ; where a great 
 bed, which occurs in serpentine, is in some parts mingled with copper 
 pyrites, and in others is nearly pure sulphuret of iron. 
 
 Magnetic Magnetic pyrites or pyrrhotine is found with cubic pyrites near 
 St. Jerome ; and, it is said, by Prof. Chapman, to be abundant near Balsam 
 Lake. It occurs in many other localities ; among which may be mentioned 
 St. Francis, Beauce, where it is found in a quartz vein with cubic pyrites, 
 mispickel, blende, and galena, and Barford, where it is associated with 
 copper pyrites, native copper, apatite, and mica, also in a vein of quartz. 
 
 suiphuret ^Q on ]y ore O f this metal yet observed in Canada is the sulphuret or 
 zinc blende. This occurs in some of the veins on Lake Superior, as at 
 Mamainse and at Prince's Mine, where it is abundant with copper-glance 
 and native silver. It has also been found in small quantities in veins of 
 calcite in the Laurentian rocks, in the county of Berthier, and at St. Ire'ne'e. 
 Among the rocks of the Quebec group, blende has been found dissem- 
 inated in dolomite in St. Armand, in Leeds, and in a quartz vein 
 in St. Francis, Beauce, with mispickel and argentiferous galena. It 
 occurs in like manner in small portions, with galena in calcite, at the Ram- 
 say lead mine. Blende is also occasionally met with in small masses of a 
 honey-yellow color, imbedded in the limestones of the Trenton group at 
 Kingston, Montreal, and Montmorency Falls, and in the dolomites of the 
 Niagara formation, in the west. At Niagara Falls, it sometimes appears 
 to replace fossils ; and at other times, occurs in beautiful wax-yellow 
 cleavable masses, imbedded in nodules of gypsum. 
 
 copper The ores of copper observed in Canada are copper pyrites, the varie- 
 
 gated sulphuret or erubescite,and the vitreous sulphuret or copper-glance, 
 besides native copper, and small portions of the blue and green carbonates, 
 and more rarely, of the red oxyd. In the rocks of the Laurentian series, 
 copper copper is frequently met with in the form of yellow sulphuret. Thus, in 
 pyrites. Escott, this ore is found in a bed with magnetic iron and with iron pyrites ; 
 and, according to Dr. Bigsby, variegated sulphuret of copper occurs 
 among the beds of magnetic iron ore on Crow Lake in Marmora. Small 
 veins and masses of very pure copper pyrites sometimes incrusted with 
 the blue carbonate, occur in the crystalline limestone in several localities 
 in the township of Burgess, and large rolled masses of copper pyrites have 
 been found on Gananoque Lake. In Bastard also, small portions of this ore 
 have been found in a vein with calcareous spar, and in similar conditions in 
 Fitzroy, and with blende in a vein in the Augmentation of Lanoraie. The 
 
CHAP. XVII.] MINERAL SPECIES. 515 
 
 great deposits of native copper in the trappean rocks of the north shore Native 
 of Lake Superior often present beautifully crystallized varieties, associated c PP er - 
 with calcite, prehnite, and laumontite, and sometimes with red oxyd of copper, 
 and with native silver. The veins intersecting these rocks also afford 
 copper pyrites, and the variegated and vitreous sulphurets of copper. 
 The copper-bearing veins which traverse the Huronian rocks on the north 
 side of Lake Huron, at the Bruce Mines and several adjacent localities, con- 
 tain, in a gangue of quartz, the yellow, variegated, and vitreous sulphu- 
 rets, generally massive, but in some cases crystallized, and occasionally 
 associated with heavy-spar, calcite, and pearl-spar. Besides the ores in 
 the veins, the yellow sulphuret is sometimes found in the beds, as at Root 
 River, where it occurs disseminated in a greenish argillite. The diorite 
 from White Fish Lake in like manner contains minute portions of copper 
 pyrites, with nickeliferous magnetic pyrites and magnetic iron ore. The 
 arseniuret of copper, domeykite, which occurs with nickeline on Michipi- 
 coten Island, has already been noticed on page 506. 
 
 The distribution of copper through the rocks of the Quebec group, is 
 very general, and seems to indicate that this metal was almost everywhere 
 present in the waters from which these strata were deposited. The copper 
 generally occurs in the form of one of the sulphuretted ores, but more 
 rarely in the native state, or as red oxyd, or green or blue carbonate. 
 The sulphurets are generally found in the beds in grains, plates, and 
 lenticular masses, sometimes of considerable size. Occasionally, as in a 
 portion of the Acton mine, the variegated and vitreous sulphurets form 
 the cement of a conglomerate rock, enclosing masses and grains of chert of c PP er - 
 and of limestone. The ores of copper are- not confined to any one 
 division of the rocks of the Quebec group. Sometimes, as at Acton and 
 Upton, they are in the dolomites, or, as in Ascot, in a chloritic limestone, 
 while in many other localities they are found in micaceous or chloritic 
 slates, or in steatite. Ores of copper are also disseminated in small 
 portions through the slaty iron ores of Brome and Sutton ; and small stains 
 and flakes of the green carbonate are found among the slates and 
 sandstones of the Quebec group, at Sillery and St. Nicholas. Red oxyd 
 of copper occurs in cinnabar-red stains upon blackish shales, at Acton. 
 
 Native copper has been found in thin plates imbedded in a greenish 
 layer running with the stratification, in the midst of a mass of red 
 slates, near St. Henri, in the bed of the Etchemin River. Masses of 
 native copper found in the rums of the red slates from Point LeVis, and 
 in the drift in the ChaudiSre valley, have probably had a similar source. 
 Small portions of native copper have also been met with in a bed of 
 amygdaloidal diorite, at St. Flavien. In the more altered portions of this 
 copper-bearing region, the ores of the metal are also found in veins. At 
 Acton, the dolomites are traversed by quartz veins, which contain only 
 
516 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 traces of copper ; but in Leeds and Inverness, great numbers of these 
 veins or courses are met with, which traverse the slates. They are seldom 
 continuous for great lengths, but often include large quantities of variegated 
 and vitreous sulphurets of copper, in a gangue of quartz and bitter-spar. 
 Near to Harvey's Hill, in Leeds, is a vein which traverses steatite, and 
 contains, in a gangue of bitter-spar, vitreous copper, with specular iron, and 
 native gold. In a quartz vein in Barford, copper pyrites and dendritic 
 native copper occur with apatite and mica. 
 
 LEAD. 
 
 suipnuret The only ore of lead met with in Canada is the sulphuret or galena. 
 This is found in many localities on Lake Superior, as at Prince's Mine, 
 Thunder Cape, and Pointe des Mines, where it occurs in small quantities in 
 veins, often associated with blende, and with iron and copper pyrites. 
 This galena sometimes contains a notable proportion of silver. Veins 
 holding galena are found in very many localities cutting the Laurentian 
 limestones, as in the townships of Bedford, Lansdowne, and Ramsay. The 
 gangue of the galena in these veins is calcareous spar, and more rarely 
 
 Ramsay, sulphate of barytes. Small portions both of blende and of copper pyrites 
 are associated with the lead at Ramsay. This vein traverses the dolomites 
 of the Calciferous formation, and, from its resemblance to those of Bedford, 
 and Lansdowne, which occur in the older Laurentian system, it is prob- 
 able that all of these latter are more recent than the Calciferous forma- 
 tion. At Bay St. Paul, small portions of galena are found in veins of 
 white calcite, mixed with green fluor-spar, which here traverse the rocks 
 of the Trenton group (page 161).* 
 
 Quebec Small quantities of galena have been found in the black calcareous 
 
 shales of the city of Quebec, in veins with white calcite and purple fluor- 
 spar. In various other parts of the Quebec group, galena has been met 
 with, sometimes disseminated in the dolomites, and at others forming small 
 layers or detached masses, generally granular in texture, and associated 
 with the ores of copper, as at Acton, Upton, and Ascot. So far as yet 
 
 Lennox- examined, these ores contain but little silver. More highly argentiferous 
 galena has, however, been found in small quantities in quartz veins, as 
 at the rapids of St. Francis on the Chaudiere, and at Moulton Hill near 
 Lennoxville ; in both cases with mispickel. A similar vein has been 
 observed in St. Annand, a little to the east of Cook's Corners. It runs 
 with the stratification, through the dolomitic limestone, and contains, 
 beside argentiferous galena, small portions of copper pyrites and blende. 
 The latter mineral is also disseminated in the adjacent limestone. Galena 
 occurs in workable quantities in veins which traverse the Gaspe' lime- 
 
 * On page 463, the fluor-spar of this locality is said, by advertence, to occur in veins 
 cutting the Potsdam sandstone. 
 
CHAP. XVII.] MINERAL SPECIES. 517 
 
 stones at Cape Gaspe* and Indian Cove (page 400). The dolomites of 
 the Niagara formation, throughout Western Canada, frequently contain 
 galena in disseminated grains and crystals, in small fissures of the rock, 
 often with pearl-spar, and sometimes associated with blende. For a de- 
 scription of one of these localities in the township of Clinton, see page 324. 
 
 Native silver occurs in small quantities at several of the copper locations Native 
 on Lake Superior, as St. Ignace and Michipicoten Islands, where it is 6ilver - 
 sometimes associated with copper-glance, and at other times with native 
 copper, the two metals being often soldered together, or the silver com- 
 pletely imbedded in the copper. At Prince's Mine, native silver has 
 been found in a vein of calcareous spar, with sulphuret of silver, copper- 
 glance, blende, and arseniate of cobalt. The quantity of sulphuret was 
 small ; but the native silver was disseminated in considerable abundance, 
 in small laminae, through the calcareous spar. It was however confined 
 to a mass of a few hundred weight, which yielded three and a half per cent, 
 of silver. The silver contained a portion of gold, equal to one part in 
 seven thousand. 
 
 The copper ores of the Eastern Townships frequently contain small por- 
 tions of silver. One thousand parts of copper reduced from a specimen of 
 the mixed variegated and vitreous sulphurets of Acton, yielded about two 
 parts of silver. Traces of silver were also found in the copper pyrites of 
 Upton ; and from 10,000 parts of copper reduced from the pyrites found 
 in a quartz bed on the seventeenth lot of the seventh range of Ascot, there 
 were obtained nine parts of silver and one and two-thirds parts of gold. 
 
 It is well known that the native sulphuret of lead is almost never free Argentifer- 
 from silver, which is sometimes present in so large a quantity as to consti- ous galenju 
 tute a silver ore. A vein which occurs at the rapids of the ChaudiSre in st - Francis - 
 St. Francis, Beauce, contains, in a gangue of quartz, argentiferous ga- 
 lena, blende, mispickel, besides cubic and magnetic pyrites, with minute 
 grains of native gold. A portion of galena from the assorted and washed 
 ore, which still retained an admixture of blende and pyrites, gave by 
 assay sixty-nine per cent of lead, and thirty-two ounces of silver to the 
 ton of 2240 pounds of ore. The assay of a second portion of the same 
 dressed sample gave, however, not less than 256 ounces of silver to the 
 ton. This result was probably due to the presence of a fragment of native 
 silver, or some rich silver ore among the dressed galena ; inasmuch as a 
 third assay, of another portion of the ore, more carefully dressed than 
 the first, yielded thirty-seven ounces of silver to the ton. The silver 
 from the cupellation of the reduced lead contained a little gold, and both 
 silver and gold were obtained from the blende and pyrites of the same 
 vein. 1000 grains of the pyrites, still mingled with a small portion of 
 
518 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 the other ores, were roasted, and then fused with litharge, borax, salt of 
 tartar, and metallic iron. The resulting button of lead gave by cupella- 
 tion 0-15 grains of an alloy of gold and silver. 700 grains of the blende 
 treated in the same manner, gave 0-19 grains of a similar alloy, of a pale 
 yellow color. The two precious metals seem thus to be generally dissemi- 
 nated throughout the ores of this vein. 
 
 Mouiton Hiii. The galena from Moulton Hill, mentioned above, was much mixed with 
 mispickel, even in selected specimens. A portion of the crushed and 
 washed ore gave by assay twenty-eight per cent of lead ; and this contain- 
 ed one part in 500 of silver, equal to sixty-five ounces to the ton of lead. 
 A galena which occurs at Meredith's location on Lake Superior, associated 
 with variegated copper ore, in calcareous spar with laumontite, yielded thirty 
 ounces of silver to the ton of reduced lead. 
 
 The other lead ores of the country, so far as examined, for the most 
 part contain but very small portions of silver. The galena of Bedford 
 yielded rather less than two ounces, that of Lansdowne an ounce and 
 a half, and that of Ramsay two and a half ounces of silver to the ton 
 of ore : subsequent trials gave less than two ounces. Specimens of ga- 
 lena from Bay St. Paul, Brome, Chateauguay, Fitzroy, from the North 
 Petite Nation River, and from near Toronto, have also been assayed, and 
 yield only traces of silver. A specimen of the galena from Acton gave 
 eighty-two per cent, of lead, containing two ounces of silver to the ton of 
 metal. The lead from the galena of Upton gave, in like manner, from 
 two to three ounces of silver to the ton. 
 
 The native gold of the Eastern Townships is always alloyed with a 
 certain portion of silver. 
 
 Mercury. The native gold obtained from the gravel of the Riviere du Loup is 
 often found to be covered with a white coating of mercurial amalgam, and 
 globules of running mercury are said to have been met with in washing 
 the auriferous sand of this region. It is not impossible that the presence 
 of the mercury here may be accidental ; but traces of this metal have been 
 observed in like manner with the native gold of Plymouth, in Vermont, 
 and a native amalgam of gold is found both in Columbia and Cali- 
 fornia. It may here be mentioned, that, according to Mr. Hautefeuille, the 
 native copper from one of the mines on the south shore of Lake Superior, 
 contains, besides a portion of silver, about one part in 4000 of mercury. 
 
 GOLD. 
 
 The existence of gold in the sands of the Chaudidre valley was first 
 made known by Lieutenant, now General, Baddeley, R. E., in 1835 
 [Am. Jour. Sci. (1), xxviii, p. 112] ; and within the last twelve years 
 
CHAP. XVII.] MINERAL SPECIES. 519 
 
 repeated examinations have shown that the precious metal is not confined Native 
 to that region, but exists in the superficial deposits of a wide region on gold> 
 the south side of the St. Lawrence, extending from the St. Francis to the 
 Etchemin rivers, and from the first line of hills on the north-west to the 
 province line on the south-east. The source of the gold appears to be the its source, 
 crystalline schists of the Notre Dame range ; and the materials derived 
 from their disintegration, not only constitute the superficial material 
 among the hills of this range, but are spread over a considerable area 
 to the south of them. These same gold-bearing rocks may be traced 
 south-westwardly, along the great Appalachian chain to the southern 
 United States, and are supposed to belong, for the most part, to the Quebec 
 group. Native gold has, however, been found in small grains with galena, 
 blende, and pyrites, in a well-defined quartz vein, cutting slates which are 
 supposed to be of Upper Silurian age, at the rapids of St. Francis, on 
 the Chaudiere. In Leeds, at Nutbrown's shaft, masses of native gold of Gold in 
 several pennyweights are found with copper-glance and specular iron ore, vems> 
 in a vein of bitter-spar ; and small grains of the metal have also been found 
 imbedded in the white garnet-rock described on page 496. These latter 
 localities belong to the rocks of the Quebec group ; but the precious metal 
 has rarely been found in place, and the working of it in Canada has been 
 confined to the superficial deposits of clay, sand, and gravel already men- 
 tioned. The occasional occurrence in these of pieces of gold partially im- 
 bedded in quartz, shows that it was derived, in part at least, from beds or 
 veins of this mineral, which are common among the talcoid slates of the 
 region. The observations among the gold-bearing rocks of the Southern 
 States seem to show, that the precious metal was originally deposited in 
 the beds of various sedimentary rocks, such as slates, quartzites, and lime- 
 stones, and that by a subsequent process it has been, in some instances, 
 accumulated in the veins which intersect these rocks. The formation 
 of these veins would seem, from the one above described at St. Francis, 
 to be subsequent to the Silurian period. The same considerations apply 
 to the copper and lead ores of the Eastern Townships. 
 
 The gold is found very generally disseminated throughout the diluvial 
 deposits over the region already designated in Canada, and is not confined goldl 
 to the river beds ; the action which distributed the gravel over the 
 surface being anterior to the formation of the present water-courses. 
 When, by the process of washing, the heavier portions of the auriferous 
 gravel have been brought together, they are found to contain abundance 
 of black ferruginous ores, consisting of magnetic iron, hematite, both 
 specular and compact, chromic iron and ilmenite, with occasional grains 
 of garnet, rutile, and more rarely zircon and corundum. The gold is in 
 grains, sometimes angular, but more often rounded, and varying in size 
 
520 GEOLOGY OP CANADA. [CHAP. XVII. 
 
 from masses of half a pound to a fine dust, which last is separated by 
 amalgamation from the black iron sand. 
 
 The gold thus obtained is alloyed with a portion of silver : a small mass 
 from St. Francis, Beauce, contained 13-27 per cent. The specific gravity 
 of five worn fragments of gold from the RiviSre du Loup was as follows : 
 15-76, 16-49, 16-65, 17-60, 17-77. The third specimen, after being 
 hammered into a thin plate, and annealed, had a specific gravity of 17-024, 
 and gave 13-60 per cent, of silver. The fifth, after a similar treatment, 
 acquired a specific gravity of 17-848, and gave 12-23 per cent, of silver. 
 A third specimen, in fine scales, had a density of 16-57, and contained 
 10*76 per cent, of silver. It would seem from the variations in specific 
 gravity, that these specimens of native gold were not homogeneous, but 
 were cavernous and held earthy impurities. An apparently pure frag- 
 ment, weighing 7*5 grammes, had a specific gravity of 15*76 ; but by 
 prolonged fusion with nitre and carbonate of soda, it lost 1*76 per cent, of 
 its weight, and acquired a specific gravity of 17-43. In the assays above 
 given, the gold was precipitated by oxalic acid from its solutions, which 
 contained, besides, only traces of copper and iron. The pure gold thus 
 separated, after fusion with nitre, had a specific gravity of 18-68-19-04, 
 as determined on two specimens. 
 
 Ferrugi- A portion of the gold-dust from the washings at the Riviere du Loup was 
 nd ' subjected to amalgamation, and left one third of its weight of black ferru- 
 ginous sand, of which eighteen per cent, were magnetic. The non-magnetic 
 portion was rendered soluble by the successive action of hydrochloric acid 
 and fused bisulphate of potash, leaving 4-8 per cent of silicious residue. 
 From the solutions, which contained iron and chromium, ebullition threw 
 down 23-15 per cent of titanic acid. The liquid was examined without 
 success for tin, uranium, cerium, and the rarer metals, which are sometimes 
 found in the auriferous gravel of other regions. The gold obtained by 
 the distillation of the amalgam lost 4-27 per cent of its weight by fusion 
 with borax, and the assay of the resulting ingot gave 12-87 per cent of 
 silver. This gold contained neither copper nor palladium, but a minute 
 traoe of platinum. 
 
 The presence of small portions of gold associated with silver in the cop- 
 per pyrites from Ascott, and with the native silver from Prince's Mine, 
 has been noticed on page 517. 
 
 PLATINUM AND ERIDO8MINE. 
 
 Platinum. Grains of native platinum have been found in smalj quantities among 
 the native gold of the Riviere du Loup, and also, it is said, in other locali- 
 ties in the same region. Associated with the platinum are small hard 
 steel-gray plates of a metal insoluble in aqua-regia, and having the char- 
 acters of iridosmme, the native alloy of osmium and iridium. 
 
CHIP. XVII.] MINERAL SPECIES. 521 
 
 CARBONACEOUS MINERALS. 
 
 Under the head of carbonaceous minerals may be mentioned the various 
 forms of liquid and solid bitumen, carburetted hydrogen gas, bituminous 
 shales, coal, and graphite. Of these, the latter species is common to the 
 Laurentian and the altered palaeozoic rocks, but the others are only met 
 in the unaltered palaeozoic strata. 
 
 BITUMENS. 
 
 Portions of hydrocarbonaceous matters, probably derived from organic Bitumen, 
 remains, are found from the base of the palaeozoic rocks in Canada, and 
 in many cases assume the form of bitumen. The presence of a bituminous 
 matter is evident in many of the limestones and dolomites of the Quebec 
 group, from the odor which these rocks evolve when heated, struck, or dis- 
 solved in acids. Its presence is still more strongly marked in the limestones 
 of the Trenton group, and indeed hi most of the palaeozoic limestones of 
 Canada. In many places it appears in the form of petroleum or mineral Petroleum, 
 oil. Thus, in the limestones of the Trenton group in Pakenham, the 
 cavities of large orthoceratites sometimes hold several ounces of it ; and it 
 is said to occur in similar conditions hi Lancaster. In the limestone 
 of the Birdseye formation, at the RiviSre a la Rose, Montmorenci, 
 petroleum exudes in drops from fossil corals. A petroleum spring rises 
 from the Utica formation on the Grand Manitoulin Island ; and Dr. Beck 
 has described a similar spring issuing from the Hudson River formation in 
 the township of Guilderland, near Albany in New York. But it is chiefly 
 in the higher formations that petroleum is met with in Canada. In the Gasps, 
 vicinity of Gaspe* Basin, it has been observed in several places rising from 
 strata of Devonian age. In describing these rocks on page 402, the 
 springs of petroleum on the St. John's River and on Silver Brook have 
 already been described, as well as the occurrence of the oil in the cavities 
 of an amygdaloidal greenstone dyke at Tar Point. Other localities of 
 petroleum have since been noticed in that vicinity, at the entrance to 
 Gasp Basin, and also near the north-east corner of the Douglastown 
 lagoon. About a mile and a half to the south-east of Gaspe* Basin, and on 
 the line of the northern anticlinal, is found a layer of mineral pitch or 
 dried bitumen, about an inch in thickness, lying beneath the surface of 
 vegetable mould, while the soil for some distance to the eastward is satu- 
 rated with petroleum. 
 
 The dolomites of the Niagara formation in the western basin are gener- 
 ally more or less bituminous: in some parts of western New York they are 
 said to contain so much solid bitumen, that it exudes from the rock when 
 this is heated. The limestone of the Corniferous formation is, in certain 
 portions, still more bituminous. The occurrence of petroleum in certain 
 
522 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 coralline beds in Bertie has been already noticed on page 378. Two oil- 
 tion< bearing beds are here visible, the one three and the other eight inches in 
 
 Bertie. thickness, while others were said to be concealed by the water in the quarry. 
 When the rock is recently broken, the oil is seen to be confined to the 
 cells of corals, which belong to the genera Heliophyllum and Favosites, 
 and make up a great part of the beds in question. The corals are sur- 
 
 Petroieum rounded bv a solid crystalline encrinal limestone, which is free from oil : 
 
 in corals, gf , ,1 r J "U .0, ^ -i J 
 
 but, as the limestone dries by exposure to the air, the oil spreads, and 
 colors the portions around the corals, giving rise to the appearance of a 
 continuous band of the dark oil-stained rock, which is limited both above 
 and below by the solid and Iigh1>colored limestone. This appears to be not 
 only destitute of petroleum, but impermeable to it. In some of the beds 
 were found large Heliophylli, where pores were open, but contained no 
 oil. A thin and continuous bed of JFavosites was white, porous, and desti- 
 tute of petroleum, while beds above and below were filled with it. One 
 of these, three inches in thickness, was seen to be twice interrupted in a 
 distance of a few feet, giving rise to the appearance of lenticular masses 
 of dark oil-stained coralline limestone, imbedded in the lighter colored and 
 compact rock. The surface of the latter may be readily wetted with 
 water, which runs off from the oily beds without moistening them. Where 
 these rocks are exposed in quarrying, the oil flows out, and may be col- 
 lected on the pools of water ; but its quantity does not seem to be consi- 
 derable. The beds of limestone are here somewhat inclined ; they are 
 very massive, and the oil-bearing layers show no disposition to separate 
 from the contiguous portions. 
 
 A similar coralline bed, impregnated with petroleum, and lying imme- 
 diately beneath a layer of chert, occurs a mile to the west of the village of 
 Jarvis ; and the quarries in the limestone of the Corniferous formation at 
 Gravelly Bay in Wainfleet, present petroleum under similar conditions to 
 those described in Bertie. In the township of Rainham, shells of Penta- 
 merus aratus, in the same limestone, are found, having an interior cavity 
 lined with crystals of calcite and filled with petroleum. 
 
 Asphaitum j n O t ner localities the bitumen in this formation is solid, and takes 
 the form of asphaltum or mineral pitch. On the sixth and seventh lots on 
 the south line of Kincardine is a quarry where about twenty feet of the 
 Corniferous limestone is exposed. The lower beds are yellowish-grey, mas- 
 sive, finely granular, fitted for building, and holding a few corals. In the 
 
 Kincardine. U pp er part of the section are thinner slaty beds, some of them of a dark 
 chocolate color, alternating with pale yellowish earthy layers. Specimens 
 from one thin bed in the upper part of the section contained no less than 
 12-8 per cent, of bitumen soluble in benzole. In others, which were much 
 less colored, the combustible matter, which gave a smoky flame when the 
 stone was placed on the fire, was in great part insoluble in the same liquid. 
 
CHAP. XVII.] MINERAL SPECIES. 523 
 
 A brown crystalline porous magnesian limestone from the Grand Mani- 
 toulin Island, had in like manner portions of asphaltum in its interstices, 
 and contained from 7*4 to 8-8 per cent, of soluble bitumen. 
 
 Petroleum occurs in conditions similar to those just mentioned in the 
 Devonian limestone of Ohio, and in the higher members of the Devonian 
 rocks in New York, where, according to Hall, there are found, both at the 
 base and the summit of the Hamilton, formation, septaria containing min- 
 eral oil. The overlying Devonian sandstones of the Portage and 
 Chemung group are very often impregnated with petroleum, and have long 
 been known to yield oil springs. It is in these sandstones, and in still ou weiis. 
 higher strata, that are found the oil wells of Pennsylvania and Ohio ; but 
 it seems probable that these, like the wells of Western Canada, have their 
 source in the oil-bearing Corniferous formation just described. The oil 
 springs of Enniskillen, and of the banks of the Thames, were known to 
 the Indians, and to the settlers of Western Canada, from a very early 
 period ; and since an economic use has been found for the petroleum, the 
 wells dug in these districts have afforded large quantities of it. 
 
 The districts yielding oil in Western Canada were made known by 
 natural oil springs, small quantities of petroleum being found floating 
 upon the surface of the water, or, as in Enniskillen, forming^ by its drying 
 up, beds of a tarry bitumen. On sinking through the clay, which in En- 
 niskillen covers the surface of the rock with a thickness of from forty to 
 sixty feet, a bed of gravel is generally met with, from which considerable 
 supplies of petroleum are obtained. These constitute what are called surface 
 wells ; but they are generally less productive in oil than those which are bored 
 in the older stratified rock beneath, and which are known as rock wells. 
 The relations of the oil springs and the reservoirs of oil to the anticlinals of 
 the rocky strata, are discussed on page 379. The areas within which 
 natural oil springs have been observed in Western Canada, besides the one 
 found on Grand Manitoulin Island, are four in number. Two of these are 
 in Enniskillen, one in the southern part of the township, on Oil Creek, 
 and another in the northern part. A third locality is in the townships of 
 Mosa and Oxford ; on the Thames, and a fourth on the Big Otter Creek 
 in Dereham, near Tilsonburg. Wells have been sunk in all these places ; Tiisonburg. 
 in the two former, with great success. In-Enniskillen, as already mentioned 
 on page 386, the shales of the Hamilton formation are found beneath the 
 clay ; while in Dereham, the Corniferous limestone is covered only by about 
 forty feet of drift clay. Further descriptions of these wells, and of the 
 mode of working them, will be given in a subsequent chapter. 
 
 The modifications which petroleum undergoes by exposure to the air, 
 are very instructive. Partly by volatilization, and partly by oxydation, it 
 becomes less fluid, and eventually is changed to a solid form. Thus, 
 near to Oil Creek, in Enniskillen, the thickened oil forms two layers, known 
 
524 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVII. 
 
 Thickened as gum beds, of a viscid tarry consistency, and covering together two or 
 petroleum. ^hree acres? -^h a thickness varying from a few inches to two feet. At 
 Petrolia, in the northern part of Enniskillen, in sinking a well near a 
 natural oil spring, a bed of mineral pitch or asphaltum, similar to that just 
 described, but more solid, was met with at a depth of ten feet in the clay, 
 and reposing upon a layer of gravel of four feet. This bed of bitumen 
 is from two to four inches in thickness, and is readily separable into thin 
 layers, which are so soft as to be flexible, and show upon their surfaces the 
 remains of leaves and insects, which had become imbedded in the bitumen 
 during its slow accumulation and solidification. It is mingled with a con- 
 siderable portion of earthy matter. This little deposit is instructive, as 
 showing the probable manner in which certain beds of bituminous rocks 
 may have been produced with the concurrence of previously formed 
 sources of petroleum. 
 
 Mineral In some instances the hardened bitumen is found in the cavities of the 
 
 bituminous rocks themselves. Thus, at Kincardine, a black, hard, bril- 
 liant form of mineral pitch occurs in small quantities in the fissures of the 
 bituminous limestones above described ; and at the quarries in Bertie already 
 noticed, a peculiar change is observed in the bitumen of the corals which 
 have been long exposed at the outcrop of the rock. It is converted 
 into a black matter, which lines the cells ; and it no longer repels water, like 
 the oily corals from within. Benzole, which readily dissolves the bitu- 
 men from these, does not affect the black color of the weathered corals, in 
 
 which the bitumen has evidently been converted into an insoluble modifica- 
 tion, as is shown by the following observations. A fragment of a Favosites 
 impregnated with this black matter, was crushed and treated with dilute 
 muriatic acid, which removed the carbonate of lime, and left five per cent, 
 of a brownish-black residue. . This, when exposed to heat, burned with 
 flame, without melting, and left a voluminous, coherent, coaly residue, 
 which gave a little ash. When treated with a large amount of boiling 
 benzole, the residue gave up only 16'5 per cent, of soluble bitumen; and the 
 subsequent analysis of the insoluble portion afforded volatile matter 28-1, 
 Altered bit- carbon 67*7, ash 4-2 = 100-00. From these results, it appears that the 
 umen. soluble and liquid bitumen of the corals had become in great degree replaced 
 by an insoluble, infusible carbonaceous matter, the result of the slow 
 oxydatton of the petroleum. It is probable that a less advanced stage in 
 the process would present the solid but soluble bitumens of Kincardine and 
 Grand Manitoulin. A black, brilliant carbonaceous matter, apparently 
 similar to that from Bertie, occurs at Cornwall, in the cells of a coral of the 
 Trenton group, the Oolumnaria alveolata. It has not however as yet been 
 chemically examined. 
 
 These observations serve to throw light upon the origin of a black 
 combustible coal-like matter, which occurs in many places in the Quebec 
 
CHAP. XVIL] MINERAL SPECIES. 525 
 
 group, and has in different localities been mistaken for coal. It was first 
 described by Vanuxem, in the Geology of New York, under the name of coai-iike 
 anthracite, as occurring in the Calciferous formation with crystals of bitter matter- 
 spar and quartz. It sometimes coats these crystals, or the walls of the 
 cavities, and at other times appears in the form of buttons or drops, evi- 
 dently, according to Mr. Vanuxem, having been introduced into these 
 cavities in a liquid state, and subsequently hardened hi a layer above the 
 crystals, showing, by its having conformed to them, that this coal-like mat- 
 ter was once in a plastic state. It is very pulverulent, brittle, of a shining 
 black, and according to Vanuxem yielded but a small amount of ash, and 
 11*5 per cent of volatile matter, which he regarded as consisting of 
 water. (Geology of New York, iii, 33.) 
 
 In the Quebec^ group in Canada, which is regarded as the equivalent of 
 the Calciferous formation, this substance has been observed at Quebec, Quebec group. 
 Orleans Island, Pointe L6vis, Sillery, St. Nicholas, Lotbinidre, Drummond- 
 ville, Acton, the vicinity of the Chatte River in Gasps', and many other 
 places. It fills veins and fissures in the limestones, shales, and sandstones, 
 and even in the trap rocks which traverse these. Sometimes it is found 
 in buttons or drops, as described by Vanuxem, forming botryoidal masses. 
 At other times it lines fissures, and is seen, as at Drummondville and at 
 Sillery, spread over a surface which had been previously encrusted with small 
 crystals of calcite. The shrinking of the layer has here given rise to cracks, 
 such as are sometimes seen in a coat of varnish. In other cases it fills 
 fissures several inches in diameter ; so that it has been mistaken for coal, 
 and attempts have been made to work it at Quebec and elsewhere. The 
 mineral is never, however, in true beds like coal, but is always confined to 
 veins and fissures which cut the strata ; showing its deposition to have been 
 posterior to the formation of the rocks. Near to the camp, on the western Orleans 
 portion of the island of Orleans, there is a considerable vein of it in the shales, Island * 
 from which several hundredweights might be easily obtained. At St. Flavien st. Fiavien. 
 in Lotbini^re there occurs, in the copper-bearing slates, a vein of it an 
 inch or two in width. The walls of the vein are lined with quartz, and the 
 coaly matter is itself cut by thin veins of quartz, of later formation. In another 
 specimen from this locality, the vein is nearly filled with crystalline quartz, 
 and the bituminous matter is in small almond-shaped masses in the 
 centre of the vein. At Acton it fills irregular cracks and fissures, and Acton, 
 sometimes forms masses of several inches in diameter. This matter is of 
 a shining black color, very brittle, breaking into irregular fragments with 
 a conchoidal fracture. It is easily pulverized, giving a very black powder, 
 and flies to pieces when heated. It varies considerably in its chemical 
 characters. The mineral from Acton is much harder than from the other 
 localities mentioned. When heated to redness in a close vessel, it gives off 
 a portion of water, but no inflammable gas or vapor, and loses 6*9 per cent. 
 
526 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 of its weight; leaving a carbon which is difficult of combustion, and gives when 
 incinerated 2*2 parts of ash. Like the specimens described by Vanuxem, it 
 approaches to anthracite in its characters. That from the other localities 
 examined, gives off, when heated, a greater or less proportion of combus- 
 tible vapor, which condenses in part into a tarry liquid. Carefully selected 
 specimens yield after incineration only a few thousandths of ash, appa- 
 rently due to accidental impurities. In a specimen from the Mountain Hill, 
 Quebec, the volatile matter equalled 19'5 per cent. ; that from the Island 
 of Orleans, 21-0; that of St. Flavien, 15' 8 ; and from another locality, 
 six miles from this, 24' 5 per cent. The latter, when exposed to heat, swells 
 up, and leaves a porous coke, the fragments adhering like a caking 
 coal. The same thing is observed, to a less extent, with the specimens 
 from Orleans Island. These carbonaceous matters are insoluble in ben- 
 zole, with the exception of that last mentioned, which appears to contain a 
 small amount of soluble bitumen. The resemblance of this substance to 
 the altered insoluble bitumen from the Devonian corals at Bertie, taken in 
 connection with the evidences that it was once in a liquid state, are such that 
 it can scarcely be doubted that the coaly matters of the Quebec group 
 have resulted from the slow alteration of liquid bitumen in the fissures of 
 the strata. This is the more probably as the magnesian limestones of the 
 Quebec group at Point Levis are still distinctly bituminous. 
 
 The chert beds among the Upper Copper-bearing rocks of Lake Superior, 
 which are supposed to be the equivalents of the Quebec group, contain 
 small portions of a black anthracitic matter, filling fissures, and apparently 
 identical with the material just described (p. 68). A carbonaceous mat- 
 ter, not unlike this, has been described by Durocher as occurring in 
 Sweden, among crystalline rocks which are not improbably of the same 
 age as those of the Quebec group. 
 
 origin of As * * ne origin of bitumens, it has been by some supposed that they 
 bitumens. nave na( j their origin in the action of heat on coal and similar organic 
 matters, which by a slow distillation have yielded these oily matters, that 
 have been condensed in the overlying strata. To this is to be objected 
 the fact that bitumens occur in rocks in which there is no evidence of the 
 action of heat ; and moreover, that, from the distribution of the bitumen, 
 as at Bertie, it is clear that it has not been brought into its present posi- 
 tion by distillation, but has been generated in the porous beds where it is 
 now found. This conclusion is in accordance with that of Mr. Wall, from 
 his researches in Trinidad. The bitumen of that region, which belongs to 
 the newer Tertiary rocks, and is associated with beds of lignite, is confined 
 to particular strata which once contained vegetable remains. These, ac- 
 cording to him, have undergone " a special mineralization, producing a bitu- 
 minous matter instead of coal or lignite." This operation is not attributable 
 to heat, nor of the nature of a distillation, but is due to chemical reactions 
 
CHAP. XVII.] MINERAL SPECIES. 527 
 
 at the ordinary temperature, arid under the normal conditions of climate." 
 (Proc. Geol. Society of London, May 1860.) 
 
 In the palaeozoic rocks of North America, the organic matter which has 
 yielded the bitumen, must be derived either from a marine vegetation, or 
 from the remains of marine animals. These, especially the lower forms, palaeozoic 
 differ but little in elementary composition from plants, and may as bltumen8 - 
 readily yield bitumen by their change. The transformation by which or- 
 ganic matters may be converted into bitumen, does not differ very greatly 
 from that which produces the more bituminous coals, to some of which 
 indeed, certain of the asphaltums approach very closely in composition. 
 The true petroleums retain a larger proportion of hydrogen, and result from 
 a change, under conditions as yet but imperfectly understood, by which a 
 greater proportion of hydrogen is retained in combination. The diverse 
 results of the fermentation of sugar under varying conditions, suggest analo- 
 gies to the different transformations of vegetable and animal tissues which 
 have resulted in the formation of lignite, coal, anthracite, asphaltum, and 
 petroleum, together with carbonic acid and gaseous hydrocarbons as acces- 
 sory products. 
 
 While a vegetable origin is assigned to the bitumen of more recent 
 geological formations, it is probable, that, although a marine vegetation may 
 have in some degree contributed to the formation of the bitumen of the 
 palaeozoic strata ; an accumulation of molluscous animals in certain strata 
 may have given rise, by a sub-aqueous decomposition, to the petroleum which 
 is now found in these rocks. The small amount of organic matter which 
 the corals contain, would, in itself, be altogether inadequate to the produc- 
 tion of the quantity of oil which is found associated with them ; so that 
 other organic bodies, which have left no solid skeletons, must have furnished 
 by far the greater part of the petroleum of these palaeozoic limestones. 
 
 The light carburetted hydrogen or marsh-gas, which is so often a pro- Marsh-gas, 
 duct of the transformation of organic matters at ordinary temperatures, is 
 abundant in the palaeozoic rocks of Canada, and issues from many mineral 
 springs. Those of Caledonia, Varennes, and Caxton, in the Lower Silu- 
 rian series, give off great volumes of this gas, which keep the waters in con- 
 stant agitation. Many other less important instances of the same kind 
 might be mentioned ; while in the higher strata of Western Canada, this 
 gas is still more abundant, as at the well-known burning-spring near Nia- 
 gara Falls, and in the region of the oil wells. In boring these, reservoirs 
 of it are frequently penetrated, from which the gas is liberated with 
 explosive violence. In nearly all the oil wells there is a greater or less 
 disengagement of inflammable gas ; so that it would appear that the strata 
 almost everywhere in that region hold, in a condensed state, portions of 
 light carburetted hydrogen, which is discharged wherever a natural fissure 
 or an artificial boring furnishes a vent. 
 
528 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 BITUMINOUS SHALES, OB PYKOSCHI8T8. 
 
 Bituminous The epithet bituminous is commonly applied not only to rocks like those 
 of Bertie, Kincardine, and the Grand Manitoulin, which contain ready- 
 formed bitumen, but to coals, shales, and similar matters, which when strong- 
 ly heated suffer decomposition and give off volatile oily hydrocarbons. These 
 bodies, which closely resemble bitumen in composition and properties, do 
 not exist ready formed in the coals and shales, but, like the similar oily 
 matters obtained by destructive distillation from lignite, peat, and even 
 from wood, are products of decomposition. The black inflammable 
 shales which belong to the Coal formation, and to many lower and higher 
 geological horizons, are of this character, and owe their combustibility, and 
 their property of yielding oily hydrocarbons by distillation, to an admixture 
 
 pyroschists. of a substance allied in composition to coal or lignite. The German name 
 of brandscheifer, which may be translated by pyroschist,* may serve to 
 distinguish these inflammable shales from others, which, like the slaty lime- 
 stone of Kincardine, contain ready-formed bitumen. Pyroschists occur in 
 at least two horizons in Canada. They form the black shales of the base of 
 the Portage and Chemung group of the Devonian series, and those of 
 . the Utica formation of the Lower Silurian. These latter contain very 
 variable amounts of combustible matter ; and they give when distilled, besides 
 inflammable gases, portions of oily matter, which, in the shales of Colling- 
 wood, the richest yet examined, are equal to four or five per cent. The 
 Devonian shales of Kettle Point, in Bosanquet, in the same manner yielded, 
 by experiments on a small scale, 4*2 per cent, of crude oil, together with a 
 portion of ammoniacal water. 
 
 It is probable that some of the strata of the Quebec group, as well as 
 the black shales at its base (page 234), are pyroschists ; for the altered 
 rocks of this series are in many places very carbonaceous, and contain an 
 admixture of plumbago. 
 
 COAL. 
 
 Coal The black bituminous shales or pyroschists of the Portage and Che- 
 
 mung group contain the remains of terrestrial plants, including a species 
 of Calamites, the flattened stems of which are sometimes found to be con- 
 verted into coal (page 388). The higher portions of the Devonian series 
 in Gaspe*, abound, in some portions, with similar remains of carbonized 
 plants ; and in the lower part of the Gaspe* sandstones there is a well- 
 defined seam of coal, with carbonaceous shale, measuring together three 
 inches, and having beneath it a bed of clay holding the roots of plants. 
 The section of these sandstones, given on page 394, shows that a terres- 
 
 * This compound word is completely analogous to the name of pyrorthite, given by 
 Berzelius to a variety of orthite containing an admixture of combustible matter. 
 
CHAP. XVII.] MINERAL SPECIES. 529 
 
 trial vegetation prevailed throughout the whole series, jet in no other part 
 of the thickness of 7000 feet was there observed a distinct coal seam. 
 The same Upper Devonian strata, in the state of New York, contain, in 
 like manner, thin seams of coal, which are of no economic importance. 
 The rocks of the Bonaventure formation in Gaspe* (page 405) , the only 
 representatives in Canada of the true coal-bearing series, have afforded 
 nothing but a few carbonized plants. 
 
 PLUMBAGO OK GRAPHITE. 
 
 Plumbago occurs in the altered rocks of the base of the palaeozoic series, pi um bago 
 in the Eastern Townships, generally finely disseminated in calcareous or 
 argillaceous shales, rendering them soft, unctuous, black, and shining; but 
 it has nowhere been found among them in sufficient quantity to be of eco- 
 nomic value. Examples of these plumbaginous slates are to be seen, 
 among other localities, in Granby, Melbourne, and St. Henry ; in the 
 latter place enclosing graptolites. The altered Devonian limestones of 
 Owl's Head are also plumbaginous. The plumbago which is found in 
 Massachusetts, in the continuation of this metamorphic region, is well Metamor- 
 known to belong to more recent rocks, and to be, in fact, the coal of the pbic origiB 
 Carboniferous system in an altered condition. The principal deposits of 
 plumbago in Canada, however, belong to the Laurentian series, and by 
 analogy suggest the existence of great accumulations of organic matters 
 in the sediments of that remote period. 
 
 The plumbago of the Laurentian rocks generally occurs in beds or seams 
 of from a few inches to two or three feet in thickness. These are often 8eries - 
 interrupted, giving rise to lenticular masses, which are sometimes nearly 
 pure, and at other times mingled with carbonate of lime, pyroxene, and 
 other foreign minerals. These deposits of plumbago generally occur in 
 the limestones, or in their immediate vicinity, and granular varieties of 
 this rock often contain large crystalline plates of plumbago. At other 
 times, this mineral is so finely disseminated as to give a bluish-grey color 
 to the limestone, and the distribution of bands thus colored serves to mark 
 the stratification of the rock. Workable deposits of plumbago occur in 
 the townships of Burgess, Lochaber, and Grenville. In one locality 
 in the latter township, it is associated with sphene, zircon, pyroxene, 
 and tabular-spar. 
 
 The plumbago of the Laurentian series is, however, not confined to the 
 limestones. Large crystalline scales of it are occasionally disseminated in 
 pyroxene rock, in pyrallolite, and sometimes in quartzite and in feldspathic 
 rocks, or even in magnetic oxyd of iron, as at the Hull ore bed. A 
 description of those localities of plumbago which are of economic impor- 
 tance will be given in another chapter. 
 
 II 
 
530 GEOLOGY OF CANADA. [CHAP. XVII. 
 
 sulphur. Native sulphur is of rare occurrence in Canada. In some countries it 
 is found in abundance associated with gypsum, and it is met with in small 
 quantities in the gypsum of the Onondaga formation in New York, although 
 it has not yet been seen in this position in Canada. The numerous springs 
 impregnated with sulphuretted hydrogen in Western Canada, however, 
 often give rise to deposits of sulphur, which encrusts the objects over 
 which the water flows. This is well seen at the Charlotte ville sulphur 
 spring. In some other localities, small accumulations of sulphur are 
 found, which probably owe their origin to the action of similar springs. 
 In the township of Clinton there is a deposit of this kind, which is said to 
 be found at the surface of the ground, and affords masses of pure yellow 
 compact or fine-grained sulphur, cavities in which are lined with small 
 transparent crystals of sulphur. Dr. Bigsby has described native sulphur 
 in a pulverulent form, and in minute crystals, coating the calcareous shales 
 at the foot of Niagara Falls, on both sides of the river. Here also, as 
 sulphurous springs are not uncommon in these rocks, it is probable that, as 
 at Charlotte ville, the sulphur is derived from the decomposition of sulphu- 
 retted hydrogen gas. 
 
CHAP. XVIIL] WATERS OP MINERAL SPRINGS. 531 
 
 CHAPTER XVIIL 
 
 WATERS OF MINERAL SPRINGS AND OF RIVERS. 
 
 MINERAL WATERS OF CANADA; THEIR DIVISION INTO six CLASSES. ALPHABETICAI, LIST 
 OF MINERAL SPRINGS. TABLES OF ANALYSES OF WATERS, OBSERVATIONS ON THEIR 
 CHEMICAL COMPOSITION; [SALTS OF POTASH AND SODA; SALTS OF LIME AND MAGNESIA; 
 BARTTA AND 8TRONTIA; IRON, MANGANESE, AND ALUMINA; CHLOHIDS, BROMID8, AND 
 IODID8; SULPHATES, SULPHURET8, AND SULPHURIC ACID; ALKALINE AND EARTHY 
 CARBONATES; SILICA AND SILICATES; BORATES AND PHOSPHATES; ORGANIC MATTERS. 
 GEOLOGICAL DISTRIBUTION OF MINERAL SPRINGS. WATERS OF THE ST. LAWRENCE 
 AND OTTAWA RIVERS. 
 
 The unaltered palaeozoic rocks of Canada abound in mineral springs, a 
 great number of which have been submitted to chemical analysis. It is 
 proposed in the present chapter to notice, in alphabetical order, such 
 springs as have been examined,* giving, in some cases, the results of their 
 chemical examination, but reserving most of the analyses for a series of 
 tables at the end of the list, which will serve to show the comparative 
 composition of the principal mineral springs. After this, the chemical 
 and geological history of these waters will be considered more at length. 
 The result of some examinations of the waters of the St. Lawrence and 
 Ottawa rivers will be appended to the chapter. 
 
 The mineral waters of Canada may for convenience be arranged in ciassmca- 
 six classes, according to their chemical composition. In the first three tion * 
 classes chlorids predominate ; in the fourth, carbonates ; and in the fifth 
 and sixth, sulphuric acid and sulphates. The waters of the first, second, 
 and sixth classes are neutral ; those of the third and fourth are alkaline ; 
 and those of the fifth are acid. 
 
 The first class includes saline waters containing chlorid of sodium, with First class, 
 large portions of chlorids of calcium and magnesium, sometimes with 
 sulphates. The carbonates of lime and magnesia are either present only in 
 very small quantities, or are altogether wanting. These waters are generally 
 very bitter to the taste, and always contain portions of bromids and iodids. 
 Examples, St. Catherines, Ancaster, Whitby, Hallo well. 
 
 * In many cases, the springs not having been visited by the officers of the Geological 
 Survey, the locality is given on the authority of the person collecting the water. 
 
532 GEOLOGY OF CANADA. [CHAP. XVIII. 
 
 second The second class includes a large number of saline waters, which differ 
 
 from the first in containing, besides the chlorids of sodium, calcium, and 
 magnesium, considerable portions of bicarbonates of lime and magnesia, the 
 latter carbonate generally predominating. Small quantities of oxyd of iron, 
 and of baryta and strontia, are frequently present. These waters generally 
 contain much smaller proportions of earthy chlorids than the first class, and 
 are therefore less bitter, and more pleasant to the taste. Examples, 
 Plantagenet, St. L6on, Ste. Genevive. 
 
 nurd class. The third class includes those saline waters which contain, besides chlorid 
 of sodium, a portion of carbonate of soda, with bicarbonates of lime and 
 magnesia. Small amounts of baryta, strontia, and of boracic and phosphoric 
 acids, are often present in these waters, and bromids and iodids are very 
 rarely wanting. Examples, Caledonia, Varennes, Fitzroy. 
 
 Fourth The waters of the fourth class differ from the last in containing but a 
 
 small proportion of chlorid of sodium, while the carbonate of soda predom- 
 inates. These waters generally contain a much smaller amount of solid 
 matters than those of the previous classes, and have not a very marked 
 taste until evaporated to a small volume, when they are found to be strongly 
 alkaline. Examples, Chambly, St. Ours. 
 
 Fifth class. ^he fifth class includes acid waters, which are remarkable for containing 
 a large proportion of free sulphuric acid, with sulphates of lime, magnesia, 
 protoxyd of iron, and alumina. These springs, which are few in number, 
 and characterized by their acid styptic taste, generally contain some sul- 
 phuretted hydrogen. Examples, Tuscarora and Niagara. 
 
 Sixth class. ^ n the sixth class may be included some neutral saline waters in which 
 the sulphates of lime, magnesia, and the alkalies predominate, chlorids' 
 being present only in small amounts. To this class belongs a mineral 
 water from Hamilton, and another from Charlotte ville. 
 
 ALFRED. 
 
 The water of a saline spring, said to occur on the ninth lot of the tenth 
 range of Alfred, belongs to the second class, and contains 14-5 parts of 
 solid matter in 1000. It rises from the Lower Silurian limestones.* 
 
 On the tenth lot of the sixth range of Alfred, two mineral springs 
 are said to occur, both of which yield saline and somewhat alkaline waters 
 of the third class, containing a small proportion of sulphates. The speci- 
 mens examined were mingled with surface water. 
 
 * By the Lower Silurian limestones, in this chapter, are to be understood those of the 
 Trenton group, and of the Chazy and Calciferous formations, excluding the rocks of the 
 Quebec group, which in certain districts represent the Calciferous formation, and also 
 give rise to mineral springs. 
 
CHAP. XVIII.J WATERS OF MINERAL SPRINGS. 
 
 ANCASTER. 
 
 The water of a salt well about two miles east of the village of Ancaster 
 belongs to the first class. An attempt was formerly made to manufacture 
 common salt from it ; but from the large amount of earthy chlorids, the purifi- 
 cation of the salt was found to be difficult. For its analysis, see Table I, 1. 
 
 A sulphurous water belonging to the second class occurs about a mile 
 and three quarters north-west of the village of Ancaster. When examined 
 in 1847, the water had a specific gravity of 1005 '2, and, besides the 
 ingredients mentioned in the analysis below, contained a small portion of 
 bromine. The amount of sulphuretted hydrogen was found equal to only 
 0*4 of a cubic inch in 100 cubic inches of water. The water appeared 
 to be slightly thermal, inasmuch as its temperature was 50 F., while an 
 adjacent fresh-water spring was only 48 F. The water of this spring 
 was analyzed in 1854, by the late Dr. George Wilson, of Edinburgh, 
 and gave for 1000 parts, as follows : 
 
 Chlorid of sodium, 3-5476 
 
 " potassium, -0052 
 
 " calcium, 1-3528 
 
 " magnesium, -4190 
 
 Sulphate of lime, -6500 
 
 Carbonate of lime, -2035 
 
 " magnesia, -0160 
 
 " iron, -0274 
 
 Silica, , -0097 
 
 Organic matters, phosphoric acid, alumina, and 
 
 iodine, traces. 
 
 6-2312 
 
 The carbonates exist in the water as bicarbonates. The sulphuretted 
 hydrogen was, by Dr. Wilson, found equal to 5 6 cubic inches in 100 cubic 
 inches of the water; which, as will be seen above, is a much larger quantity 
 than existed in the water examined at the spring in 1847. As however 
 sulphuretted hydrogen is generated when water containing sulphates 
 with organic matter, is preserved in close vessels in warm weather, the 
 large amount of this gas found by Dr. Wilson is not surprising. These 
 two waters issue from rocks of the Niagara formation. 
 
 ASSUMPTION. 
 
 In the range of Assumption, called Point-du-Jour, is a saline mineral Assumption, 
 water of the second class, known as the Aurora Spring. It contains 7-36 
 parts of solid matter in 100.0, including small portions of strontia. The 
 spring disengages large volumes of carburetted hydrogen gas, and 
 probably rises from the Lower Silurian limestones. 
 
534 GEOLOGY OP CANADA. [CHAP. XVIII. 
 
 BAIE DTI FEBVBB. 
 
 Bale du Several springs are known to exist in this seigniory, four of which have 
 
 been examined. Of these, two are waters of the second class, both contain- 
 ing strontia. One of them, on the land of Antoine Loizeau, near the line 
 of Nicolet, in the Grand Range, contains 5-44 parts of solid matter in 
 1000, and 4-54 parts of alkaline chlorids, of which 2-0 per cent, are chlorid of 
 potassium. The other, in the same range, is on the land of Mr. Lefort, 
 about a mile above St. Antoine church. It is more saline than the last, 
 yielding 15-94 parts of solid matter to 1000, and contains a little boracic 
 acid. Two other springs to be noticed, belong to the third class, both of 
 which give off bubbles of carburetted hydrogen gas, and contain small por- 
 tions of strontia. One of these is on the land of David Houle*, adjoining 
 that of Antoine Loizeau above-mentioned, and contains 4-96 parts of solid 
 matter in 1000. The other is on the land of Ignace CourchSne, about 
 half a league east of the church. For its analysis, see Table III, 7. The 
 chlorid of potassium in this water equalled 0*92 per cent, of the chlorids. 
 All of these waters probably rise from the Hudson River formation. 
 
 BAY ST. PAUL. 
 
 Bay st. A very bitter saline spring from the Lower Silurian limestones at Bay 
 
 St. Paul, contains 20-68 parts of solid matter in 1000, and is to be 
 referred to the first class. Several other mineral springs in the same 
 vicinity contain only insignificant amounts of saline ingredients, and are at 
 the same time feebly sulphurous. One of a similar kind, but more sulphur- 
 ous, from Les Eboulemens, gave 0*42 of a cubic inch of sulphuretted 
 hydrogen to 100 cubic inches of the water, and contained 0-70 parts of 
 solid matter in 1000. 
 
 BELCEIL. 
 
 A saline water, said to come from the seigniory of Beloeil, belongs to the 
 third class, and contains a notable proportion of strontia, besides undeter- 
 mined amounts of iodids and bromids. It rises from the Hudson River 
 formation. For its analysis, see Table III, 8. 
 
 BERTHIEK. 
 
 Berthier. A copious saline spring of the second class occurs on the land of Charles 
 Boucher, on the Bayonne, a league above the church of Berthier, and prob- 
 ably belongs to the Lower Silurian limestones. For its analysis, see Table 
 II, 9. A spring regarded as chalybeate, near the manor-house at Ber- 
 thier, contains a feeble proportion of iron, with earthy carbonates. 
 
CHAP. XVIIL] WATERS OF MINERAL SPRINGS. 535 
 
 BRAMPTON. 
 
 A reputed mineral spring in the village of Brampton was found to con- Brampton. 
 tain : 38 parts in 1000, of earthy and alkaline chlorids and sulphates, 
 with a good deal of organic matter. Another copious spring on the river 
 Etobicoke, a little below the village of Brampton, was also found to be 
 very feebly saline. 
 
 BRANT.- 
 
 A copious spring of mineral water, belonging to the sixth class, occurs Braat. 
 on the fifty-third lot of the township of Brant. It is described as filling a 
 basin of eighty-eight by forty-five feet, having a depth of about forty feet, 
 and situated upon a mound composed of calcareous tufa. From the clear 
 blue color of the water in the basin, it has received the name of the Blue 
 Spring. The flow from the spring is constant and copious, and the water 
 is sulphurous to the taste and smell. No gas is evolved from the spring. 
 A partial analysis of the water gave as follows for 1000 parts : 
 
 Sulphate of lime, 1-240 
 
 " magnesia, '20t 
 
 Carbonate of lime, -198 
 
 1-645 
 
 The carbonate of lime, which was precipitated by prolonged boiling, 
 was" without any carbonate of magnesia. The water held no trace of 
 chlorids, but the amount of sulphuric acid obtained was a little more than 
 is required to form the sulphates of lime and magnesia, and it is probable 
 that a small portion of sulphate of soda exists in the water. 
 
 CALEDONIA. 
 
 Four springs are known at this watering place, three of which are very 
 near to each other, and belong to the third class. One of these is known as 
 the Gas Spring, from the quantity of carburetted hydrogen gas which it 
 evolves, and which was roughly estimated at 300 cubic inches per minute. 
 Another is called the Saline Spring, though less strongly saline than 
 the first ; and the third is known as the White Sulphur Spring. The 
 amount of sulphuretted hydrogen in this was found not to equal a cubic 
 inch in a gallon of the water, but it is said to have formerly been much 
 more sulphurous. The supply of water from the first spring was estima- 
 ted at about four gallons, and of the others at about ten gallons each, in a 
 minute. The analyses of these waters wiU be found in Table HI, 1, 2, 3. 
 The fourth, known as the Intermittent Spring, on account of the inter- 
 mitting discharge of carburetted hydrogen gas, is a water of the second 
 class. Its analysis is given in Table II, 1. All of these waters issue 
 from the Trenton group. 
 
. 
 536 GEOLOGY OF CANADA. [CHAP. XVIII. 
 
 CAXTON. 
 
 A saline spring of the second class rises from the Lower Silurian lime- 
 stones in the township of Caxton, on the banks of the Yamachiche, and 
 affords from six to eight gallons of water a minute, disengaging at the 
 same time great quantities of carburetted hydrogen gas. Its analysis will 
 be found in Table II, 3. 
 
 CHAMBLY. 
 
 <7hambiy. About a league north of the village of Chambly, in the Rang des Qua- 
 rantes, upon the land of Mr. Cherrier, there are two saline springs 
 belonging to the third class, and rising from the Hudson River formation. 
 From one of these flows a considerable current of pleasantly saline water, 
 containing 5-74 parts of solid matter in 1000. Baryta and strontia are 
 present in it in considerable quantities. This spring, which evolves abun- 
 dance of carburetted hydrogen gas, has a temperature of 53 F. The 
 second spring, near to this, was slightly ferruginous, and had a feeble 
 sweetish saline taste, but was not farther examined. 
 
 A remarkable spring occurs on the land of Antoine Jette*, on the Grand 
 Coteau, where a well has been sunk eight or ten feet, and the water over- 
 flows in a small stream. A little carburetted hydrogen gas is evolved from 
 the well, the temperature at the bottom of which was like that of the spring 
 mentioned above, 53 F., shewing these waters to be slightly thermal. This 
 water is feebly sweetish and saline to the taste, and belongs to the fourth 
 class. The carbonate of soda forms more than one half of the solid contents 
 of this water, which affords evidence of the presence of boracic acid, 
 bromine, iodine, strontia, and baryta. Two analyses closely agreeing with 
 each other, were made of portions of this water, collected in 1851 and 
 1852. The latter analysis is given in Table IV, 1. 
 
 CHAMPLAIN. 
 
 There are two springs near the village of Champlain which have a local 
 reputation. One of these, when visited, was full of surface water ; the 
 other was feebly saline and belonged to the second class. 
 
 CHARLOTTE VI LLK . 
 
 charlotte- A remarkable sulphurous spring, belonging to the sixth class, occurs on 
 YiUe - the third lot of the twelfth range of Charlotteville. The water fills a natu- 
 ral basin, covering about a hundred square yards, from which the discharge 
 was found to be about sixteen gallons a minute. The water rises through 
 several holes in the mud at the bottom of the basin. This is covered with 
 a layer of sulphur and carbonate of lime, a mixture /)f which incrusts leaves 
 and twigs placed in the spring. The water is remarkable for the predomin- 
 
CHAP. XVIII.] WATERS OF MINERAL SPRINGS. 537 
 
 ance of earthy sulphates, and for the great amount of sulphuretted hydro- 
 gen which it contains, amounting to 11 '6 cubic inches in 100 cubic inches 
 of water. This was determined at the spring, by precipitating it from the 
 recent water by means of a solution of chlorid of arsenic. The temperature 
 of this water in the basin was 45 F., its specific gravity 1002-7. It is 
 limpid and sparkling, and pungent to the taste from the great amount of 
 sulphuretted hydrogen which it contains. 1000 parts of the water yielded 
 on analysis : 
 
 Sulphate of potash, -0510 
 
 soda, -4718 
 
 lime, 1-1267 
 
 " magnesia, '4351 
 
 Chlorid of magnesium, -0878 
 
 Carbonate of lime, -3050 
 
 " magnesia, '0179 
 
 iron, traces 
 
 Sulphuretted hydrogen, -1776 
 
 The amount of solid matters is 2-495 parts in 1000. The carbonic acid 
 was equal to -273 parts, of which the carbonates require -143, leaving 
 -130, or scarcely enough to form with them bicarbonates. This spring 
 issues from the Corniferous formation. 
 
 A saline spring belonging to the third class, and rising from the Chazy or Htiroj , 
 the Calciferous formation, occurs on the tenth lot of the second range of 
 Fitzroy, on the land of Mr. Francis Gillan. It contains traces of strontia, 
 and a portion of phosphoric acid. For its analysis, see Table III, 6. 
 
 A spring on the twelfth lot of the sixth concession of the same township, 
 is feebly saline and sulphurous to the taste, and belongs to the second 
 class. It has not been quantitatively analyzed. 
 
 GLOUCESTER. 
 
 A water said to be from a spring on the land of Mr. Borthwick in Gloucester. 
 Gloucester, belongs to the second class, and is strongly saline, giving 11-20 
 parts of solid matter in 1000. It contains a little strontia, and rises from 
 the Lower Silurian limestones. 
 
 HALLOWBLL. 
 
 Several wells have here been sunk in the Trenton formation, with a view 
 of obtaining brine for salt-making, and have yielded bitter saline waters of 
 the first class. On the eleventh lot of the second range, a portion of 
 
538 GEOLOGY OF CANADA. [CHAP. SVIII. 
 
 Haiioweii. water was taken from a well twenty-seven feet deep, on the land of Mr. 
 Amos Hubbs. It was very bitter and saline, and gave only traces of pot- 
 ash salts, no sulphates, but bromids, and an unusually large proportion of 
 iodids. Its analysis is given in Table I, 3. A similar water, but less strong, 
 was afterwards received from Mr. Hugh McDonell of Hallowell. Its 
 analysis is given in Table I, 4. 
 
 HAWKE8BURY. 
 
 Hawkes- The water from a mineral spring said to be on the ninth lot of the 
 sixth range of Hawkesbury, is both saline and strongly alkaline, belonging 
 to the third class. A partial analysis gave for 1000 parts, chlorid of 
 sodium 8*177, sulphate of soda -083, carbonate of soda 1-200, carbonate 
 of lime -076, carbonate of magnesia -063 = 9-599. It contains moreover, 
 bromids, iodids, and boracic acid, with a little silica and oxyd of iron. 
 The quantities of these ingredients were not determined. 
 
 HAMILTON. 
 
 Hamilton. In the Canadian Journal for 1853, page 153, Prof. Henry Croft, of 
 Toronto, has described a mineral water said to be from Young's Spring at 
 Hamilton. It belongs to the sixth class, and is distinguished by the very 
 large proportion of sulphate of magnesia which it contains. The specific 
 gravity of this water was found to be 1006-4, and its composition, 
 according to Prof. Croft, was as follows, for 1000 parts : 
 
 Chlorid of sodium, -5098 
 
 Sulphate of soda, 1*6985 
 
 " lime, 1-1246 
 
 " magnesia, . . . . , 4-7799 
 
 8-1128 
 
 HENRY VILLE. 
 
 A sulphurous water belonging to the third or the fourth class, is found on 
 the land of David Miller, about two miles south of Henryviiie. It contains 
 a large proportion of carbonate of soda, with chlorids, and a trace of iodine, 
 together with sulphuretted hydrogen equal to 1-6 cubic inches in 100 
 cubic inches of the water. 
 
 JACQUES CARTIER RIVER. 
 
 Jacques A strongly sulphurous spring at Marcotte's Mills on the Jacques Cartier 
 
 cartier. River, belongs to the fourth class. It rises from the Utica formation, and 
 contains but a small amount of solid matter, of which carbonate of soda 
 makes up the largest part. It appears to hold a considerable proportion 
 *f borates. The chlorid of potassium equals 2-95 per cent, of the alkalies 
 estimated as chlorids. For the analysis of this water, see Table IV, 3. 
 
OHAP. XVIiL] WATERS OF MINERAL SPRINGS. 539 
 
 JOLT. 
 
 In the township of Joly there is a sulphurous spring, issuing from the 
 Hudson River formation, on the banks of a brook called the Magnenat, 
 about five miles from Methot's Mills. The water, which is feebly saline, 
 belongs to the fourth class, and contains a portion of boracic acid, besides 
 sulphuretted hydrogen gas equal to 7*5 cubic inches to a litre. See the 
 analysis, Table IV, 4. 
 
 KINGSTON. 
 
 In boring for water at Morton's distillery in Kingston, two mineral Kingston, 
 springs were met with. The waters of these are bitter and saline, par- 
 taking of the characters of the first class, but they are remarkable for the 
 large proportions of sulphates and of earthy carbonates which they contain. 
 In the presence of the latter elements, they approach in composition to the 
 waters of the second class. These waters have been examined by the Rev. 
 Professor Williamson, of Queen's College, Kingston, and the results of his 
 analyses, as calculated for 1000 parts, are as follows : 
 
 Upper well. Lower well. 
 Chlorid of sodium, 29-864 5-216 
 
 f>a1/MHTYi 19.QOA 4*010 
 
 1-763 
 2-441 
 
 " magnesium .... ... 
 
 6-954 
 
 
 
 " lime, 
 
 . ... -396 
 
 
 . ... '492 
 
 
 . ... -3TO 
 
 
 .... l-28f 
 
 
 
 400 
 
 52-25Y 13-830 
 
 Specific gravity, 1043-2 1010-0 
 
 The waters of the upper well contain, according to Dr. Williamson, both 
 iodine and bromine, the latter being the more abundant. In the lower 
 well, traces of sulphuretted hydrogen are met with. These waters are 
 from the Lower Silurian limestones. 
 
 LANORAIE. 
 
 A saline spring, rising from the Lower Silurian limestones, and belong- Lanoraie. 
 ing to the second class, occurs about mid-way between the villages of 
 Lanoraie and Industry. It gives off large volumes of carburetted hy- 
 drogen gas, and is remarkable for the considerable proportion of salts of 
 baryta and strontia which the water contains. An analysis of it will be 
 found in Table II, 5. 
 
540 GEOLOGY OF CANADA. [CHAP. XVIII. 
 
 A spring of acid water, belonging to the fifth class, is found in the 
 south-west corner of Niagara, on the land of Mr. McKinley. The basin 
 of the spring is about thirty inches deep, and three or four feet in diameter, 
 and is in a yellow clay, which at a depth of three or four feet is underlaid 
 by the red and green sandstone of the Medina formation. The basin, 
 which had no visible outlet, was nearly full of water. This was in constant 
 ebullition from the escape of inflammable gas, and had a decided taste 
 and smell of sulphuretted hydrogen. A half dried-up pool, about twenty 
 yards distant, contained a small quantity of very acid water. The water of 
 the basin is slightly yellowish, turbid, and very styptic and acid to the 
 taste. It contains sulphuric, but no hydrochloric acid, and portions of lime, 
 magnesia, alumina, protoxyd of iron, and alkalies, besides an organic mat- 
 ter, which causes the residue of the evaporated water to blacken when 
 heated. The specific gravity of this water is 1002-16, and the mean of 
 two determinations gave 2-1376 parts of sulphuric acid (S0 3 ) to 1000. 
 The same amount of water gave -074 of lime, equal to -180 of sulphate, 
 while the residue from calcination, after evaporating the water, consisting 
 of sulphates of lime and magnesia, with oxyd of iron and alumina, was 
 only equal to -600 ; so that in round numbers the water may be said to con- 
 tain two parts of hydrated sulphuric acid in 1000. After being kept for 
 some months in close vessels, a peculiar organic growth made its appear- 
 ance in the water. This, under the microscope, seemed to consist of 
 groups of filaments, each composed of a single chain of yellow translucent 
 homogeneous globules. 
 
 About a mile and a half above Chippewa, near the Niagara River, is a 
 similar spring, which has been described by Dr. Mack of St. Catherines. 
 The water is very sour to the taste, and strongly impregnated with sulphu- 
 retted hydrogen. A qualitative analysis shows it to be similar in composi- 
 tion to the water described above, but somewhat stronger. This spring 
 rises from the Onondaga formation ; but another similar water, said to 
 be near St. Davids, rises, like that of Niagara, from the Medina formation. 
 For farther particulars about these acid waters, see the description of the 
 spring of Tuscarora. 
 
 WICOLET. 
 
 Nicoiet. i n the concession of the Quarante Arpents, in Nicolet, and near to the 
 
 line of St. Gregoire, upon the farm of the widow Honore* Hubert, is a small 
 area destitute of vegetation, and impregnated with water, which was col- 
 lected by digging a hole in the earth. The color of the water, which be- 
 longs to the fourth class, was brownish-yellow, and its taste was alkaline, 
 but scarcely saline. An analysis of the soluble salts of this water will be 
 found in Table IV, 5. 
 
CHIP. XVIII.] WATERS OP MINERAL SPRINGS. 541 
 
 Another similar spring occurs on the land of Olivier Roy in Nicolet, 
 not far from the line of the Baie du Febvre. When evaporated, the 
 water becomes strongly alkaline to the taste. These two springs rise from 
 the Hudson River formation. 
 
 PLANTAQEHET. 
 
 Three saline waters, belonging to the second class, and issuing from piantagenet. 
 the Lower Silurian limestones, have been examined from this township. 
 The first is that of Larocque, generally known as the Piantagenet Spring, 
 of which the analysis will be found in Table II, 4. 'The second is the 
 so-called Georgian Spring, and differs from the last in containing a small 
 proportion of sulphates. Its analysis is given in Table II, 6. The third is 
 a water similar to the first, and was furnished by Mr. Peter Mclntosh. It 
 contains 10*16 parts of solid matter to 1000, and yields traces of boracic 
 acid, and a comparatively large amount of strontia. 
 
 The water of a saline and alkaline spring, containing no sulphates, 
 received from Mr. Sheriff Treadwell, is said to occur on the twelfth lot of 
 the first concession of Piantagenet. The specimen was diluted with surface 
 water, but evidently belonged to the third class. 
 
 QUEBEC. 
 
 A sulphurous water, which was formerly in some repute, rises from the Quebec 
 rocks of the Quebec group, in St. John's suburb, Quebec, on the property 
 of Mr. Joseph Hamel. It contains, besides common salt and carbonate of 
 soda, a portion of sulphates, and apparently belongs to the fourth class, 
 but when examined was diluted with surface water. 
 
 Two springs have been examined from the township of Rawdon. One of 
 the third class from the twenty-fifth lot of the third range, is somewhat 
 strongly saline, containing 4*96 parts of solid matter in 1000, and yielding 
 the reactions of baryta, boracic acid, bromine, and iodine. The other, 
 from the twenty-seventh lot of the same range, is an abundant spring of 
 slightly sulphurous water, belonging to the fourth class, which yields only 
 0*32 parts of solid matter in 1000, and contains portions of sulphates and 
 borates, with a trace of bromine. These springs apparently rise from the 
 Potsdam formation. 
 
 KIVIEBB OUELLE. 
 
 A saline spring occurs on the south side of the river, in the third 
 concession of this seigniory, on the land of Mr. Charles Rocheford, and 
 issues from the rocks of the Quebec group. An area of about half an 
 acre of clayey soil is here impregnated with salt water, which collects 
 in four basins, the largest being four or five feet in diameter and three 
 or four feet deep, the others somewhat smaller. The streams issuing 
 
542 GEOLOGY OF CANADA. [CHAP. XVIII. 
 
 from these unite to form a small rivulet. The water of all these basins is 
 apparently alike, and strongly saline and bitter. A portion from the 
 largest gave 13'36 parts of solid matter to 1000. It contained a small 
 amount of earthy carbonates, a very large proportion of chlorids of calcium 
 and magnesium, besides some sulphates, and distinct reactions of bromine 
 and iodine. This water belongs apparently to the first class. 
 
 SABKEVOIS. 
 
 Near to the village of Pike River, in Sabrevois, are several mineral 
 springs near to each other, the waters of two of which, known as the 
 Saline and Sulphur Springs, have been examined. Both are feebly saline 
 and sulphurous waters, of the second class, and rise from the Utica or the 
 Hudson River formation. The first contains salts of baryta and strontia ; 
 the second, and the stronger of the two, holds, on the contrary, soluble 
 sulphates. Both of these waters are very slightly impregnated with sul- 
 phuretted hydrogen. 
 
 SCARBOROUGH. 
 
 Scarborough. Two springs on the sixteenth lot of the fourteenth range of Scarborough 
 have a local reputation as mineral springs. Their waters give by boiling 
 a small amount of earthy carbonates ; but even when evaporated to one 
 tenth, they have no marked taste. They contain, besides, only sulphate 
 of lime, with traces of chlorids. 
 
 The water of a well at the Bank of Upper Canada in Toronto has a 
 similar composition, while that of a spring at Spadina, which deposits a 
 large amount of carbonate of lime in the form of calcareous tufa, contains 
 in solution only traces of chlorids, and no sulphates. 
 
 STB. ANNE DE LA POCATIEBE. 
 
 ste. Anne. In the second concession of this seigniory, on the land of Nicholas Rou- 
 leau, is a copious spring of slightly sulphurous water, which issues from a 
 hill of sandstone of the Quebec group, and has a temperature of 44*5 F. 
 It gives by evaporation only 0*36 parts of solid matter to 1000 : the resi- 
 due is strongly alkaline to the taste, and contains a small portion of sul- 
 phates. This water belongs to the fourth class. In the same concession, 
 about a mile to the north-east of the last, and a mile south of the college, 
 is a small spring of bitter saline water, which contains, besides chlorids, an 
 abundance of sulphates of lime and magnesia, and a small portion of car- 
 bonates. It belongs to the second class, and yields 5-06 parts of solid 
 matter to 1000. 
 
 ST. BBNOIT. 
 
 A spring nearly opposite to the old church of St. Benoit rises through 
 the clays, which here overlie the Fotsdam formation. The specific gravity 
 
CHAP. XVIIL] WATERS OF MINERAL SPRINGS. 543 
 
 of the water is 1004-3, and it contains about 6-0 parts of solid matter to st. Benoit. 
 1000. This water, which may be referred to the first class, contains traces 
 of carbonates, and large amounts of calcareous and magnesian salts, both 
 chlorids and sulphates. 
 
 ST. CATHABIUE8. 
 
 A well was sunk some years since in the town of St. Catharines in the st. Catharines, 
 hope of obtaining brine for the manufacture of salt. A boring, five inches 
 in diameter, was carried to a depth of about 500 feet, and after traversing 
 the red strata of the Medina formation, is said to have penetrated fifty or 
 sixty feet into the schists of the Hudson River formation. The well is 
 stated to yield about twenty-two gallons of water per minute. The brine 
 is so much charged with lime and magnesia salts as to be unfit for the 
 manufacture of salt ; but it has acquired a considerable reputation in the 
 treatment of many diseases. It is used at the well, both internally and 
 externally, and is also evaporated to a small volume, and sent over the 
 country in a concentrated form. This water, which belongs to the first 
 class, was analysed a few years since by Prof. Croft of Toronto, whose 
 analysis is given below (I). Its specific gravity was 1036-0. 
 
 A second boring, made in the town of St. Catharines by Mr. E. S. 
 Adams in 1861, has resulted in the discovery of a saline water similar to 
 that of the old well, but somewhat less strong. The composition of this 
 last seems subject to some variation, as will be seen by comparing with the 
 analysis of Prof. Croft, the results of a partial examination of a specimen 
 of the water obtained from the old well, in December, 1861, (II), at 
 the same time with the water of the new well (III). In these analyses 
 the chlorid of potassium and the iodid of sodium were not determined. 
 These waters gave for 1000 parts as follows : 
 
 I. n. in. 
 
 Chlorid of sodium, 29-8034 23-00 19-94 
 
 potassium, -3555 
 
 " calcium, 14-8544 9-66 6-49 
 
 " magnesia, 3-3977 2-40 1-95 
 
 Iodid of sodium, -0042 
 
 Sulphate of lime, 2-1923 1-75 1-77 
 
 50-6075 36-81 30-15 
 
 ST. BU8TACHE. 
 
 About two leagues beyond the church of St. Eustache, on the land of 
 Joseph Laurin, is a feebly saline spring belonging to the second class, and 
 yielding 1-88 parts of solid matter to 1000 of the water. It contains a 
 portion of sulphates, and issues from the Lower Silurian limestones. 
 
544 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. XVIII, 
 
 STE. GENEVIEVB. 
 
 Ste. 
 
 St. Hyacinth. 
 
 St. L6on. 
 
 Ste. Martine. 
 
 Ste. Genevieve, on the Batiscan River, offers several strongly saline 
 springs of the second class, two of which have been analysed, and are re- 
 markable for the large proportion of iodids which they contain. The first is 
 on the land of Olivier Trudel, a league above the church, and disengages 
 bubbles of carburetted hydrogen gas ; the supply of water is abundant. 
 Another spring occurs at the ferry, directly opposite to the church. These 
 waters rise from the Lower Silurian limestones. The analyses of both of 
 them are given in Table II, 7 and 8. 
 
 ST. HYACINTH. 
 
 The so-called Providence spring of St. Hyacinth, is a saline water of the 
 third class, issuing from the Hudson River formation. It is strongly alka- 
 line, and contains a portion of strontia. The solid matters of the water 
 equalled 5'16 parts in 1000. 
 
 ST. LEON. 
 
 A strongly saline spring is met with in the valley of the Riviere a la Glaise, 
 about a mile from the church of St. Le'on. It rises from the Hudson River 
 formation, or from the Lower Silurian limestones. The volume of water 
 discharged is considerable, and it is accompanied with large quantities 
 of carburetted hydrogen gas. This water belongs to the second class, and, 
 besides small portions of baryta and strontia, contains sufficient carbonate 
 of iron to give it a chalybeate taste. Its analysis is given in Table II, 2. 
 
 STE. MARTINE. 
 
 A feebly saline water from the parish of Ste. Martine, in Beauharnois, 
 belongs to the third class, and probably rises from the Calciferous formation. 
 It gives 1-98 parts of solid matter to 1000, and contains a small portion of 
 sulphates. This spring is said to be sulphurous. 
 
 St. Oure. 
 
 In constructing a lock on the Richelieu River, at St. Ours, a mineral 
 spring was found, which was inclosed in such a manner as to make it 
 accessible from above by a pump. The water, which rises from the 
 Hudson River formation, and belongs to the fourth class, contains only -53 
 parts of solid matter to 1000, among the soluble parts of which carbonate 
 of soda predominates, with chlorids and small portions of borates. Its 
 analysis is given in Table IV, 2. The large proportion of potash salts 
 is remarkable. 1000 parts of this water gave -2250 of alkalies, estimated 
 as chlorids, of which -0565 parts, or 25-11 per cent, were chlorid of 
 potassium. Another determination gave 24-52 per cent of chlorid of po- 
 tassium. A portion of water taken from the spring several weeks previ- 
 
CHAP. XVIII.] WATERS OF MINERAL SPRINGS. 545 
 
 ously, gave a larger amount of alkalies, equal to -3400 of chlorids in 1000 
 parts, of which -0596, or 17*53 per cent, were chlorid of potassium ; appar- 
 ently showing an admixture of a more saline water, richer in soda salts. 
 
 TU8CAKORA. 
 
 What is known as the Sour Spring of Tuscarora is upon the Indian 
 Reserve, about nine miles south of Brantford, and three miles south of the 
 bank of the Grand River. The water issues from a small mound around 
 the roots of a decaying pine tree, whose ruins constitute 'the soil. This for 
 some distance around is saturated with acid water, and destitute of vege- 
 tation. Several depressions at the foot of the mound are filled with acid 
 water, the largest being about eight feet in diameter, three or four feet 
 deep, and nearly full, but without any visible discharge. The water is 
 kept in constant agitation by a discharge of inflammable gas. It is slightly- 
 turbid and brownish, and has a styptic, acid and sulphurous taste. The 
 presence of sulphuretted hydrogen is also evident from the odor, and from 
 the ready blackening of bright silver when immersed in the water. Its 
 amount was determined on the spot, by a solution of arsenic, and was 
 found equal to only one fourth of a cubic inch in 100 cubic inches of the 
 water. The specific gravity of the water was 1005-58. It contained no 
 trace of chlorids, but gave by analysis as follows for 1000 parts : 
 
 Sulphate of potash, -0608 
 
 " soda -0502 
 
 " lime, -7752 
 
 " magnesia, -1539 
 
 " protoxyd of iron, -3o38 
 
 " alumina, -4681 
 
 Phosphoric acid, traces 
 
 Hydrated sulphuric acid (S0 3 HO), 4-2895- 
 
 6-1615 
 
 A portion of organic matter is present, which causes the water to- blacken 
 when evaporated to a small volume. No traces of zinc, manganese, cobalt, 
 or nickel could be detected in this water ; and the presence of free sulphu- 
 retted hydrogen is evidently incompatible with the existence, in solution, of 
 most of the other metals occasionally found in mineral springs, such as tin, 
 lead, copper, antimony, and arsenic. 
 
 The above analysis was made with water taken from the spring in Octo- 
 ber, 1847. A portion of the water, collected in April, 1846, had been 
 previously submitted to a partial analysis by Prof. Croft of Toronto, whose 
 results show a considerable ehange in the composition of the water. His 
 determinations are here given (I), and are compared with those obtained 
 in the analysis already given above. 
 
 KK 
 
546 GEOLOGY OP CANADA. [CHAP. XVHI. 
 
 I. II. 
 
 Sulphuric acid (S0 3 ), .......... 2-9069 ........ 4-6350 
 
 Potash, ....................... - ........ '0329 
 
 Soda, ......................... - ........ -0219 
 
 Lime, ........................ -4798 ........ -3192 
 
 Magnesia, ..................... '2036 ........ -0524 
 
 Peroxyd of iron and alumina, ... '5148 ........ -3315 
 
 4-1051 5-3929 
 
 The water examined by Prof. Croft is more dilute, but contains a greater 
 amount of bases than that collected eighteen months later. In the former, 
 the sum of the bases is to the amount of sulphuric acid as 412 : 1000, and 
 in the latter, as 152 : 1000. The proportion of the lime to the acid is about 
 as 1 : 6, by weight, in the first, and as 1 : 15 in the second. 
 
 The proportions between the magnesia and the sulphuric acid in the 
 two are respectively as 1 : 15 and 1 : 90. If it be supposed that the 
 water at its source contained only sulphuric acid, and dissolved the various 
 bases in its way through the strata, it would follow, that, as these gradually 
 become exhausted of their soluble elements, the proportion of saline matters 
 in the waters of the spring must diminish. 
 
 The two saline springs of Varennes rise through the clays which overlie 
 the Utica, or the base of the Hudson River formation, and belong to 
 the third class. They are situated about a mile and a half below the 
 church, not far from the St. Lawrence, and are about 100 rods apart. 
 The one enclosed within the house is known as the Gas Spring, from the 
 large volume of carburetted hydrogen gas which it gives off. This was 
 formerly collected in a gas-holder, and employed in lighting the house. 
 The outer one is known as the Saline Spring, and is generally resorted to 
 for drinking. It affords, from time to time, a few bubbles of carburetted 
 hydrogen, and yields two or three gallons of water in a minute. The 
 temperature of the Saline Spring, on the 20th of November, 1847, was 
 found to be 47 F., and that of the Gas Spring only 40, the air being 19. 
 On the 18th of October, 1848, the air being 44, the Saline Spring was 
 47*5, and the Gas Spring 45*5. While the former spring, although un- 
 covered, scarcely freezes, it is said that in winter the latter becomes filled 
 with ice. This difference may be in part due to a less abundant supply of 
 water in the Gas Spring, rendering it more affected by atmospheric influ- 
 ences. At the same time, the escape and rarefaction of large volumes of 
 carburetted hydrogen gas, from a state of compression in the strata below, 
 may be supposed to diminish the temperature of the Gas Spring, from the 
 waters *of which gas is constantly escaping. The analyses of these two 
 waters are given in Table III, 4 and 5. 
 
CHAP. XVIII.] 
 
 WATERS OF MINERAL SPRINGS. 
 
 547 
 
 WE8TMEATH. 
 
 On the thirteenth lot of the sixth range of Westmeath is a spring which 
 deposits a considerable amount of calcareous tufa, and is known as the 
 Petrifying Spring. The water contains, besides carbonate of lime, small 
 quantities of chlorids, and is feebly sulphurous. On the twenty-third lot 
 of the same range, a copious spring, similar to the last, occurs on Tucker's 
 Creek. It contains a large amount of carbonate of lime, and a little iron ; 
 besides which, it holds only traces of sulphates and chlorids. 
 
 WHITBY. 
 
 At Bowerman's Mills, on the thirty-second lot of the third range of wintby. 
 Whitby, there is a copious saline spring of the first class, containing an 
 abundance of bromine, but only traces of iodine. It yields also minute 
 portions of strontia and oxyd of iron, and very small quantities of potash 
 salts. The analysis of this water is given in Table I, 2. 
 
 TABLE I. WATERS OF THE FIRST CLASS. 
 
 
 1. 
 
 2. 
 
 3. 
 
 4. 
 
 
 17-8280 
 
 18-9158 
 
 38-7315 
 
 17*4000 
 
 
 0920 
 
 traces 
 
 traces 
 
 
 
 12-8027 
 
 17-5315 
 
 15-9230 
 
 9-2050 
 
 
 5-0737 
 
 9-5437 
 
 12-9060 
 
 9-4843 
 
 
 1178 
 
 2482 
 
 4685 
 
 undet 
 
 lodid of " 
 
 
 0008 
 
 0133 
 
 <( 
 
 
 7769 
 
 
 
 
 
 traces 
 
 0411 
 
 
 
 
 
 0227 
 
 
 
 
 
 traces 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 36*6911 
 
 46*3038 
 
 68-0423 
 
 36*0893 
 
 
 1029'! 
 
 
 1053-11 
 
 
 
 
 
 
 
 1. Ancaster. 2. Whitby. 3. Hallo well, Amos Hubbs. 4. Hallo well, H. McDonell. 
 
548 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. XVIII. 
 
 S'O 
 
 9 a 
 oo ss 
 
 60t-M . 
 
 MOROCCO 
 
 OiflO^H . 
 
 ^999 
 
 &<>< 
 *>oi5 
 
 2 
 
 9 ^ 2 fl 
 
 OO 
 Or* 
 COO 
 
 OOlMCit-OS 
 
 00 
 
 00 
 
 <> 
 oocomoococM O l' 
 
 OCOOOO-MCiOoS I C CO <M CVi &> ? "S CO 
 
 i ^ o o CN c* oo I o o re rf o * oo o 
 
 < * * 53 c*i o 
 
 OO . . Tj< "M O CM . . .OTfCOOW 00 
 
 cp2 ; .'2^00 * '. ' oao >-, ^ r 
 ^ ::' ':::* '^coo 
 
 OO . .COCOlMOi . . .OCOTj*CTiO CO CO 
 
 oo . -orjiTj-co . .coa:nt-o *-* co 
 m r co o . * n o ^J" o o _. 
 t-o . .ocooo . .^10000 cp 
 
 CO O 
 
 l_ 
 
 coco ' r-t COO5-*. "dioo^co^ co c5 
 
 C3500OOt-COOO . . ! **" CO OO -^ CO 
 ^^OOOCOOO . .COOiOOO 00 
 
 co o 
 
 o .r-cococ> . Icoco 4l cNi* J os 
 CO.OOCOC<IO.. (MCO^iM CO 
 
 wo .CNIOOO . .-toogog cp 
 
 Oj 
 
 - 
 S t^. 
 
 M 
 
 II : I 
 
 rn 
 
 SI 
 
 s 
 
 I 
 
 .2 3 
 
 2 <S 
 
 o "^ 
 
 t? 
 
 a. . 
 
 co b 
 
 02 
 
 
 
 Vtt tf 
 
 .2 2 
 
 1:0 
 
 23 
 
 I M 
 
CHAF. VIIII.] 
 
 WATERS OP MINERAL SPRINGS. 
 
 549 
 
 <0 -rj -r; -3 
 
 la! a 
 
 JO P 3 3 I 
 
 O CO CO O Oi <n O 00 
 
 CO 0*1 O5 C5 O ^ ^" CD 
 
 C CO O O . C-1 O * ft <> - O o 
 
 "tOOO . COOOCOCO?" f 5 o 
 
 
 
 oocooogo fr- 
 
 os : : *- ' 6 o 
 
 o o o w co .00 . .oowcoo 
 
 5S2|2 :S : :SS8gS 5? g 
 
 0000*0 * . .C<I<MOO Oi 
 
 ***" : * ::"**" 
 
 OJCOp^OO .N . .O<MW,Jif5 O 00 
 
 oo*. Sl* g^5 T? ^ 
 
 Tt<OOOO . ^ > O ? S O CO 
 
 10 . . o e-? n o co 
 
 5 - 1Q .GO 
 O .^ . -'..-^N^.-* 
 
 osoppo p . r-iooo t- g 
 
 1^. 
 
 :*:::::: L ' *" 
 
 : : : L : j-S ! S 
 S"'5 B" 2 ^"- b i S" SB 
 
 .3 r ! - .* ^ . "o ^ 
 
 O O O V. CM oo *> 
 
 O O " eS 
 
 ft W> 
 
 s^s's-ti- ^ g < 
 
 g-g-a-^^J E^S'S 
 
 3 2-3^2^ =s a SL 
 
 O CQ O2^.O <5 02 i-i O2 
 
 * 
 
 i 
 
 ;-i 
 
 " 
 
 2 
 
 - 2 
 i Oi 
 > 03 
 
 bo 
 
 .5 
 
 fl 
 
 03 [24 
 
 i! 
 
 o .2 
 
 t 
 
 G 
 
 *"S 
 leg 1 
 
 C. w 
 
 w 2 
 
 3 
 
 Oi 
 02 
 
550 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XVIII. 
 
 TABLE IV. WATERS OF THE FOURTH CLASS. 
 
 
 1. 
 
 2. 
 
 3. 
 
 4. 
 
 5. 
 
 Chlorid of sodium, 
 
 8381 
 
 0207 
 
 0347 
 
 3818 
 
 3290 
 
 " potassium, . . 
 
 0324 
 
 0496 
 
 0076 
 
 0067 
 
 0318 
 
 
 
 0081 
 
 traces 
 
 0215 
 
 traces 
 
 Carbonate of soda 
 
 1-0604 
 
 1340 
 
 1952 
 
 2301 
 
 1'1353 
 
 
 
 
 
 
 
 strontia 
 
 0045 
 
 
 
 
 
 " lime, 
 
 0380 
 
 1740 
 
 0710 
 
 0620 
 
 undet. 
 
 " magnesia, . 
 
 .0765 
 
 1287 
 
 0278 
 
 0257 
 
 (i 
 
 " iron, 
 
 0024 
 
 traces 
 
 
 
 
 
 
 0063 
 
 undet 
 
 undet. 
 
 undet. 
 
 it 
 
 Silica, 
 
 0*730 
 
 0160 
 
 0110 
 
 0245 
 
 u 
 
 
 
 
 
 
 
 In 1000 parts of water, . 
 
 2-1322 
 
 5311 
 
 3473 
 
 7523 
 
 1-5591 
 
 1. Chambly. 2. St. Ours. 3. Jacques Cartier. 4. Joly. The -0215 in this analysis 
 is sulphate of soda. 5. Nicolet, Hebert's Spring. 
 
 ON THE CHEMICAL COMPOSITION OF THE PRECEDING WATERS. 
 
 The results obtained during the long series of analyses which have 
 been given above, offer many points of interest, which will now be indicated 
 in discussing successively the principal constituents of the mineral waters, 
 and their chemical history. 
 
 SALTS OF SODA AND POTASH. 
 
 potash aud The compounds of soda generally predominate in saline waters, and it is 
 only in rare cases that the saline ingredients of these consist chiefly of the 
 salts of lime and magnesia. By a reference to the Tables II and III, it will 
 be seen that the chlorid of sodium, or common salt, forms the greater portion 
 of the solid matter of these saline waters, and that it is only among the 
 waters of the fourth class that the alkaline carbonates constitute a large 
 portion of the soluble salts present. The relative proportions of soda and 
 potash are subject to considerable variations. In the waters of the ocean the 
 potash does not form more than two or three per cent, of the alkalies, 
 calculated as chlorids; while in the various brine springs of England, 
 
CHAP. XVIIL] WATERS OF MINERAL SPRINGS. 551 
 
 Germany, and Canada, it is still less ; often amounting, as in the waters of 
 the first class, to traces only. In the waters of the second class, its propor- 
 tion becomes somewhat greater ; and in those of the third class, and more 
 especially in the fourth, where alkaline carbonates predominate, the propor- 
 tion of potash salts is sometimes worthy of especial notice. The alkaline 
 chlorids of the water of Nicolet yield I 4 89 per cent, of chlorid of potassium, 
 those of Jacques Cartier 2*95, and those of St. Ours not less than 25*0 per 
 cent. There does not, however, appear to be any constant relation between 
 the proportion of alkaline carbonates and the potash, since the Nicolet and 
 Jacques Cartier waters are more alkaline than the water of St. Ours, while 
 the salts from the spring of Joly contain less than one per cent, of potash. 
 
 SALTS OF LIME AND MAGNESIA. 
 
 The waters of the first class are characterized by the presence of great Lime and 
 quantities of chlorids of magnesium and calcium ; amounting, in several maglief 
 cases, to more than one half the solid contents of the water. This compos- 
 ition is altogether unlike that of any waters hitherto studied. The bittern 
 left after the partial separation of the salt from sea-water by evapora- 
 tion, contains a large amount of chlorid of magnesium, but lime salts are 
 altogether wantirfg'in it. These have been separated during evaporation in Earthy 
 the form of sulphate, in which state a portion of magnesia still exists in the chlor 
 bittern, showing an excess of sulphuric acid over that required to combine 
 with the lime. In the waters of the first class, on the contrary, lime abounds, 
 while Sulphates are absent, or are present only in small quantities. The 
 water of the Dead Sea offers some resemblance to these curious brine 
 springs, in its large amount of chlorid of magnesium ; but it differs in contain- 
 ing a much smaller proportion of chlorid of calcium, and a larger quantity 
 of chlorid of potassium ; resembling in this respect the bittern of sea-water, 
 in which, from the separation of the chlorid of sodium, the potash has 
 accumulated. The occasionally large proportion of iodine in these brine 
 springs, is especially worthy of notice. The stratigraphical relations of 
 these waters, which issue from the limestones near the base of the palaeozoic 
 series, will be considered farther on. 
 
 While the waters of the first class are destitute of earthy carbonates, 
 or, like sea-water and most true brine springs, contain them only in small 
 amounts, those of the second, third, fourth, and sixth classes deposit, by boil- 
 ing, considerable quantities of the carbonates of lime and magnesia. The 
 relative proportions of these carbonates vary. In the precipitate from the 
 waters of the second class, which contain chlorids of calcium and magnesium, 
 the carbonate of magnesia greatly predominates over the carbonate of lime, 
 and sometimes exceeds seven or eight per cent, of the solid matters present, 
 as in the St. Le*on and Caxton springs. A similar predominance of carbon- 
 ate of magnesia is observed in the precipitates obtained by boiling the 
 
552 GEOLOGY OF CANADA. [CHAP. XVIII, 
 
 alkaline saline waters of the third class ; while in the more alkaline waters 
 of the fourth class, these proportions are reversed, and the carbonate of 
 lime predominates ; as is likewise the case in those of the sixth class. 
 Earthy car- At the temperature of boiling water, carbonate of lime slowly decomposes 
 a solution of chlorid of magnesium, with the production of carbonate 
 of magnesia and chlorid of calcium ; so that the proportions of the 
 two bases in the precipitated carbonates will depend upon the length 
 of time which the water has been boiled. Thus in the analysis of the 
 water of Ste. Genevive (II, 7), the proportion of the two carbonates 
 is given as 12 : 750. When, however, another portion of the same 
 water was boiled to one sixth of its volume, in contact with the separated 
 carbonates, the lime had entirely disappeared from the precipitate, which 
 was only carbonate of magnesia. From this, it follows that the proportions 
 in which the chlorine is divided between the calcium and magnesium in a 
 mineral water, cannot be determined from the results of analysis. In some 
 experiments made with the intention of elucidating this question, it was found 
 that from an artificial mineral water, containing chlorids of calcium and 
 magnesium, besides bicarbonates of the same bases, there was separated, 
 by thirty minutes' boiling, a precipitate which contained -173 of carbonate 
 of magnesia and -666 of carbonate of lime ; while by spontaneous evapora- 
 tion, a portion of the same liquid gave -805 carbonate of lime, without any 
 carbonate of magnesia. This same fact is curiously illustrated in the case of 
 the Plantagenet water (Table II, 4), whose analysis gives chlorid of cal- 
 cium -1364, chlorid of magnesium -2452, with carbonate of lime -0330, and 
 carbonate of magnesium -8904 ; the latter numbers being deduced from 
 the precipitate obtained by ebullition. When however this water is left 
 to spontaneous evaporation, the whole of the lime is deposited as car- 
 bonate, and the solution remains, for a time, charged with sesqui-carbonate 
 of magnesia. This compound, even in closed vessels, is spontaneously decom- 
 posed, with the precipitation of a portion of crystalline hydrated carbonate 
 of magnesia, equal to *772 parts of carbonate of magnesia to 1000 parts 
 of the liquid, while bicarbonate of magnesia and chlorid of magnesium 
 remain in solution. 
 
 TWO types The various saline waters of the Lower Silurian rocks may be looked 
 r saline upon as derived from two types, the one of which is represented by the 
 waters of the first class, derived from the limestones, and the other 
 by those of the fourth class, which apparently have their origin in the 
 shales and sandstones. In some cases, the brines of the first class appear 
 to pass unchanged through the overlying formations, as at Ancaster ; but 
 more frequently they become mingled with the alkaline waters of the fourth 
 class. In order to make known the reactions which would result from this 
 admixture, a series of experiments was made, with the following results. 
 When to an artificial water, resembling in composition that of Whitby or 
 
CHAP. XVIII.] WATERS OP MINERAL SPRINGS. 553 
 
 of Hallowell, there is added a dilute solution of carbonate of soda, a pre- 
 cipitate is formed, which consists of carbonate of lime, with about sixteen 
 per cent, of carbonate of magnesia. The solution, evaporated at a gentle 
 heat, afterwards deposits carbonate of magnesia, with only sixteen per cent. 
 of carbonate of lime. When a solution of bicarbonate of soda is sub- 
 stituted, the precipitate of carbonate of lime does not contain more 
 than two or three per cent, of carbonate of magnesia, and the liquid retains, 
 in the form of bicarbonate, a portion of lime, which may be separated by- 
 evaporation at the ordinary temperature ; but at a boiling heat, as already 
 stated, it reacts on the chlorid of magnesium present, and gives rise to a pre- 
 cipitate of carbonate of magnesia. In this way, may be explained the 
 generation of the waters of the second and third classes from the admix- 
 ture of the carbonated alkaline waters of the fourth with those of the first 
 class. It will be observed, that the waters of the third class contain less 
 solid matter than those of the second, showing apparently a greater admix- 
 ture of the more dilute alkaline waters of the fourth class. 
 
 SALTS OF BARYTA AND STRONTIA. 
 
 The presence of baryta and strontia has been detected in a great Baryta and 
 number of the saline waters of Canada ; and it is probable that in most 8trontia - 
 cases the two bases will be found together. In several of the analyses 
 given above, the formation of a precipitate by a solution of gypsum, in 
 the concentrated and acidulated water, was regarded as sufficient evi- 
 dence of the presence of one or both of these bases ; but in the 
 waters of Varennes, St. Le*on, and Lanoraie, the precipitate of sulphates 
 thus obtained was submitted to further examination, and found in each 
 case to consist of a mixture of the sulphates of baryta and strontia. In the 
 waters of the second class, a portion of these bases was found in the pre- 
 cipitate of carbonates obtained by boiling, while another portion remained 
 in solution as chlorids. It is probable that the carbonates of baryta and 
 strontia react with the chlorid of magnesium like the carbonate of lime, 
 so that the remarks already made about the salts of magnesia and lime 
 will equally apply to the present case. 
 
 SALTS OF IRON, MANGANESE, AND ALUMINA. 
 
 Traces of iron are seldom or never wanting in those waters which con- iron. 
 tain earthy carbonates. The proportion is ordinarily very small ; but 
 the waters of St. Le'on, Caxton, Plantagenet, and the Saline Spring of 
 Varennes may be regarded as slightly chalybeate. In every case when a 
 portion of one of the saline or alkaline waters, or the precipitate obtained 
 from it by boiling, is evaporated to dryness with an excess of hydro- 
 chloric acid, and the residue treated with dilute hydrochloric acid to 
 separate silica, the solution will be found to yield with ammonia a precipi- 
 
554 GEOLOGY OP CANADA. [CHAP. XVIII. 
 
 Alumina, tate. This, which is often colorless, is partly soluble in potash, and contains 
 a portion of alumina. When dissolved in hydrochloric acid, it gives with 
 a sulphocyanid the reaction of iron, and with molybdate of ammonia, indicar 
 
 Manganese, tions of phosphoric acid. When heated with a little caustic soda on silver 
 foil, the precipitate rarely, if ever, fails to give evidence of the presence 
 of manganese. The small portion of alumina which these waters contain, 
 is not derived from suspended argillaceous matters, but appears to be 
 in a state of solution. 
 
 CHLORIDS, BKOMIDS, AND IODID8. 
 
 The characteristic element of the saline waters is chlorid of sodium, with 
 variable proportions of chlorid of potassium, and in the first and second 
 classes, with chlorids of the earthy bases. These chlorids are accompanied 
 by portions of bromids and iodids. The proportion of the bromids to the 
 chlorids however appears to be less in these springs than in the sea-water 
 of the present day. Thus, according to Usiglio, 100 parts of the salts of 
 the Mediterranean contain 1-48 of bromid of sodium ; and ten analyses, by 
 Von Bibra, of the waters of different oceans, give from -86 to 1-46 parts, 
 affording for 100 parts of salts, an average of 1/16 parts of bromid of 
 sodium, equal to 1-04 parts of bromid of magnesium. The waters of 
 Whitby and Hallowell, on the contrary, which are the richest in bromids, 
 give only -54 and -69 parts of bromid of sodium to 100 parts of solid matters ; 
 while the two springs of Ste. Genevive contain respectively only -28 and 
 21 parts of bromid of sodium (or magnesium), and that of Lanoraie 
 22 parts of bromid of magnesium. The proportion of bromids in many 
 other saline springs of the country is still smaller. 
 
 The variations in the amount of iodine are not less remarkable. 
 In the waters of the modern ocean, it is well known that iodine is 
 present only in minute traces ; and in some strongly saline springs, like 
 that of Whitby, it is only in the alcoholic extract of the evaporated 
 residue that iodine can be detected. The Hallowell water (Table I, 3), 
 which closely resembles this in its general composition, and in its propor- 
 tion of bromine, contains however so much iodine that its presence can 
 readily be discovered without evaporation. It suffices to add to the 
 recent water, acidulated by hydrochloric acid, a little solution of starch, 
 and a few drops of nitrite of potash, to obtain an intense blue color. The 
 iodid of sodium in the first water was found equal to '0017 parts of the 
 solid matter ; and hi the second to -019, or nearly twelve times as much. 
 The saline waters of Ste. Genevive give as marked a reaction for iodine as 
 that of Hallowell, and when acidulated with . hydrochloric acid, without 
 previous evaporation, yield, with a salt of palladium, an insoluble precipitate 
 of iodid, after a few hours. The spring II 7 contains -063 parts, and II 8 
 yields -138 parts of iodine for 100 of solid matters ; so that there appears 
 to be no constant proportion between the chlorids, bromids, and iodids 
 
CHAP. XVIII.] WATERS OP MINERAL SPRINGS. 555 
 
 of these saline waters. The springs of Ste. GeneviSve are remarkably 
 rich in iodine, as will be seen by comparing them with the various 
 aafine waters of Canada and of other regions. The Congress Spring of 
 Saratoga, which is an alkaline saline resembling that of Varennes, but 
 charged with carbonic acid gas, gives, according to Schweitzer's analysis, 
 for 100 parts of solid matters *464 parts of bromid of sodium, and *013 
 parts of iodid of sodium. 
 
 SULPHATES, SULPHUBETS, A1TO STTLPHUBIO ACID. 
 
 A great number of the saline and alkaline waters of Canada contain sulphates, 
 soluble salts of baryta, whose presence is incompatible with the existence 
 of sulphates in solution. These are however met with in the waters of the 
 third class, from Caledonia, and in all those of the fourth class which have 
 been examined, that from Chambly excepted. In all of these waters, 
 however, chlorids or carbonates of soda predominate, and the sulphates 
 are present only in comparatively small quantities. In the waters of the 
 sixth class, on the contrary, the chlorids are present in small amounts, and 
 the sulphates of lime and magnesia are the characteristic ingredients, the 
 former salt predominating in the springs of Brant and Charlotteville. The Magnesian 
 water of Young's Spring, from Hamilton, differs from these ; inasmuch as, 8ul P hate 
 according to Prof. Croft's analysis, more than one half of the saline con- 
 tents of the water consists of sulphate of magnesia. Such waters are 
 but rarely met with ; but a spring near Crown Point, in Essex County, New 
 York, according to Dr. Emmons, contains in 1000 parts, 18-78 parts of 
 solid matter, which consists principally of sulphate of magnesia, with a 
 little sulphate of lime. It is probable that mineral waters of this kind are 
 directly connected with the sulphate of magnesia which has already been 
 described as incrusting the dolomites of the Clinton formation in western 
 Canada, and efflorescing elsewhere upon Lower Silurian shales (page 460). 
 
 The origin of the sulphate of magnesia, which is often found in similar its source, 
 conditions upon magnesian rocks, is, upon the authority of Mitscherlich, 
 ascribed to the decomposition of sulphate of lime by the carbonate of 
 magnesia of dolomite. A series of experiments has, however, shown that, 
 although a solution of gypsum is readily decomposed by hydrated carbonate 
 of magnesia, it may remain for months in contact with dolomite without 
 change. It is probable that the sulphate of magnesia which now impreg- 
 nates mineral springs, or effloresces from the surface of certain rocks, 
 existed, like other saline elements, disseminated in the strata ; except in 
 those cases where, as at Marmora, it is produced from magnesian rocks 
 by the sulphuric acid from oxydizing pyrites. 
 
 The waters of Brant and Charlotteville closely resemble in composition 
 the well-known sulphur springs of Sharon and of Avon, in New York. In 
 all of these, the sulphuretted hydrogen has doubtless been formed by the 
 
556 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. XVIII. 
 
 Solpharet- 
 
 ted hydro- 
 gen 
 
 Sulphuric 
 
 reducing action of organic matter, which converts the sulphates into sul- 
 phurets ; these, in their turn, are decomposed by carbonic acid, with the 
 separation of sulphuretted hydrogen. This reaction is probably the source 
 of all sulphuretted waters ; and it may be, in some cases, carried so far as to 
 decompose the whole of the soluble sulphates in a water, converting them 
 into carbonates. An example of this is seen in the saline water of the 
 second class from Sabrevois, which contains no sulphates, but holds in 
 solution sulphuretted hydrogen and a portion of baryta. 
 
 The origin of the sulphuric acid in the waters of the fifth class is not 
 easily explained. A few similar springs are known elsewhere, in volcanic 
 countries ; and the origin of the acid in these cases is ascribed, either to 
 the oxydation of the sulphurous acid formed by the combustion of sul- 
 phuretted hydrogen, or to the slow and direct oxydation of the latter gas, 
 in the presence of air and moisture, at ordinary temperatures. Neither 
 of these reactions, however, can explain the origin of the acid in the 
 springs of Tuscarora and Niagara, or the similar ones in Western New 
 York. These waters are not thermal, and rise from undisturbed and un- 
 altered Silurian rocks, far removed from any volcanic region. They con- 
 tain from two to four thousandths of sulphuric acid, with small portions of 
 soluble sulphates, and are accompanied with carburetted and sulphuretted 
 hydrogen gases. It is possible that the origin of the sulphuric acid in 
 these waters is due to the decomposition of a sulphate, such as gypsum, 
 by the action of silica and water, under the influence of an elevated tem- 
 perature, and at a great depth. The sulphuric acid would either be set 
 free without decomposition, or be resolved into sulphurous acid and oxygen, 
 which would re-combine in their upward progress through the strata. 
 
 CARBONATES AND CARBONIC ACID. 
 
 The most interesting facts connected with the carbonates of lime 
 and magnesia in mineral waters, have already been mentioned in 
 speaking of these bases. The absence of free carbonic acid from the 
 mineral springs of Canada, is remarkably evident in the want of dissolved 
 carbonate of lime in the waters of the first class, which flow from lime- 
 stone rocks ; nor do any of the other waters offer that excess of car- 
 bonic acid, which gives to certain springs, like those of Saratoga, their 
 acidulous taste and sparkling appearance. The waters of the St. Le'on 
 Spring gave, by direct determination, 1*224 of carbonic acid for 1000 
 parts. Of this, -651 were required to form the neutral carbonates obtained 
 in the analysis ; leaving -673 parts of carbonic acid, or very little more 
 than is required to convert them into bicarbonates. The Caxton Spring 
 gave, in like manner, 1-126 of carbonic acid; of which, -651 are required 
 for the neutral carbonates, leaving only -475 of carbonic acid in excess. 
 Of alkaline waters, the Saline Spring of Varennes yielded -920 parts of 
 
CHAP. XVIII.] WATERS OP MINERAL SPRINGS. 557 
 
 carbonic acid ; of which, *451 parts, or very nearly one half, is required to 
 form neutral carbonates. The Gas Spring of Varennes shows, like the 
 Oaxton Spring, a deficiency of carbonic acid. 
 
 Of the waters of Caledonia, in which the carbonic acid was determined 
 with great care at the springs, the Gas Spring contained in 1000 parts, -705 
 of carbonic acid; of which, '856, or a little more than one half, is combined 
 in the form of neutral carbonates. The Saline Spring gave -648 O f Bioarbonat< - 
 carbonic acid, being an excess of -292 over that required to form neutral 
 carbonates ; while in the Sulphur Spring, which contained in 1000 parts, 
 only '590 of carbonic acid, -349 parts are combined as carbonates, leaving 
 only '141 parts for the formation of bicarbonates. In the latter water, as 
 well as in the Gas Spring of Varennes, there is, then, a deficiency in the 
 amount of carbonic acid, so that the bases represented as carbonates can- 
 not all exist in the form of bicarbonates. This deficiency is most marked in 
 the waters which contain the greatest amount of carbonate of soda. It is 
 well known, however, that an excess of carbonic acid is not necessary to 
 retain carbonate of magnesia in solution. Carbonate of magnesia is solu- 
 ble to a considerable extent in an excess of carbonate of soda, or of 
 chlorid of magnesium ; and a large quantity of magnesia may be held in 
 solution in the form of a sesqui-carbonate, as shown in the case of the 
 Plantagenet water submitted to spontaneous evaporation (page 552). The 
 small amount of carbonic acid in these waters is explained, when it is con- 
 sidered that the earthy carbonates have been derived from the decom- 
 position of the chlorids in the waters of the first class, by the action of the 
 carbonate of soda contained in the waters of the fourth class. The alka- 
 line salt having been formed from the decomposition of feldspathic matters 
 in the presence of earthy carbonates, probably contains no excess of car- 
 bonic acid. It will still be desirable to determine the amount of carbonic 
 acid in some of the waters of the fourth class, like those of Chambly 
 and of St. Ours. 
 
 The amount of carbonate of soda, as given in the analyses of the alkaline Carbonat* 
 waters, is calculated from the excess of soda over that required to combine 
 with the chlorine and sulphuric acid. Attempts were made to cpntrol these 
 determinations by evaporating the water to dryness to separate the earthy 
 salts, dissolving the residue, and precipitating the alkaline solution with 
 chlorid of barium. From the weight of the carbonate of baryta thus 
 obtained, the amount of carbonate of soda in the liquid was then cal- 
 culated. As thus determined, however, it was always found to be some- 
 what less than that deduced from the excess of soda. The following 
 results were obtained for the amounts of carbonate of soda in certain 
 waters whose analyses are given in tables III and IV, when calculated 
 by the two methods above described ; A, by the excess of soda over the 
 chlorine and sulphuric acid ; B, by the amount of carbonate of baryta: 
 
558 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. XVIII. 
 
 
 Ill, 3. 
 
 III, 6. 
 
 IV, 1. 
 
 IV, 2. 
 
 IV, 3. 
 
 IV, 5. 
 
 A 
 
 4558 
 
 5885 
 
 1-0604 
 
 1340 
 
 1952 
 
 1*135 
 
 B 
 
 2540 
 
 5466 
 
 1-0156 
 
 1125 
 
 1470 
 
 ro7s 
 
 
 
 
 
 
 
 
 It would appear from these results that a portion of the excess 
 must be combined with some other acid, capable of forming a soluble salt 
 with baryta. It was found in the case of the Chambly water, that the 
 precipitate of carbonate contained a sparingly soluble baryta-salt, which 
 was not entirely removed even by long continued washing with water. 
 This was probably a borate of baryta, since salts of boracic acid are 
 now known to be present in all of these alkaline waters. 
 
 SILICA AND SILICATES. 
 
 Silica. 
 
 It will be seen by reference to the tables of analyses, that the mineral 
 waters of the second class always hold in solution small portions of silica, 
 varying from '15 to *60 parts for 100 of solid matters ; and that in those 
 of the third class, there is a larger quantity of the s^ame element, which, 
 up to a certain point, augments with the amount of carbonate of soda. 
 In the following table, the proportions of carbonate of soda and of silica 
 in 100 parts of solid matters, are given for certain springs, whose analyses 
 will be found in Tables III and IV : 
 
 
 Ill, 
 
 III, 
 
 III, 
 
 III, 
 
 III, 
 
 III, 
 
 III, 
 
 III, 
 
 IV, 
 
 iv, 
 
 iv, 
 
 IV, 
 
 
 1. 
 
 4. 
 
 2. 
 
 5. 
 
 6. 
 
 8. 
 
 3. 
 
 
 
 2. 
 
 4. 
 
 1. 
 
 3. 
 
 Carb. Soda. 
 
 6 
 
 1-6 
 
 2-4 
 
 3-4 
 
 7-0 
 
 8-0 
 
 9-2 
 
 21-0 
 
 25-0 
 
 30-0 
 
 50-0 
 
 56-0 
 
 Silica 
 
 4 
 
 4 
 
 6 
 
 6 
 
 1*6 
 
 1-6 
 
 1-7 
 
 2-9 
 
 3-0 
 
 3-2 
 
 3'4 
 
 3-2 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 soda. 
 
 The amount of silica which these waters contain, does not in any case 
 exceed one or two ten-thousandths ; and it is well known that water at the 
 ordinary temperature may dissolve very much more than this amount of 
 snicate of silica, even in presence of alkaline chlorids and bicarbonates. Carbonic acid 
 expels silica from its combination with soda, at ordinary temperatures ; but 
 at the boiling-point the affinities are reversed, and silicate of soda is regene- 
 rated. At that temperature, however, a mutual decomposition takes place 
 between the silicate of soda, and the carbonates of lime and magnesia, 
 giving rise to silicates of these bases, which are sparingly soluble in water. 
 Hence it happens that when a water, like those of the third and fourth 
 classes, containing dissolved silica, with carbonates of lime, magnesia, and 
 soda, is boiled, there is deposited, with the earthy carbonates, a portion of sil- 
 icates. In the case of the Beloeil water, the precipitate obtained by boiling, 
 
CHAP. XVIII.] WATERS OF MINERAL SPRINGS. 559 
 
 gave with hydrochloric acid a clear solution, from which gelatinous silica 
 
 was afterwards separated. A portion of the earthy silicates is, however, silicates ot 
 
 lime and 
 
 retained in solution, even to an advanced stage of the evaporation. It ma egia 
 was found that the water from Gillan's Spring in Fitzroy, which had been 
 evaporated to one tenth and filtered, became turbid by farther boiling, and 
 gave a flocculent precipitate, which consisted of silica combined with lime 
 and magnesia. A similar reaction was observed with the Varennes and 
 other saline waters ; and likewise with the waters of the St. Lawrence and 
 Ottawa Rivers, to be described farther on. 
 
 The proportion of silica thus held in solution, in combination with 
 the earthy bases, is considerable. In the water of Gillan's Spring, 1000 
 parts of which contain '133 parts of silica, the precipitate obtained by 
 evaporating to one tenth, contained *088 parts of silica, leaving *045 parts 
 still in solution, together with portions of lime and magnesia. 1000 parts 
 of the Beloeil water, treated in the same way, deposited -050 parts of 
 silica with the carbonates, retaining -064 in solution. When the water was 
 evaporated to complete dryness in contact with the earthy precipitate, the 
 whole of the silica was obtained in an insoluble form ; but when the carbo- 
 nates were removed from the concentrated alkaline liquid, it was found 
 that by evaporation to dryness, a reaction took place, by which the pre- 
 cipitated silicate of lime was partly decomposed, and the silica was re-dis- 
 solved by the alkaline carbonate ; a result which did not happen when an 
 excess of earthy carbonates was present. When 1000 parts of the 
 Chambly water, containing -073 of silica, were evaporated to one twentieth, 
 042 parts of silica remained in solution. 
 
 There are not wanting observations which confirm the above results. 
 Dr. J. Lawrence Smith noticed the existence of a dissolved silicate of 
 lime, apparently combined with soda, in the concentrated alkaline waters 
 of Broosa ; and a silicate of lime is deposited from the thermal springs of 
 Weisbaden. The existence of proto-silicates of iron and manganese has 
 been observed in several mineral waters, and the separation of gelatinous 
 silica from certain limonites and ochres, as already described (pages 511 
 and 512), shows the existence of a silicate of iron in these ores. Berzelius 
 observed that a silicate of magnesia separates during the evaporation of 
 the hot alkaline waters of Carlsbad ; and according to Kersten, the carbo- 
 nated waters of Marienbad, when evaporated either at ordinary or elevated 
 temperatures, deposit at first carbonates, and then silicates of lime and 
 magnesia, which gelatinize with acids, like the silicates separated from the 
 Beloeil water (Bischof, Chem. GeoL, i, 4 and 5). This production of sili- 
 cates of lime and magnesia by the evaporation of natural waters, is highly 
 interesting in a geological point of view, since it explains the formation of 
 many natural silicates, such as, for example, the deposits of hydrous sili- 
 cate of magnesia, which occur interstratified with unaltered fresh-water 
 
560 GEOLOGY OF CANADA. [CHAP. XVIII. 
 
 tertiary strata in France and elsewhere. To the metamorphism of such 
 silicates may be due the formation of steatites, serpentines, and many 
 allied minerals. 
 
 BORATE8 AND PHOSPHATES. 
 
 The frequent occurrence of small portions of boracic acid in natural 
 waters has only been made known within a few years ; and since that time, 
 all the alkaline waters of Canada which have been examined, have shown the 
 presence of borates, by the power of the evaporated water to redden tur- 
 meric paper in the presence of free hydrochloric acid. This reaction is 
 particularly marked with the waters of the fourth class ; but it has also been 
 observed with some of those of the second class, as in Lefort's Spring 
 from Baie du Febvre. In speaking of the alkaline carbonates (page 558), 
 allusion has already been made to the fact, that a portion of the soda 
 which is represented as carbonate, in these waters, appears to be in combi- 
 nation with boracic acid. As no direct process for separating this acid 
 is known, its determination must be effected by indirect means. The 
 alkaline water of Joly gives a strong reaction of boracic acid ; and having, 
 by evaporation, obtained a quantity of its saline matters, the silica was 
 separated by carbonate of ammonia, and the chlorine by carbonate of 
 silver. There was thus obtained a mixture of salts of soda and potash, 
 combined only with carbonic, sulphuric, and boracic acids. By directly 
 determining all the other ingredients, the boracic acid was calculated from 
 the loss, and wa? found equal to -028 parts in 1000 parts of the water, 
 which contained -752 of solid matter. By the use of bicarbonate of baryta 
 to separate the sulphuric acid from the mixed salts, the above process 
 of analysis might be simplified. 
 
 Phosphoric The presence of traces of phosphates in these waters has been alluded 
 to on page 554. They are probably never alsent; and in some of the 
 alkaline waters, they may exist in larger quantities than has been 
 supposed. In the case of Gillan's Spring in Fitzroy, the amount of 
 phosphoric acid was found to be equal to -0087 parts in 1000 of the water. 
 
 ORGANIC MATTERS. 
 
 organic The alkaline waters, although colorless when recent, generally become of 
 matters. ft k rowiugn ..y e ii ow color when boiled. This change appears to be due to 
 the presence of some organic matter, which is modified by the action of the 
 alkaline carbonate. When a litre of the Chambly water was evaporated 
 to one sixth, and separated by filtration from the earthy salts, it had a 
 clear bright brown color, which the addition of a slight excess of acetic 
 acid rendered paler, without causing any precipitation. Acetate of 
 copper then threw down a brown precipitate, having the characters of 
 apocrenate of copper, and corresponding to *0043 of apocrenic acid. The 
 filtrate, treated with carbonate of ammonia, gave no evidence of crenic acid. 
 
CHAP. XVIII.] WATERS OF MINERAL SPRINGS. 561 
 
 GEOLOGICAL DISTRIBUTION OF MINERAL SPRINGS. 
 
 The great palaeozoic area of Canada has been shown to be divided into 
 two secondary basins, by an axis extending from Deschambault on the St. P 8ition - 
 Lawrence, in a south-west direction, to Lake Champlain. The eastern part 
 of the western basin is more or less affected by undulations, which are 
 subordinate to the great fault that brings up the Quebec group against 
 the Hudson River formation, and by others of minor importance. It is 
 in this disturbed region that by far the greater number of the mineral 
 springs occur ; and although it is often difficult to establish the presence, or 
 to trace the extent of the faults in the stratification, on account of the 
 alluvial deposits which generally cover the Lower Silurian rocks of 
 the region, it is evident that in a great number of cases the mineral 
 springs occur along the lines of disturbance, and it is probable that a con- 
 stant relation of this kind exists. 
 
 As the south-eastern limit of the western basin is approached, the mineral 
 springs become more numerous ; but this boundary once passed, a region 
 is soon reached where the rocks have become profoundly altered, and fur- 
 nish no more mineral waters. The great western portion of the occidental western 
 basin, which is less disturbed, presents but very few mineral springs; Canada - 
 although the wells which have been sunk at Kingston, Hallowell, St. 
 Catherines, and elsewhere, show that the rocky strata of this region are 
 charged with saline waters. Of the waters of Western Canada, those of 
 Ancaster rise from the Niagara, and those of Brant and Charlotteville from 
 the Corniferous formation. Of the acid springs of the fifth class, those of 
 Tuscarora and Chippewa issue from the Onondaga formation, and those of 
 Niagara and St. David's from the Medina. With these exceptions, all of 
 the mineral waters noticed in the preceding descriptions, issue from Lower Eastern 
 Silurian rocks. Of the alkaline waters of the third and fourth classes, of Canada, 
 which twenty-one have been examined, those of Caledonia rise from the 
 , Trenton group, and that of Fitzroy from the Chazy or the Calciferous 
 formation ; to which last, or to the Potsdam formation, the waters of Ste. 
 Martine, and those of Rawdon, are probably to be referred. All the 
 others of these classes belong to the Hudson River formation ; except those 
 of Varennes and Jacques Cartier, which appear to rise from the Utica 
 formation, and those of Ste. Anne and Quebec, which issue from the 
 Quebec group of rocks. 
 
 Of the waters of the second class, of which more than thirty have been 
 examined, those of La Baie, Sabrevois, and perhaps St. Le*on and Assump- 
 tion, rise from the Utica or the Hudson River formation ; while the others 
 issue from the Trenton, Chazy, Calciferous, or Potsdam formation. The 
 neutral saline waters of Ste. Anne and Rividre Ouelle, and several similar- 
 
 LL 
 
562 GEOLOGY OF CANADA. [CHAP. XVIII. 
 
 saline springs at Cacouna and Green Island, rise from the rocks of the 
 Quebec group. 
 
 Origin of Setting aside for the moment the waters of the Quebec group, it would 
 appear, that, for the other springs of the first four classes, the source of the 
 neutral salts, consisting of alkaline and earthy chlorids, is in the limestones 
 and the other strata, from the Potsdam to the Trenton group inclusive ; while 
 the alkaline carbonates are derived from the argillaceous sediments which 
 make up the Utica and Hudson River formations. These sediments are 
 never deficient in alkaline silicates, whose slow decomposition yields to 
 infiltrating waters the alkaline carbonates and silicates which characterize 
 the waters of the fourth class. These, mingling in various proportions 
 with the brines which rise from the limestones beneath, produce the waters 
 of the second and third classes, in the manner already explained while 
 speaking of the calcareous and magnesian carbonates of these waters. 
 The occurrence of several springs of the third class, like those of 
 Caledonia and Fitzroy, rising from the Lower Silurian limestones, is not 
 surprising, when it is considered that the Chazy formation in the Ottawa 
 valley includes a considerable thickness of shales, sandstones, and argilla- 
 ceous limestones, approaching in composition to the sediments of the Hudson 
 River formation. That great mass of strata which constitutes the Quebec 
 .group, and is regarded as the equivalent of the Potsdam and Calciferous 
 formations, offers, in its lithological composition, successions of limestones 
 and shales similar to those of the higher portions of the Lower Silurian 
 series, and furnishes the same variety of saline and alkaline waters. 
 
 Association As an evidence that the different classes of waters have their origin 
 in different strata, may be cited the fact that springs very unlike in com- 
 position are often found hi close proximity, and apparently rising from a 
 common fissure or dislocation. Thus at Caledonia, three waters of the 
 third class are found within a few feet of each other ; one of them being 
 sulphurous, while the others are not so, and are much more strongly saline. 
 Not far from these rises a very different water, belonging to the second 
 class. At Ste. Anne de la Pocati^re, a spring of the second class, and 
 another of the fourth class, are found not far apart. In Sabre vois, of two 
 springs of the second class, very near together, one contains salts of baryta 
 and strontia, and the other soluble sulphates ; while in the seigniories of 
 Nicolet and Baie du Febvre, six springs have been described, which rise 
 through the Utica formation, along a line, in a distance of three or four 
 leagues. Of these springs, two belong to the second, two to the third, 
 and two to the fourth class ; these last being probably derived entirely from 
 the shales, while the others have their source in the underlying limestones. 
 The great rarity of mineral springs in the uncomparatively undisturbed 
 region of Western Canada has already been alluded to. The waters of 
 Scarborough and of Brampton probably do not rise from the palaeozoic 
 
CHAP. XVIII.] WATERS OP MINERAL SPRINGS. 563 
 
 rocks, but derive their feeble saline impregnation from the overlying clays 
 and sands. 
 
 The extended series of analyses here given, offers many points of inter- 
 est. Nowhere else, has such a complete systematic examination of the 
 waters of a region, and of a great geological series been made ; and an addi- 
 tional importance is given to the results from the fact, that the waters are 
 derived from palaeozoic strata, which prepares us to find certain points of 
 difference between these waters and those of other countries, for the most 
 part belonging to more recent geological formations. The brine springs Brine springs, 
 of the first class are altogether unlike those of England, Germany, and the 
 state of New York. In all of these, common salt greatly predominates, and 
 the earthy chlorids form but a very small portion of the solid contents ; 
 while in the waters of the first class, these chlorids constitute more than 
 one half of the saline ingredients. The brine springs of other regions are 
 supposed to arise from the solution of rock salt, which occurs in beds, or in 
 crystals disseminated through the strata, as in the saliferous marls of the 
 Onondaga formation. In the process of crystallization the common salt 
 separates from the earthy chlorids ; and hence the brine springs of New 
 York, which have their source in this formation, are solutions of chlorid of 
 sodium, with but very little impurity. The brine springs of the Lower Silu- 
 rian limestones, on the contrary, may be supposed to represent the com- 
 position of the ancient ocean in which these early strata were deposited. 
 The action of the carbonate of soda from feldspathic rocks, through long 
 ages, has since decomposed the greater part of the chlorid of calcium of 
 the ocean, replacing it by chlorid of sodium, and forming the carbonate 
 of lime of which vast limestone formations have been built up. The 
 analyses by Lenny, of some waters from deep wells in the Carboniferous 
 series on the Alleghany river, show the existence of brines which resemble 
 those of Whitby and Hallowell, in containing large amounts of chlorids of 
 calcium and magnesium, and traces of baryta, sulphates being invariably 
 absent. (Bischof, Chem. Geology, i, 377.) 
 
 The mineral waters of the second class, which are distinguished by con- 
 taining a large proportion of carbonate of magnesia, and but very little 
 carbonate of lime, seem, from the numerous analyses of Berzelius and 
 Struve, to be very rare in Germany. The relations of these lime and 
 magnesia salts have already been discussed. Since it has been suggested 
 that these waters have been formed by the action of alkaline salts upon 
 waters of the first class, it may be asked why more examples have not 
 been given of springs which contain, at the same time, large amounts of 
 earthy carbonates, and considerable portions of chlorids of the same bases, 
 indicating a composition intermediate between the waters of the first class, 
 and those of St. Le*on, Plantagenet, and Lanoraie. To this, it is to be 
 said, that the object of these analyses having been primarily the exami- 
 
564 GEOLOGY OF CANADA. [CHAP. XVIII. 
 
 nation of those springs which had attracted attention as medicinal waters, 
 the more bitter saline springs have been to a great extent neglected. 
 The Whitby Spring, however, contains a portion of carbonates; and the 
 bitter salines of Rividre Ouelle and of Kingston apparently represent waters 
 intermediate between the first and second classes. It should here be 
 observed, that the springs which have been examined make but a small 
 portion of those which are known or reported to exist in the country. 
 
 Economic The saline springs of the first class are too much charged with earthy 
 chlorids to be suited to the manufacture of common salt ; while those of the 
 second class contain too small a proportion of salt to be employed with 
 advantage. It is not impossible that the large amount of alkaline carbon- 
 ates in some of the springs of the fourth class might be made economically 
 available, provided that the waters were concentrated, during the heats of 
 summer, by solar evaporation. The supplies of dilute sulphuric acid fur- 
 nished by the waters of the fifth class might also be found of value, in 
 their vicinity, for manufacturing purposes. 
 
 Medicinal In a medicinal point of view, the mineral waters of Canada are already 
 known to a considerable extent ; but they are generally employed without 
 much reference to the great variations in their composition. Among 
 saline waters, those containing considerable quantities of earthy 
 chlorids must evidently possess medicinal properties very different from 
 those in which large amounts of carbonate of soda are present. The salts 
 of iodine, which are rarely absent, and are found in such unusually large 
 quantities in the saline waters of Ste. GeneviSve, and the salts of baryta 
 and strontia which occur those of St. Le*on, Lanoraie, Varennes, and many 
 other springs, are also especially worthy of consideration in a therapeutic 
 point of view. 
 
 Thermal None of the mineral springs of Canada, so far as they have yet been 
 
 waters. examined, offer any considerable elevation of temperature above the mean 
 of the region in which they occur. Few of these springs are very copious, 
 and the water in their basins is consequently subject to more or less 
 modification from atmospheric influences. The annual mean temperature of 
 Montreal, as deduced from the observations of twenty-seven years, is, 
 according to Dr. Archibald Hall, 44 -6 F. ; while the temperature of the 
 Caledonia springs was found to vary from 44-5 to 46 d , that of St. Le*on 
 being 46, and Caxton -49. The temperature of the Varennes springs 
 has already been noticed, of which the saline was 47 *5. The two springs 
 of Chambly, taken under favorable conditions, gave each a temperature of 
 53 ; so that many of these waters are to be regarded as slightly thermal. 
 
CHAP. XVIII.] WATERS OF MINERAL SPRINGS. 565 
 
 WATERS OF THE ST. LAWRENCE AND OTTAWA RIVERS. 
 
 Analyses of the waters of the St. Lawrence and Ottawa Rivers were 
 made in 1854, with reference to the supply of water for Montreal. Inde- 
 pendent of their local value, the results are important as showing the com- 
 position of two immense rivers, which drain a large portion of the continent. 
 These waters were collected in the month of March, before the melting of the 
 snows had commenced. That of the Ottawa was taken on the 9th of water of 
 March, at the head of the St. Anne lock, and was remarkably free from th 
 any sediment or mechanical impurity. Its color was of a pale amber-yellow, 
 very distinct in layers of six inches. When heated, the color deepens, 
 and by boiling, a bright brown precipitate appears, which, when the water 
 is reduced to one tenth, is seen to consist of small brilliant iridescent scales, 
 and consists of carbonates, with silica and organic matter. Meanwhile the 
 water becomes much darker colored, and has an alkaline reaction. A por- 
 tion was reduced to one fortieth, filtered, and being still farther evaporated, 
 deposited an opaque film, which was imperfectly soluble in hydrochloric 
 acid. The concentrated liquid was now dark brown and alkaline, red- 
 dening turmeric paper. It was evaporated to dryness, and gave a deep 
 brown residue, which carbonized without deflagration, giving off an 
 agreeable vegetable odor, and leaving a little carbon. The soluble portion 
 of the ignited residue was alkaline to the taste. The insoluble portion did 
 not effervesce with hydrochloric acid, which removed from it a portion of 
 lime, but no magnesia, leaving a residue of pure silica, and showing it to 
 be a silicate of lime. 
 
 The precipitate obtained from the water by ebullition, gives up its coloring organic 
 matter when boiled with a dilute solution of potash, which assumes a bright matter - 
 brown color from the organic substance. This seems to consist in part of 
 crenic acid. When the same precipitate is boiled with hydrochloric acid 
 and a little chlorate of potash, and evaporated to remove silica, the acid 
 solution gives with ammonia a colorless precipitate, which consists in large 
 part of alumina, but contains, besides, an abundance of phosphoric acid, and 
 small portions of iron and manganese. When the concentrated water, with silica, 
 its precipitate, is evaporated to dryness with an excess of hydrochloric acid, 
 and the residue treated with a dilute acid, a large amount of silica is obtained, 
 which after ignition is perfectly white, and equals one third of the solid 
 contents of the water. Examined under the microscope, it is amorphous, 
 like chemically separated silica. 
 
 The recent water gives, with the ordinary tests, only traces of sulphates 
 and chlorids. The proportions of these, and of the other elements, were 
 ascertained by two or more concordant determinations, made upon quanti- 
 ties of two and four litres of the water. The experiments already detailed 
 
566 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. XVIII. 
 
 silicate of 
 
 water of 
 
 show that the concentrated water holds in solution a portion of silicate of 
 lime. Ten litres of the water evaporated to one thirtieth, still retained, 
 thus dissolved, -046 grams of silica, and -013 of lime. The chlorine and 
 sulphuric acid are sufficient to neutralize only about one half of the alkaline 
 bases present. The remaining portion, which is represented below as car- 
 bonate of soda, may be considered as in part combined with silica and with 
 an organic acid. 
 
 The water of the St. Lawrence was collected on the 30th of March, on 
 tne soutn ^de f tne P om te des Cascades, Vaudreuil. It was clear and 
 transparent, and, unlike the water of the Ottawa, exhibited no color when 
 in layers of several niches in thickness. When boiled, it lets fall a white 
 crystalline precipitate, which adheres to the sides of the vessel ; and the 
 liquid, which is turbid from a little suspended yellow matter, is but slightly 
 colored. The reactions for chlorine and sulphuric acid were much more 
 distinct with this than with the Ottawa water, and the dried residue con- 
 tains much less organic matter. The residue from two litres sufficed to 
 give the reactions of iron and manganese : the ammoniacal precipitate was 
 however chiefly alumina, with some phosphoric acid. Like the Ottawa 
 water, this retains in solution a portion of silicate of lime. When evapo- 
 rated to one fortieth, ten litres contained -075 grams of silica, and -028 of 
 lime. The determinations for the two waters are given below, the alkalies 
 being represented as chlorids. They are as follows for 10,000 parts : 
 
 Ottawa. St. Lawrence. 
 
 Carbonate of lime, ................. -2480 -8033 
 
 " magnesia, ............ -0696 -2537 
 
 Chlorine, ......................... -0076 * -0242 
 
 Sulphuric acid, .. .................. -0161 -0687 
 
 Silica, ............................ -2060 -3700 
 
 Chlorid of sodium, ................. -0607 -1280 
 
 " potassium, ............... -0293 -0220 
 
 Residue dried at 300 F., ........... -6975 1-6780 
 
 " ignited, ................... -5340 1-5380 
 
 In the following table are given the results, calculated in like manner for 
 10,000 parts, the excess of soda being represented as carbonate : 
 
 Ottawa. St. Lawrence. 
 
 Chlorid of potassium, ............... '0160 -0220 
 
 " sodium, ........... f ......... -0225 
 
 Sulphate of potash, ................. -0122 .... 
 
 " soda, .................. -0188 -1229 
 
 Carbonate of " .................. -0410 -0061 
 
 " lime, .................. -2480 -8083 
 
 " magnesia, ........ ..... -0696 -2537 
 
 Silica, ............................ -2060 -3700 
 
 Alumina and phosphoric acid, ....... traces traces 
 
 Oxyds of iron and manganese, ....... " " 
 
 6116 
 
 1-6055 
 
CHAP. XVIIL] WATERS OP MINERAL SPRINGS. 567 
 
 In the water of the Ottawa the amount of chlorine is not sufficient to 
 saturate the potash, and the excess of this tihse is therefore given as sul- 
 phate. In the water of the St. Lawrence, on the contrary, the chlorine 
 suffices not only for the potash, but for a portion of the soda. 
 
 The difference in the color of the waters of the two rivers is very 
 distinctly marked in front of the island of Montreal, a long distance below 
 their junction ; but in the amber-colored waters before the city, the current 
 of the Ottawa has already become mingled with a large proportion of the 
 St. Lawrence water. This is shown by some analyses made in 1854. 
 In I are given the determinations made of the water taken at Lower 
 Lachine, about thirty feet from the shore, and opposite to the entrance to 
 the present aqueduct, on the 9th of March, the same day as the Ottawa 
 water whose analysis is given above. II is the water which was, at that 
 time, raised by pumping from the river in front of the city. It was taken 
 on the 15th of March. Ill was also from the city supply hi April, 1850, 
 when the spring floods had increased the volume of the Ottawa river, 
 and consequently the proportion of its water in front of the island. These 
 are given, as before, for 10,000 parts. 
 
 I. II. in. 
 
 Carbonate of lime, -6440 -7400 -4228 
 
 " magnesia, -1910 -2160 -0989 
 
 Chlorine, -0183 -0296 -0296 
 
 Sulphuric acid, -0487 -0498 -0447 
 
 Silica, -3250 -3450 undet. 
 
 Residue dried at 300 F., . . . 1-4150 1-5600 
 
 " ignited, 1-2020 1-3750 " 
 
 The amount of chlorine in the city supply on the 14th of April, 1854, 
 was -0284. The proportion of chlorine found in the water before the city, 
 being greater than that of the unmixed St. Lawrence water, indicates a 
 local source of this element, which was probably due to the sewerage of the 
 town,Vhose waters, impregnated with alkaline chlorids, were carried near 
 to the supply-pipe for the old water-works. 
 
 The comparison of the waters of the two rivers shows the following differ- comparison 
 ences : the water of the Ottawa, containing but little more than one third of the two 
 
 wfttcrs 
 
 of the solid matter of the St. Lawrence, is impregnated with a much larger 
 quantity of organic matters, and contains a large proportion of alkalies 
 uncombined with sulphuric acid or chlorine. Of these bases, determined 
 as chlorids, the chlorid of potassium in the water of the Ottawa forms 
 thirty-two per cent., and in that of the St. Lawrence only sixteen per cent. 
 In the former, the silica equals thirty-four per cent., and in the latter 
 twenty-four per cent., of the mineral matter. 
 
 The Ottawa flows through a region of crystalline rocks, and receives 
 from them the greater part of its waters. It also drains great areas of 
 
568 GEOLOGY OF CANADA. [CHAP. XVIII. 
 
 forest and of marsh, and from the decomposition of the vegetation derives 
 the organic matters, and the great proportion of potash salts which it con- 
 tains. The St. Lawrence, at its source, in Lake Superior, drains a region 
 of ancient sandstones and crystalline rocks ; but it afterwards passes 
 through lakes whose basins are composed of palaeozoic strata abounding 
 in limestones, which are rich in gypsum and salt. It is these rocks 
 that give to the waters of the river that predominance of soda, sulphuric 
 acid, and chlorine which distinguishes it from the Ottawa. Both of these 
 great rivers flow through a series of lakes, in which the waters are 
 enabled to deposit their suspended impurities, and are thus rendered 
 remarkably clear and transparent. 
 
 silica and ^ ne g 1 * 6 ^ proportion of silica and of potash carried down to the 
 potash. ocean by these rivers, the latter amounting, even in the St. Lawrence, to 
 one sixth of the alkaline salts, is particularly worthy of consideration, in 
 connection with the small proportion of these elements which the ocean 
 waters contain. Silica is doubtless never wanting in river waters, though it 
 has hitherto been, in most cases, wholly or in great part overlooked, except 
 by Deville, in his analyses of the river waters of France. It is interesting to 
 contrast this large proportion of silica in the Ottawa and the St. Lawrence, 
 with the small amount of it found in the mineral waters of the second, 
 third, and fourth classes. The soda from the decomposition of the feld- 
 spars in sedimentary strata, is liberated in the form of a silicate, which is 
 decomposed, in its passage towards the surface, by compounds of lime and 
 magnesia ; giving rise, in this manner, to insoluble silicates of these bases, 
 which remain behind, and to soluble soda-salts. 
 
CHAP. XIX.] GEOLOGY OF CANADA. 5(59 
 
 CHAPTER XIX. 
 
 ON SEDIMENTARY AND METAMORPHIC ROCKS. 
 
 GENERAL CONSIDERATIONS; DECOMPOSITION OF ROCKS; ACTION OF WATERS; VEGETATION; 
 SOLUTION OF IRON; PROCESS OF REDUCTION; DEPOSITION OF SILICA; CARBONATES OF LIMB 
 AND MAGNESIA; GYPSUMS; CLASSIFICATION OF SEDIMENTS; NATURE AND THEORY OF THK 
 METAMORPHISM OF ROCKS . LAURENTI AN ROCKS . HURONI AN ROCKS ; PALEOZOIC ROCKS 
 OF THE EASTERN DISTRICT; PALAEOZOIC ROCKS OF THE WESTERN DISTRICT. CLAYS ANI> 
 SOILS; PEATS. 
 
 It is proposed in the present chapter to consider the chemical and 
 mineralogical composition of the stratified rocks of the province, and the 
 nature of that metamorphism to which portions of them have been 
 subjected. The distribution and the general characters of these rocks 
 have been given in the preceding part of this volume, and, in another 
 chapter, the principal mineral species which they contain have been noticed 
 in detail. The stratified rocks of Canada are especially interesting, 
 inasmuch as they include crystalline or metamorphic strata belonging P Wc 8trata - 
 to three great geological periods. These are distinguished by remarkable 
 mineralogical differences, which are apparently connected with the greater 
 or less antiquity of the formations. 
 
 So long as all crystalline stratified rocks were classed together under 
 the designation of primitive, and were supposed to belong to a period 
 anterior to the fossiliferous formations, the studies of the lithologist were 
 confined to descriptions of the various species of rocks, without any refer- 
 ence to their stratigraphical or geological distribution. Since however the 
 fossiliferous strata have been studied with reference to the great principle 
 of the succession of organic life, the palaeontologist has learned that the 
 fossils of each formation furnish a guide to its age and stratigraphical 
 position. Investigations have also shown that sedimentary strata of aD 
 ages, up to the tertiary inclusive, may undergo such changes as to obliterate 
 the evidences of organic life, and give to them the mineralogical characters 
 once assigned to primitive rocks. The question now arises, whether, in 
 
570 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 the absence of organic remains, or of stratigraphical evidence, there 
 exists any means of determining, even approximately, the geological age 
 of a given series of crystalline stratified rocks, or the date of its metamor- 
 phism ; in other words, whether the chemical conditions which have pre- 
 sided over the formation of sedimentary rocks, have so far varied, in the 
 course of ages, as to impress upon these rocks marked chemical and min- 
 eralogical differences. 
 
 chemical It cannot he doubted, that in the earlier periods of the world's history, 
 chemical forces of certain kinds were much more active than at the present 
 day. Thus, the decomposition of earthy and alkaline silicates under the 
 combined influences of water and carbonic acid, would be greater when this 
 acid gas was more abundant in the atmosphere. The larger amounts of alka- 
 line and earthy carbonates then carried to the sea from the decomposition of 
 these silicates, would furnish a greater abundance of calcareous matter to 
 the sediments ; and the chemical effects of vegetation, both on the soil and 
 the atmosphere, must have been much greater during the carboniferous 
 period than at present. 
 
 In the decomposition of the feldspars, which may be represented as sili- 
 
 con of feid- G ^ Q O f afamina. combined with silicates of potash, soda, and lime, the alkali 
 or lime is removed hi combination with a portion of silica ; and there remains, 
 as the final result of the process, a hydrated silicate of alumina, or clay. 
 The potash feldspar, orthoclase, is, under ordinary conditions, much less sub- 
 ject to such a decomposition than the soda feldspar, albite, or those which, 
 like labradorite, contain both lime and soda. Both Mitscherlich and Bischof 
 have remarked that where albite and orthoclase are associated, the former 
 may be found decomposed and friable, while the latter is still unaltered. 
 This change of feldspar is favored by mechanical division, which multiplies 
 the surfaces exposed ; so that when a feldspathic rock is triturated with 
 water, small portions of silica and of alkalies are taken into solution. If 
 the decomposing rock contains, like many granites, both potash and soda 
 feldspar, the latter, being first attacked, will be rendered friable, and event- 
 ually reduced to the condition of clay, with the loss of more or less of its 
 alkali, and, being readily held in suspension in the water, will become 
 mechanically separated from the heavier portions. These, consisting of 
 grains of unaltered orthoclase, with quartz, will form a sandy sediment, 
 apart from the lighter clays ; while the soda and lime, with the dissolved 
 silica, are removed by the water. Such a separation is necessarily but 
 a partial one ; for the feldspar, thus broken up and reduced to a clay, still 
 retains a considerable portion of alkali, and is moreover mingled with the 
 more finely divided parts of the orthoclase and quartz. This process 
 is evidently that which must go on in the wearing of rocks by the agency 
 of water ; and, explains the fact, that while quartz, or an excess of silica, is 
 for the most part wanting in rocks which contain a large proportion of 
 
CHAP. XIX.] SEDIMENTARY AND METAMORPHIC ROCKS. 571 
 
 alumina, it is generally abundant in those where potash feldspar predomi- 
 nates. Daubre'e has remarked, that by the prolonged attrition of frag- 
 ments of granite under water, the feldspar, being softer and more readily 
 divisible, is eventually in great part reduced to an impalpable powder, 
 which remains for some time suspended in the water, while the grains of 
 quartz are only rounded, and form a readily subsiding sand ; which will 
 however retain some portions of the feldspar. 
 
 The decomposition of aluminous and alkaline silicates goes on, not Alkaline 
 only at the earth's surface and in sediments still suspended in water, but w 
 in stratified sedimentary rocks. The evidence of this is seen in the 
 silica and the alkaline carbonates held in solution by the waters of many 
 mineral springs. Atmospheric waters, permeating strata composed of 
 the ruins of argillaceous rocks, dissolve from them large portions of 
 carbonate of soda, giving rise to alkaline springs and to natron lakes. In 
 these waters, it is found that soda greatly predominates, sometimes almost 
 to the exclusion of potash. This is due not only to the fact that soda feld- 
 spars are more readily decomposed than orthoclase, but to the power of 
 argillaceous sediments to abstract from water the potash salts which it 
 already holds in solution. Thus when a solution of silicate, carbonate, Elements 
 sulphate, or chlorid of potassium is filtered through common earth, the J^^f te 
 potash is taken up, and replaced by magnesia, lime, or soda, by a double 
 decomposition between the soluble potasTi salt, and the insoluble silicates 
 of the latter bases. Soils in the same way remove from infiltrating waters, 
 ammonia, and phosphoric and silicic acids ; the bases which were in combi- 
 nation with these acids being converted into carbonates. The drainage- 
 water of soils, like that of mineral springs, contains only carbonates, chlorids, 
 and sulphates of lime, magnesia, and soda ; all the potash, ammonia, phos- 
 phoric and silicic acids being retained by the soil. 
 
 The elements which the earth extracts from waters are precisely those Action of 
 which are removed from it by growing plants. These, by their decompo- P lantS - 
 sition under ordinary conditions, yield their mineral matters again to the 
 soil ; but when plants decay in water, these become dissolved, and hence the 
 waters of peat bogs and marshes are remarkable for the large amounts of 
 potash and of silica which they contain. The considerable extent of 
 such lands drained by the Ottawa River explains the predominance of 
 these elements in its waters (page 568). The result of such a pro- 
 cess is, through the decomposition of terrestrial vegetation, to carry large 
 amounts of potash salts and silica to the sea ; but here the agency of 
 organic life prevents their accumulation. While foraminifera appropriate 
 the silica for the formation of their shields, marine plants take up the 
 potash. According to the analyses of Forchammer, these are very rich in 
 mineral matters, in which potash salts predominate ; and the same appears 
 to be true of fresh-water plants, like duck-weed. When these aquatic 
 
572 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 plants are thrown upon the shores, or sink, and become buried beneath 
 the mud in the ocean's bottom, the potash set free during their decay will 
 be taken up by the argillaceous matters, and rendered insoluble. Thus, as 
 Forchammer has shown, the fucoidal shales of the palaeozoic series of 
 Scandinavia are peculiarly rich in potash, which has doubtless in part been 
 derived from the sea-water, through the agency of marine vegetation. 
 The formation of glauconite or green-sand, which is essentially a hydrous 
 silicate of iron and potash, is still going on in the sea, in virtue of reactions 
 as yet unknown (page 486), and must, in like manner, be continually 
 abstracting potash from the sea-water. 
 
 Fire-clays. The fire-clays (under-clays) of the coal formation, which are beneath 
 each bed of coal, are argillaceous sediments almost entirely devoid of 
 alkalies, and represent the ancient soil in which the luxuriant coal vegeta- 
 tion flourished, and apparently deprived it of the greater part of its potash. 
 From the coal itself, as from modern peats, the alkalies appear to have been 
 almost entirely removed by the action of water. These fire-clays, which 
 still retain the traces of their ancient vegetation, in the stigmariae which 
 they enclose, are not to be confounded with those deposits of kaolin which 
 in certain cases result from the direct and rapid decay of feldspathic rocks, 
 under conditions as yet imperfectly understood. The products however do 
 not differ essentially from those of the process above considered. 
 
 The coarser sediments, in which quartz and orthoclase prevail, are neces- 
 sarily more readily penetrated by water than the finer argillaceous deposits, 
 which are nearly impermeable. Hence, while the latter retain all the 
 alkalies, the lime, magnesia, and iron-oxyd which they carried down with 
 them, these elements, with the exception of the potash, are gradually re- 
 moved by solution from the coarser sediments. But when once these 
 mechanical deposits have been rendered crystalline by metamorphism, both 
 their permeability and their alterability are greatly diminished ; and it is 
 only when they are again broken down by mechanical agencies to the 
 condition of soils and sediments, that they become once more subject to the 
 Alkalies and chemical changes which have just been described. Hence the mean com- 
 Bma> position of the argillaceous sediments of any geological epoch, or, in other 
 words, the proportion between the alkalies and the. alumina, will depend 
 not only upon the age of the formation, but upon the number of times 
 which its materials have been broken up, and the length of the 
 periods during which these have remained unmetamorphosed, and exposed 
 to the action of infiltrating waters. Thus, for example, that portion of the 
 argillaceous rocks of the Lower Silurian series in Canada which became 
 metamorphosed before the close of the palaeozoic period, will have lost less 
 soluble matter than that part which still remains in the form of unaltered 
 shales and sandstones. Of these, again, such portions as remain undisturbed 
 by folds and dislocations will preserve a larger portion of alkalies than those 
 
CHAP. XIX.] SEDIMENTARY AND METAMORPHIC ROCKS. 673 
 
 strata in which such disturbances have favored the formation of mineral 
 springs, which, even now, are active in removing the soluble matters from 
 these rocks. The crystalline Lower Silurian rocks in Canada may be com- 
 pared with those of the Laurentian series on the one hand, and with the 
 Upper Silurian or Devonian on the other ; but when these are to be com- 
 pared with the crystalline rocks of secondary or of tertiary age in the Alps, 
 it cannot be determined whether the material of which these were formed, 
 and which may be supposed, for illustration, to have been directly derived 
 from palaeozoic strata, existed, up to the time of its translation, in a condition 
 similar to that of the altered, or to that of the unaltered Lower Silurian 
 strata of Canada. 
 
 The proportion between the alkalies and the alumina, throughout the variations 
 aluminous silicates of any given formation, is not therefore in direct relation j? on 5omp081 
 to its age, but indicates the extent to which it has been subjected to the 
 action of water, carbonic acid, and vegetation. If however it may be 
 assumed that this action, other things being equal, has, on the whole, been 
 proportionate to the newness of the formation, it is evident that the chemical 
 and mineralogies! composition of different systems of rocks must furnish 
 some guide to their relative ages. In the case of unaltered sediments, it 
 would be difficult to arrive at any conclusion, without greatly multiplied 
 analyses ; but in these same rocks, when altered, the crystalline minerals 
 which are formed, being definite in their composition, may to a certain extent 
 become to the geologist, what organic remains are in the unaltered rocks, 
 a guide to the geological age and succession. 
 
 In considering the influence exercised by vegetation, in its growth and Action of 
 decomposition, upon the composition of sedimentary rocks, the reducing JJJj^j 
 power of decaying organic matter must not be overlooked. In this way, 
 peroxyd of iron is reduced to the state of protoxyd, and then, being dis- 
 solved by carbonic acid, or by some organic acid, is removed from a sedi- 
 mentary deposit, to be again precipitated by oxydation, or by the loss of 
 carbonic acid, either as carbonate of protoxyd of iron, or as a sesquioxyd 
 combined with water, and often with a portion of organic matter, in the forms 
 of iron-stone, ochre, and limonite. Peroxyd of iron being insoluble, the infil- solution of 
 trating waters which take up the soda, lime, and magnesia from sediments, iron oxyd - 
 cannot remove this metal unless they contain organic matter. The evidence 
 of this reducing and dissolving action of organic matter is met with, not 
 only in the fire-clays and iron-stones of the Carboniferous system, and among 
 secondary, tertiary, and modern deposits, but on a gigantic scale in the 
 Laurentian series, where great thicknesses of sediments are found almost 
 destitute of iron ; while beds of iron ore, more extensive than any in subse- 
 quent periods, are evidences of the abundance of organic matters at that 
 period. If these have not been more frequently preserved in the forms of 
 anthracite and graphite, it is because the amount of peroxyd of iron diffused 
 
574 GEOLOGY OP CANADA. [CHAP. XIX, 
 
 through the sediments of the period, furnished the oxygen necessary for the 
 oxydation of the carbon. Inasmuch as the iron ores of these old rocks, in 
 their present forms of magnetite and hematite, are very insoluble, and are 
 so much iron withdrawn from the terrestrial circulation, it is evident that 
 the proportion of this element existing in a diffused state in recent sedi- 
 ments must be less than in those of more remote times. The solution and 
 precipitation of oxyd of manganese probably takes place under conditions 
 similar to those of oxyd of iron (page 507). 
 
 Metallic The chemical agency of organic matters is also apparent in the produc- 
 
 suiphurets. ^ on O f me t a llic sulphurets. These indicate a reduction of the soluble 
 
 sulphates of the waters to the state of sulphurets, which precipitated, in an 
 
 insoluble form, not only iron, but the zinc, lead, and copper which appear 
 
 to have been in solution in the waters in earlier geological periods. In this 
 
 Agent of way may be explained the origin of the fahlbands, and of the beds of metallic 
 
 reduction, guiphurets, which appear to be more abundant in the earlier rocks. These 
 
 sulphurets, being insoluble, except under the influence of atmospheric oxygen, 
 
 the metals thus combined are now removed from the terrestrial circulation. 
 
 All analogies lead to the conclusion that the primeval condition of 'the 
 
 metals, and of sulphur, having been, like that of carbon, one of oxydation, 
 
 vegetable life has been the only agent of their reduction. 
 
 Dissolved The silica is set free from decomposing feldspars, chiefly as silicate of soda, 
 silica. Thi s is in many cases decomposed by carbonates of lime and magnesia, 
 giving rise to silicates of these bases, which, being sparingly soluble, are in 
 great part retained by the sediments, and to carbonate of soda. Hence alka- 
 line mineral waters, even though containing much carbonate of soda, bring 
 comparatively little silica to the surface ; unless they are thermal, when they 
 are sometimes highly charged with it, and give rise to silicious deposits. The 
 case is different in rivers, where the decomposition of minerals and of plants, 
 at the surface, gives rise to waters, in which, like those of the Ottawa and the 
 St. Lawrence, the silica forms a large proportion of the solid matters pres- 
 ent. When these waters are evaporated, the lime and magnesia which they 
 always contain are separated, in part in the form of carbonates, but in part 
 also as silicates of lime and magnesia. 
 
 siiicious The large amounts of silica contained in solution in the waters of some 
 deposits, thermal springs, and of many rivers, are separated when these waters are 
 exposed to spontaneous evaporation, partly as silicates of lime and 
 magnesia, and partly in the forms of crystalline quartz, hornstone, and 
 opal. In many different formations, beds are met with, composed entirely 
 of crystallized grains of quartz, which have apparently been deposited from 
 solution. In other sediments, this element abounds in the form of grains 
 of chalcedony, or as amorphous soluble silica. The beds and masses of 
 chert, flint, hornstone, buhrstone, and many jaspers, have all apparently 
 been deposited from aqueous solutions ; and the menilite or opal, which is 
 
CHAP. XIX] SEDIMENTARY AND METAMORPHIC ROCKS. 575 
 
 found imbedded in the sepiolites of the Paris basin, has had a similar 
 origin. The large quantities of silica which occur in the form of infusorial 
 earth, have also.been held in solution in natural waters. 
 
 The carbonates of lime and magnesia', which enter into the composition carbonates 
 of sedimentary rocks, are derived from the disintegration of limestones and 
 dolomites, from their solution by carbonic acid, or from the action of the 
 latter upon silicious minerals containing lime and magnesia, such as 
 labradorite and pyroxene. The acid for these reactions may be derived 
 directly from the atmosphere, or may come from that subterranean decom- 
 position of carbonates which is connected with metamorphism. A third, 
 and tnore abundant source of the two carbonates, is to be found in the 
 decomposition, by the carbonate of soda in natural waters, of the soluble 
 salts of lime and magnesia contained in sea-water. 
 
 It is evident that the reaction between the carbonate of soda and the 
 chlorids of calcium and magnesium in the sea, must, while forming the car- 
 bonates of lime and magnesia, have greatly augmented the amount of chlorid 
 of sodium, which has thus replaced the earthy chlorids of the primeval 
 ocean. This conclusion is in accordance with the observed composition of 
 the brines which issue from the Lower Silurian limestones, in which only 
 about one half the chlorine is combined with soda, the remainder being nearly 
 equally divided between the lime and magnesia (page 551). The frequent 
 absence of sulphates from these brines leads to the conjecture that they 
 may be derived from the bitterns of the ancient ocean ; from which, by con- 
 centration, the whole of the sulphates had been separated in the form of 
 gypsum. By this reaction, not less than by the formation of sulphur and 
 metallic sulphurets, a large portion of sulphates 'has been gradually 
 abstracted from the waters of the ocean. 
 
 When alkaline waters containing bicarbonate of soda act upon sea-water, carbonate of 
 the lime salts which this contains are first decomposed, and carbonate of ma s ne8ia - 
 lime is precipitated ; accompanied, as in ordinary limestones, by two or three 
 hundredths of carbonate of magnesia. When all the soluble lime-salts 
 have been thus decomposed, a further addition of bicarbonate of soda 
 gives rise to a somewhat soluble bicarbonate of magnesia, which afterwards 
 separates by evaporation as a hydrated carbonate. The carbonate of lime Dolomite, 
 which the alkaline waters generally contain, being precipitated with the 
 magnesian carbonate, the combination of these two subsequently gives rise 
 to dolomite or to magnesian limestones. 
 
 Another source of carbonate of magnesia is the reaction between solutions 
 of bicarbonate of lime and waters containing sulphate of magnesia, from 
 which the soluble salts of lime, such as the chlorid of calcium, have previously 
 been separated in the form of sulphate or of carbonate. In this way, 
 sulphate of lime and bicarbonate of magnesia are formed by double decom- 
 position ; and by the subsequent evaporation of the mixed solution, the 
 
576 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 former salt is first separated in the form of gypsum. At a later stage in 
 the process, the more soluble bicarbonate of magnesia is deposited in the 
 form of hydrated carbonate, and becoming mingled with a portion of carbon- 
 ate of lime, gives rise to the dolomites and magnesian marls which generally 
 accompany beds of gypsum. Both of these processes seem to have been 
 active in every age ; since dolomites, with and without gypsum, belong to all 
 geological periods. These reactions, however, require inland seas, or basins 
 cut off from communication with the ocean ; while, on the other hand, the 
 conditions for the production of carbonate of lime are everywhere found. 
 Hence the amount of lime removed from the sea has been much greater 
 than that of magnesia, and the salts of the latter base are now the more 
 abundant in its waters. (Amer. Jour, of Science [2], xxviii, 170, 365.) 
 From the principles already discussed, it will be seen that the con- 
 stituents of sedimentary rocks may be reduced to the following classes : 
 
 I. Silicious deposits, including those of mechanical origin, which are 
 formed from the ruins of quartzites or quartziferous rocks, such as granite, 
 and constitute most sandstones. Besides these, are the various forms of 
 silica deposited from solution, and already enumerated above. 
 Aluminous II. Silico-aluminous sediments. These are for the most part mechanical 
 sediments. ^ ^ e j r or jg m . an( j their important relations to the chemistry of the sedi- 
 mentary rocks, have already been pointed out. These sediments may be 
 divided into four groups : First, those in which the alumina is combined 
 with the full amount of alkali (chiefly potash) necessary for the formation 
 of orthoclase or of albite : these are often mingled with quartz. Second, 
 finely divided sediments, related to the last, with a considerable excess of 
 silica, and containing a portion of alkalies (the potash generally predomi- 
 nating), insufficient to form orthoclase or albite with the whole of the 
 alumina present. Most argillites belong to this class, and contain, besides 
 a little lime and magnesia, a considerable quantity of oxyd of iron, and a 
 portion of water. Third, sediments which have been derived from soda 
 feldspars more or less completely decomposed, and finely divided, so as to 
 have been separated by the action of water from orthoclase and quartz, 
 thus containing no excess of silica. The decomposition of the feldspars 
 having been attended with a separation of silicate of soda, the amount 
 of silica and alkali diminishes as that of the alumina increases, and the 
 residue approaches to the composition of kaolin. Fourth, sediments 
 resembling the last in the proportions of silica and alumina, but containing 
 a quantity of potash, which equals five or six per cent., or even more. 
 To this group belong the rocks mentioned under the title of agalmatolite. 
 These sediments may perhaps owe their potash to the decomposition of 
 vegetable matters, as has been explained on page 572. The soils which, 
 on the contrary, have been deprived of their alkalies by vegetation, 
 evidently belong to the second group. 
 
CHAP. XIX.] SEDIMENTARY AND METAMORPHIC ROCKS. 577 
 
 III. Silicates of chemical origin. During the evaporation of many Third ciaes. 
 natural waters at ordinary temperatures, hydrous silicates of lime and 
 magnesia are deposited, and, under favorable conditions, accumulations of 
 
 these have given rise to large beds. Their production by the evaporation 
 of the waters of the Ottawa, and of various alkaline mineral springs, has 
 been already noticed (page 559). A hydrous ter-silicate of magnesia, which 
 has been described by the name of sepiolite, occurs in various regions, 
 associated with limestones and clays of tertiary age, and of fresh-water 
 origin. It is the meerschaum of some authors, and the magnesite of 
 others ; but is not to be confounded with the carbonate of magnesia, which 
 is sometimes called by the latter name. The quincite of Berthier, which 
 occurs disseminated in a fresh-water limestone, is a similar compound ; 
 and beds of sepiolite often include carbonates of lime and magnesia. This 
 substance, in its composition, approaches to talc, like which it often has a 
 lamellar structure. Unlike talc, however, it is readily decomposed by 
 acids, both before and after ignition. Although it has not been noticed 
 among the unaltered sediments of Canada, sepiolite is important as 
 probably being the source of the talc and the steatite of crystalline strata. 
 A silicate of lime, similar in its origin to sepiolite, probably exists among 
 unaltered sediments, although it has not yet been recognized. 
 
 Glauconite, which is a hydrous silicate of protoxyd of iron and potash, 
 with variable proportions of alumina, appears to be a chemical deposit 
 from solution. The amounts of the latter base found in glauconite, indicate 
 a solubility of alumina under certain conditions. The hot alkaline spring silicate of 
 of Plombieres, according to Daubre, deposits along its channel an amor- alumina - 
 phous hydrated silicate of alumina, allied to halloysite, of which the ele- 
 ments had been dissolved in the water. Evidences of the solution of a 
 silicate of alumina are also seen in the formation of the minerals allophane 
 and collyrite ; and in the crystalline hydrous silicate of alumina and mag- 
 nesia, which occurs as a recent deposit from the water of certain mines, and 
 has been described by Scheerer under the name of neolite. It is not 
 improbable that similar aluminous silicates, of a like origin, may sometimes 
 be formed in large quantities, and by their alteration give rise to chlorite, 
 as sepiolite doubtless does to talc. 
 
 IV. In the fourth class may be placed the various limestones, dolomites, Fourth cias*. 
 and magnesites, the elements of which are formed by direct chemical 
 processes, already pointed out. In the case of limestones of organic 
 
 origin, the source of the carbonate of lime is still the same. The beds of 
 phosphate of lime in ancient rocks perhaps owe their origin to deposits 
 analogous to the modern accumulations of guano. 
 
 V. In the fifth class may be included the deposits of gypsum, anhydrite, Fifth ciaee. 
 rock-salt, and more rarely of sulphate of magnesia, and of sulphate and 
 carbonate of soda, which have been formed by the evaporation of sea-water, 
 
 MM 
 
678 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 and of other natural waters. To these may be added the deposits of iron, 
 either as carbonate of protoxyd, or as peroxyd, generally hydrated, and 
 with or without organic acids ; together with occasional similar deposits of 
 oxyd of manganese, and of zinc, lead, and copper ; the latter metals as 
 
 Hydrate of carbonates, silicates, or sulphurets. Mixtures of a hydrate of alumina 
 nuna ' ! with hydrous peroxyd of iron, constituting the substance called bauxite, 
 are abundant in the tertiary sediments of the Mediterranean basin; 
 forming large beds, in which the alumina often greatly predominates. 
 These deposits are probably derived from the decomposition of solutions of 
 native alum by alkaline or earthy carbonates. Similar matters, composed 
 chiefly of hydrate of alumina, are often found in the fissures of the chalk in 
 England. Compounds of alumina with organic acids sometimes occur in 
 nature, and indicate that these may occasionally have been the dissolvent ; 
 but the existence of the sub-sulphate of alumina, websterite, in layers and 
 concretionary masses in tertiary clays, points to sulphuric acid as having 
 been, in many cases, the solvent of the alumina. These aluminous com- 
 pounds, although not known in the unaltered strata of Canada, are 
 important as showing the source of the corundum and spinel which occur 
 in the crystalline rocks. 
 
 sixth class. VI. In the sixth class may be included substances of organic origin, 
 such as coal, lignite, peat, and vegetable mould. Matters of this kind, 
 derived from plants, and in some cases apparently from animals, and 
 analogous to lignite in their nature, are occasionally intermingled with 
 calcareous and with argillaceous rocks, giving rise to what are called 
 bituminous shales or pyroschists (page 528). By their alteration, these 
 carbonaceous matters yield graphite. 
 
 Three divi- The great mass of sedimentary strata may, for general purposes, be 
 considered as composed of sandstones, shales, and limestones. In the 
 former are included the sediments of the first class. The shales or clays 
 embrace the argillaceous matters of the second class, while the limestones 
 include the compounds of the fourth class. The various matters of the 
 other classes, although they are mineralogically of great importance, make 
 up but a small part of the mass of sedimentary rocks. Of these three 
 divisions, the shales, and a great part of the silicious rocks, consist of the 
 comminuted and undissolved portions of pre-existing rocks. The elements 
 of the limestones, and of the matters of the third, fifth, and sixth classes, 
 have, on the contrary, been separated from aqueous solutions, or from the 
 atmosphere, with or without the concurrence of organic life. It is scarcely 
 necessary to remark, that mixtures, not only of different classes of sedi- 
 ments, but of various sediments of the same class, constantly occur, thus 
 giving rise to great varieties in the composition of rocks. 
 
 The conditions and modes of combination of the principal chemical 
 elements of the unaltered sedimentary rocks, may now be considered. 
 
CHAP. XIX.] SEDIMENTARY AND METAMORPHIC ROCKS. 579 
 
 The silica exists in combination with alumina in the clays and feldspathic condition 
 sediments, and in sepiolite with magnesia ; but a great proportion is Ol 
 uncombined. The alumina is chiefly united with silica, but is in part, 
 also, as a hydrate. The magnesia, although chiefly in the form of car- 
 bonate, occurs likewise as a hydrated silicate. A portion of lime may 
 also exist in a similar condition ; but with this exception, the lime in sedi- 
 mentary rocks is present in the forms of carbonate and sulphate, or more 
 rarely as phosphate. The alkalies, except such portions as exist in soluble 
 forms, are almost wholly combined with aluminous silicates. Iron occurs 
 chiefly as carbonate, or as a peroxyd, which is often hydrated. Small 
 portions of lime, magnesia, and oxyd of iron, also exist in the condition of 
 silicates, such as hornblende and labradorite, derived from the ruins of 
 crystalline rocks, and mingled with the argillaceous sediments. 
 
 In altered or metamorphic strata, the same elements appear under Minerals of 
 different aspects, and often in different combinations. The alumina exists altered rocks - 
 in part as simple silicates, such as andalusite, kyanite, and pyrophyllite, 
 and in part as double silicates. These include the alkaliferous silicates, 
 such as feldspars, micas, tourmaline, and agalmatolite, passing through 
 scapolite and anorthite, to such double silicates as garnet, epidote, 
 staurotide, chloritoid, chlorite, pyrosclerite, and loganite. To these are to 
 be added the zeolites, which may be regarded as hydrous feldspars ; and 
 the argillites, which are common both to altered and unaltered strata. The 
 aluminous minerals which do not contain silica, such as corundum, emery, 
 diaspore, spinel, and chrysoberyl, may also be mentioned, and some rarer 
 species, including fluorids, like cryolite, and some sulphates and phosphates, 
 like alunite, lazulite, and wavellite. The bases, lime, magnesia, and oxyd 
 of iron, besides entering into the composition of the double aluminous 
 silicates, occur in the various forms of hornblende, pyroxene, and wollas- 
 tonite, as well as in olivine, serpentine, talc, and lievrite. The oxyd of iron, 
 which forms the base of the latter mineral, also appears in the forms of 
 carbonate, and of hematite and magnetite. The limestones and dolomites of 
 metamorphic series, as is well known, contain great numbers of silicious 
 minerals, including both silicates of protoxyds, and double silicates of 
 these with alumina. Similar silicious minerals occur in the gypsums of 
 metamorphic regions. 
 
 One of the conditions of the metamorphism of sediments appears to be conditions 
 an elevation of temperature. As a consequence of the heat of the deeper 
 portions of the earth's crust, the strata, when buried to a certain depth, 
 are subjected to an elevation of temperature ; which, from the average 
 rate of increase, as determined by numerous observations at depths up to 
 more than 2000 feet, may be fixed at about one degree Fahrenheit for every 
 sixty feet. This, taking the temperature near the surface at 46 F., would 
 give 212, or the temperature of boiling water, at the depth of 10,000 feet. 
 
 of altera- 
 tion. 
 
580 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 It is by no means impossible that, beyond the small depth to which we have 
 internal been able to penetrate, the increase may be more rapid. The hypothesis 
 of a cooling globe necessarily leads to the conclusion, that, in earlier 
 geological periods, this augmentation of temperature must have been far 
 greater than at the present day ; so that strata buried to the depth of 
 10,000 feet, during the secondary period, would have been exposed to a 
 temperature much higher than that above supposed. Sedimentary rocks, 
 thus exposed to heat, and permeated, as they always are, by water, will 
 undergo certain chemical changes, the nature of which will vary, both 
 with the composition of the sediments, and that of the waters penetrating 
 them. The limestones, which in the older formations are exclusively of 
 marine origin, will be impregnated with sea-water, holding in solution 
 common salt, together with lime and magnesia in the form of chlorids and 
 sulphates. Similar salts will at first impregnate the accompanying argil- 
 laceous sediments ; but the feldspathic matters which these contain, by 
 their slow decomposition give out a portion of soda in the form of a soluble 
 Alkaline silicate. This decomposes the soluble salts of lime and magnesia present, 
 waters. an ^ then, reacting upon any carbonates of these bases, by a similar 
 decomposition gives rise to carbonate of soda. Hence the mineral waters 
 rising from argillaceous rocks are generally found to be alkaline from the 
 presence of carbonate of soda, which in some cases prevails almost to the 
 exclusion of the other salts of this alkali (page 550). These alkaline 
 waters may eventually penetrate, to a certain extent, the adjacent calca- 
 reous strata, and displace the earthy salts, so that the marine limestones 
 themselves will become impregnated with a solution of carbonate of soda. 
 Nature of By the chemical metamorphism of sedimentary rocks, is meant a change of 
 metamor- form, which results from new combinations, or from new arrangements of 
 their elements. The first and most obvious mode of metamorphism of a 
 rock, is the crystallization of the mechanically divided silicates which it 
 contains. In a sediment composed of the ruins of .a granite, the feldspar 
 may be re-crystallized, and so arranged as to give to the rock the form of 
 granite, granulite, or porphyry. Should the sediment be deficient in alkali, 
 a portion of the silicate of alumina may crystallize in the form of mica, 
 or even of a simple silicate of alumina, like andalusite or kyanite. In like 
 manner, amorphous silicates of lime and of magnesia, whether of mechanical 
 origin or chemically formed precipitates, may, under proper conditions, 
 be crystallized. 
 
 c staiiiza- -*-* 16 * ate researches of Daubre*e have thrown much light on the theory 
 lion of feid- of metamorphism. He found that when kaolin, a hydrated silicate of 
 alumina, was heated in contact with a solution of an alkaline silicate, to 
 a temperature of 400 Centigrade, crystallized feldspar was slowly formed ; 
 and that a foliated mineral, having the characters of a mica or of chlorite. 
 was developed in a certain clay, when this was submitted to the same 
 
CHAP. XIX.] SEDIMENTARY AND METAMORPHIC ROCKS. 581 
 
 treatment. By the action of highly heated waters upon vitreous alkaline 
 silicates, like glass and obsidian, feldspar, pyroxene, and quartz were all 
 obtained in a crystalline form. From solutions of alkalies saturated with 
 silica, a portion of the latter, through a change in the basic relations of the 
 silica, separates, at an elevated temperature, in the form of crystallized 
 quartz. The solvent power of alkaline solutions is farther shown by an 
 experiment of De Senarmont, who found that a solution of bicarbonate of 
 soda, at a temperature of 480 F., under pressure, dissolves sulphate of 
 baryta, and deposits it again in crystals on cooling. Water alone, according 
 to Schafhautl and Wohler, effects, under similar conditions, the solution 
 fend crystallization of quartz and apophyllite. 
 
 The above experiments show that silicate of alumina may combine 
 directly with an alkaline silicate to form feldspar, and that, not only this 
 mineral, but the already-formed silicates of lime and magnesia, may 
 crystallize in the presence of heated alkaline solutions, in accordance with 
 the first mode of metamorphism mentioned above. The origin of those silicates of 
 minerals which consist of silicates of lime, magnesia, and oxyd of iron, or pl 
 of double silicates of these bases and alumina, remains to be considered. 
 Two views of their formation are admissible : In the first place, these 
 silicates may have been deposited at the earth's surface, and at the 
 ordinary temperature. Such compounds have been mentioned as forming First method 
 the third class of sediments, and their subsequent metamorphism may give 
 rise to various silicious minerals. The chemical composition and the struc- 
 ture of sepiolite are such that it may, by crystallization, with the loss of a 
 part of its water, be transformed into talc or steatite. Pyroxene, chlorite, 
 and many other minerals, may have had their origin in the crystallization 
 of natural silicates of aqueous origin. 
 
 The other view is, that the silicates of lime, magnesia, and oxyd of iron, second 
 which enter into these minerals, have been generated during the process method 
 of metamorphism, by reactions between the silicious matters of the sedi- 
 ments, and the intermingled lime, magnesia, and iron, existing chiefly in 
 the form of carbonates and oxyds. A solution of carbonate of soda, at a 
 temperature of 212 F., possesses the power of dissolving silica, even in 
 the form of quartz, disengaging carbonic acid, and forming a soluble silicate 
 of soda. This, in its turn, is decomposed by carbonates of lime, magnesia, 
 and iron, with the formation of a silicate of these bases ; while the regene- 
 rated carbonate of soda is set free to dissolve a new portion of silica, and 
 thus continue the process of converting the carbonates into silicates. In 
 this way, a small portion of carbonate of soda, by its power of dissolving 
 silica, may serve as the medium of converting a large amount of insoluble 
 carbonates into silicates, which may crystallize in the forms of pyroxene, 
 hornblende, wollastonite, and olivine. The presence of a silicate of alu- 
 mina in the sediment would furnish the element necessary for the produc- 
 
582 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XIX. 
 
 tion of labradorite, garnet, epidote, and chlorite. The agency of the 
 liberated carbonic acid, in dissolving the carbonates and bringing them in 
 contact with the alkaline silicate, is also not to be overlooked. (Amer. 
 Jour, of Science [2], xxiii, 437.) 
 
 Altered The direct formation of silicates in sedimentary rocks by a reaction of 
 
 Montreal f *^^ s kind, is placed beyond question by the frequent development of 
 silicated minerals, through local metamorphism. An instructive example 
 of this kind is furnished at Montreal, where the bluish fossiliferous lime- 
 stone of the Trenton group is traversed by dykes of dolerite, which are 
 subordinate to the great intrusive mass of Mount Royal. The limestone, 
 for a distance of a foot or two, is hardened, but retains its bluish 
 tint. Within a few inches, it is changed to a greenish-white color, which 
 is seen to be due to an amorphous mineral disseminated in the white 
 carbonate of lime. The unaltered limestones from the vicinity contain 
 variable amounts of insoluble argillaceous matters. A specimen treated 
 with dilute hydrochloric acid, left a residue of about twelve per cent, of a fine 
 clayey substance, colored by a small amount of carbonaceous matter, and 
 mixed with a little pyrites, which was removed by dilute nitric acid, This 
 residue, after ignition, gave to a solution of carbonate of soda, 9*5 per cent, 
 of its weight of soluble silica ; and the insoluble portion, being submitted to 
 analysis, gave the result I. A portion of the limestone which was near to 
 the intrusive rock, and was hardened and partially altered, was subjected 
 to the action of dilute nitric acid, and gave an insoluble residue, with the 
 composition II. The more thoroughly altered greenish limestone was also 
 treated with dilute nitric acid, which dissolved the carbonate of lime, and 
 left a residue, the analyses of which, from two different portions of the rock, 
 are given under III and IV. 
 
 Silica, 
 
 Alumina, , 
 
 Lime, 
 
 Magnesia, 
 
 Protoxyd of iron, traces 
 
 Potash, 
 
 Soda, 
 
 Volatile, 
 
 99-57 98-77 98-04 95-02 
 
 The residue of the unaltered limestone, including the silica soluble in alka- 
 lies, contains nearly 75*5 parts of silica, and 16-5 of alumina. These, under 
 the influence of the intrusive rock, have become saturated with protoxyd 
 bases, including the small portions of magnesia and of oxyd of iron which the 
 limestone contains. This process evidently involves a decomposition of the 
 carbonate of lime, and the expulsion of the carbonic acid. It is worthy 
 of remark, that, while the unaltered limestone contains a little carbonate of 
 
 I. 
 
 II. 
 
 III. 
 
 IV. 
 
 73-02 
 
 54-00 
 
 42-60 
 
 40-20 
 
 18-31 
 
 14-00 
 
 13-70 
 
 9-30 
 
 93 
 
 16-24 
 
 31-69 
 
 36-40 
 
 87 
 
 5-27 
 
 4-17 
 
 3-70 
 
 .races 
 
 3-60 
 
 4-68 
 
 5-22 
 
 5-55 
 
 3-14 
 
 undet. 
 
 undet. 
 
 89 
 
 1-22 
 
 it 
 
 (i 
 
 .... 
 
 90 
 
 1-20 
 
 20 
 
CHAP. XIX.] SEDIMENTARY AND METAMORPHIC ROCKS. 583 
 
 magnesia, the rock from which III was obtained yielded not a trace of 
 magnesia to dilute nitric acid. II marks an intermediate stage in the 
 process, and shows that the alkalies are still retained in combination with 
 the aluminous silicate. These amorphous silicates, which have been formed 
 by local metamorphism, might, under favorable circumstances, have crys- 
 tallized in the forms of feldspar, scapolite, garnet, pyroxene, or some other 
 of the silicious minerals which so often occur in metamorphic limestones. 
 The agent in producing these silicates of protoxyds, at the expense of the 
 carbonates of the limestone, was probably a portion of alkaline salt, 
 either derived from the feldspathic matter of the limestone, or possibly 
 infiltrated from the contiguous feldspathic rock, whose elevated temperature 
 produced the reaction which has resulted in thus altering this limestone. 
 
 Examples of local metamorphism in sediments, which can be traced to Local meta- 
 the action of adjacent intrusive rocks, are peculiarly instructive, and have moi P Wsmi 
 been studied with great detail by Delesse. They serve to throw much 
 light on the wide-spread regional metamorphism, which has altered great 
 areas of sedimentary rocks, far removed from any intrusive masses. The 
 similarity of the phenomena in the two cases tends to show that heat has 
 been a great agent in alteration, and that the intrusive rock has served 
 only as a local source of heat, which in the case of regional metamorphism 
 has been furnished by the central heat accumulated in deeply buried 
 sediments. 
 
 Mixtures of silica and argillaceous sediments with variable proportions of 
 carbonate of lime, of carbonate of magnesia, and of oxyd of iron, may then, 
 by a reaction similar to that in the limestone just mentioned, give rise to 
 silicates, which may take the forms of pyroxene, hornblende, or serpentine ; 
 or, by uniting with the aluminous silicate, may produce labradorite, garnet, 
 epidote, chlorite, and such like species, which are among the most charac- 
 teristic minerals of metamorphic strata. It will be seen that the two 
 views here proposed to explain the origin of the silicates of protoxyd 
 bases found among metamorphic rocks, are alike admissible. The silicate 
 of magnesia formed in waters, at the earth's surface, and at ordinary tem- 
 peratures, may, by its crystallization, give rise to the same mineral species 
 as is generated, at an elevated temperature, by the reaction between 
 silica and carbonate of magnesia, in the presence of an alkaline solution. 
 Still another source of silicates of lime and magnesia in unaltered sediments, Third method, 
 has been pointed out in a previous page. It is the reaction of the silicate 
 of soda set free from the decomposing feldspars in the sediments, upon the 
 carbonates of lime and magnesia, and also upon the soluble salts of these 
 bases with which it may come into contact. 
 
 Experiments have already shown the effects of heated alkaline solutions, 
 and even of pure water, upon many of the materials of sedimentary rocks. 
 Water, in the presence of an alkaKferous silicious mineral, appears to take 
 
584 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 up a portion of alkali, and acquires new solvent powers. The presence of 
 soluble lime and magnesia salts in excess, might however be supposed to 
 prove an obstacle to metamorphism, although the presence of crystalline 
 silicates imbedded in the gypsum of metamorphic regions, indicates that 
 the sulphate of lime permits the crystallization of ready-formed silicates in 
 its midst. The apparent anomaly, which has been noticed, of seemingly 
 unaltered portions of limestone strata in the midst of the metamorphic 
 rocks of the Alps, and that of similar cases elsewhere, may probably find 
 their explanation in the presence of certain saline elements in the rock ; 
 which prevent change, while in other parts the soluble alkaline matters 
 play the part of a ferment. 
 
 The experiments of Daubre'e upon the crystallization of feldspar in pre- 
 sence of water, were made at a temperature approaching to redness ; but 
 the solution of silica by carbonate of soda, and the conversion of carbonates 
 of lime, magnesia, and iron into silicates, by its aid, may be effected at the 
 heat of boiling water. The observations made by Daubre'e upon the warm 
 
 Hot alkaline alkaline spring of Plombi^res in France, show that its waters, at a tem- 
 perature not above 160 F., have, during the course of centuries, gene- 
 rated crystallized zeolitic minerals, such as harmotome, apophyllite, and 
 chabazite. These species, together with hyalite, fluor-spar, calcite, and 
 arragonite, are found lining cavities in the bricks, and in the concrete of lime 
 and fragments of sandstone, forming the old Roman works surrounding 
 this spring, thus throwing great light upon the formation of these and 
 similar minerals in amygdaloids and other rocks. 
 
 The various silicious minerals of crystalline or metamorphic rocks may then 
 be regarded as having been formed, either by the crystallization and re- 
 arrangement of silicates occurring in the sedimentary strata, 1 or by the union 
 of silica, uncombined, or, united with an insufficient amount of base, with 
 oxyds existing in the sediments, generally in the state of carbonates. In 
 these reactions are included the formation from the materials of sedimen- 
 tary rocks, of feldspars, micas, scapolite, epidote, garnet, tourmaline, kyan- 
 ite, andalusite, staurotide, chlorite, pyroxene, hornblende, olivine, serpen- 
 tine, and talc. These minerals, with quartz, the oxyds of iron, and the 
 carbonates of lime and magnesia, make up the great mass of crystalline 
 rocks, both stratified and unstratified. 
 
 Metamor- From his observations on the local metamorphism at Plombieres, by the 
 
 act i n f tne thermal waters circulating through the masonry, Daubre'e 
 has been led to suppose that hot springs, which may have arisen along lines 
 of dislocation, and been thence diffused throughout great areas of stratified 
 rocks, may have been the agent of wide-spread or regional metamorphism ; 
 and that this may thus have been produced near to the surface of the earth. 
 It is however very difficult to admit the applicability of this theory of 
 metamorphism by thermal springs, to a system of sedimentary rocks like 
 
IHI.P. XIX.] SEDIMENTARY AND METAMORPHIO ROCKS. 585 
 
 lie Laurentian, which, in Canada alone, occupy an area of about 200,000 
 ,quare miles, and in every portion of this, so far as yet examined, are 
 )rofoundly altered. The palaeozoic rocks of eastern North America offer 
 mother example of wide-spread metamorphism, along a belt which extends 
 trom the Gulf of St. Lawrence nearly to the Gulf of Mexico, throughout 
 the whole Appalachian chain, and having a breadth, in New England, of 
 more than a hundred miles. 
 
 Thermal springs seem totally inadequate to produce effects of this kind 
 and extent, and, like the intrusion of igneous rocks, should be looked 
 upon only as a cause of local metamorphism. Heated waters have 
 however doubtless been the agents of regional metamorphism, but in the 
 way already pointed out ; and the necessary heat has been communicated 
 to the strata, not by the circulation of the waters, but by the upward 
 conduction of the internal heat, at a time when great accumulations of 
 sediment covered the strata, which, by subsequent denudation, have been 
 exposed in an altered and crystalline condition. The sediments of the 
 Laurentian system were metamorphosed and denuded before the deposition 
 of the Huronian and Silurian series, so that it cannot now be determined 
 beneath what strata they were buried at the time of their alteration. 
 The case is however different with the palaeozoic rocks of the Appalachian 
 chain. The metamorphic portion of these in Eastern Canada, embraces Metamor- 
 not only the Quebec group, but higher strata, including the Lower {J Canada 
 Devonian ; while, in Massachusetts, a portion of the carboniferous system 
 has been subjected to alteration. Above the horizon of these altered 
 Devonian strata, there is found, both in Gaspe* on the east, and in 
 Pennsylvania on the south-west, a thickness of about 10,000 feet of 
 strata before reaching the coal measures (page 389). There is reason to 
 believe that, at one time, this great volume of strata was continuous over 
 the whole area now occupied by the metamorphic strata, and many thousand 
 feet belonging* to the carboniferous series may then have covered the 
 now altered coal beds of Massachusetts. The accumulation of a great 
 thickness of strata seems to have been a condition both of the corrugation 
 and of the metamorphism of sedimentary rocks. Regions of altered strata 
 appear to be in all cases folded and corrugated. 
 
 A connection has generally been supposed to exist between the meta- Rarity of 
 morphism of a region and the presence of masses of intrusive rock, 
 This condition of things, if it anywhere exists, is however altogether 
 accidental ; since, throughout the altered regions of Canada, unstratified 
 rocks are extremely rare. As will be seen in the succeeding chapter, the 
 great igneous masses of Eastern Canada occur, for the most part, in the 
 unaltered palaeozoic strata. The serpentines, diorites, hyperites, eupho- 
 tides, and granites, which abound in metamorphic regions, have, by most 
 geologists, been regarded as rocks of igneous origin, whereas they appear 
 
586 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 to be, for the greater part, undoubtedly altered sedimentary layers or 
 masses. In the following pages it is proposed to describe, in their 
 order, the stratified rocks of the Laurentian and Huronian systems, to be 
 followed by those of the palaeozoic series, both in their unaltered and 
 their metamorphic condition. In this description, the various rocks of 
 each series will be considered in the order already laid down in the 
 preceding pages of the chapter : first, the silicious rocks ; secondly, the 
 aluminous rocks ; and, thirdly, the silicates of protoxyds, with the lime- 
 stones, dolomites, and various substances of the sixth and seventh classes. 
 Much has already been done towards the description of these rocks, in 
 the preceding chapters, to which frequent references will be made. 
 
 THE LAURENTIAN SYSTEM. 
 
 Laurentian The general characters and the distribution of the rocks of the Lauren- 
 tian system have already been described in the third chapter of this 
 volume. They have been traced from the coast of Labrador to Lake 
 Huron, and thence northward to the Arctic Ocean, and occupy moreover 
 a considerable region in northern New York. Besides these, there are 
 other areas of crystalline rocks in the west and south-west, which are no- 
 ticed on page 65, and probably belong to this system. These Laurentian 
 rocks, which underlie the Silurian and Huronian series, and are the oldest 
 known strata of the earth's crust, are generally concealed in Europe. In 
 the "Western Islands, however, and on the adjacent coast of Scotland, they 
 have been identified by Sir Roderick . Murchison ; and it is probable that 
 the crystalline rocks of Greenland are of the same age. The Primitive 
 Gneiss formation of Scandinavia seems also to be, both in position and 
 lithological characters, the equivalent of the Laurentian system,* and is, so 
 far as yet known, the only portion of it exposed on the European continent. 
 The Laurentian series has never yet been seen in an unaltered condition, 
 and is everywhere highly crystalline, but the sedimentary origin of all of 
 its members is clearly evident. This great series of strata consists, in its 
 lower part, chiefly of orthoclase gneiss, with quartzites and limestones, 
 followed by a formation of anorthosite rocks. Future investigations may 
 furnish evidence which will divide the Laurentian series into several dis- 
 tinct formations, distinguished by want of conformity and by mineralogical 
 differences. The existence of what appear to be organic forms in the 
 limestones of this series, has been noticed on page 49 ; and the indirect 
 evidences of organic life which are furnished by beds of graphite, oxyd 
 
 * See on this subject, and on the parallelism of Norwegian and Canadian rocks gen- 
 erally, Mr. T. Macfarlane's valuable memoir on The Primitive Formations of Norway 
 and Canada. Canadian Naturalist for 1862, 
 
CHAP. XIX.] LAURENTIAN ROCKS. 587 
 
 of iron, metallic sulphurets, and phosphate of lime, are abundant throughout 
 this series. 
 
 The masses of quartz rock which accompany the limestones of the Lau- Quartatee. 
 rentian series, are sometimes of considerable thickness, and are generally of 
 a nearly white vitreous quartzite, occasionally holding grains of garnet, and 
 more rarely of pyroxene. Sometimes the rock assumes the characters of a 
 granular sandstone, which encloses conglomerate beds, as in the section in 
 Bastard described on page 32. In this rock, which is interstratified with 
 a crystalline limestone holding mica, graphite, and chondrodite, some of 
 the pebbles are of vitreous quartz ; while others are of greyish sandstone, 
 in which the layers of sedimentation are perfectly distinct. This shows 
 the fallacy of the notion which attributes to metamorphic action the vitreous 
 texture of certain quartzites. This is probably due to the peculiar 
 conditions of original deposition, since vitreous quartzites are often met 
 with in unaltered regions, while, on the other hand, those of metamorphic 
 formations are sometimes granular and friable. 
 
 The highly crystalline orthoclase gneiss of the Laurentian series has Gneiss, 
 already been described, on pages 23 and 29. The coarse grained granitoid 
 and porphyritic varieties, which often form mountain masses, sometimes 
 have, at first sight, but little of the aspect of stratified rocks, and might 
 be mistaken for intrusive granites. The color of the feldspar is generally 
 white or pearl-grey, but sometimes reddish. The mica, which is never 
 abundant in the coarse-grained gneiss, is generally black or dark brown, 
 but in some cases white. Hornblende is occasionally present, giving rise 
 to a hornblendic or syenitic gneiss. 
 
 Small portions of a white triclinic feldspar, which is apparently oligo- Albite. 
 clase or albite, are occasionally found with the reddish orthoclase of the 
 coarser gneiss ; especially in small lenticular masses of the latter, which 
 sometimes occur in the finer grained beds. The albite in these rocks 
 appears, for the most part, to be confined to coarse granitic veins, which 
 are apparently the result of segregation, and have been described 
 on page 36. The analysis of a fine grained reddish gneiss from Gren- 
 ville, given on page 474, shows, however, an amount of soda nearly equal 
 to that of the potash ; while the white coarse grained gneiss described 
 on the same page, consists in great part of a nearly pure potash feldspar. 
 Beds of a rock made up of orthoclase and pyroxene, with quartz, have 
 been described on page 475, and the epidotic gneiss is noticed on page 37. 
 The Laurentian gneiss is often fine grained, and sometimes passes into a 
 sort of mica-schist, which is, however, rare and in small amount. Argil- 
 lites are moreover as yet unknown in the rocks of the Laurentian system 
 in Canada. The aluminous sediments which make up the great gneissic 
 series of the Laurentian system, had lost but small portions of their alka- 
 lies at the time of their alteration, and contained sufficient potash and soda 
 
588 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 to form orthoclase and albite with by far the greater part of the alumina. 
 The only species indicating a deficiency of alkali, which are found to any 
 extent in this series, are epidote, garnet, muscovite, agalmatolite, scapolite, 
 and tourmaline. Of these, the first three characterize portions of the 
 gneiss; while agalmatolite, or gieseckite, which closely approaches in compo- 
 sition to a hydrous potash mica, forms beds in the Laurentian series in 
 New York (page 484) , and occurs crystallized in the limestones ; in which 
 
 Garnet. scapolite and tourmaline are also of frequent occurrence. Garnet not 
 only forms a large proportion of some varieties of the gneiss, but is 
 disseminated in the quartzites, and, in some cases, constitutes small beds 
 of a nearly pure garnet-rock. From the comparative rarity of aluminous 
 silicates, other than feldspars, it seems probable that the sediments of that 
 early period were, for the most part, rapidly accumulated, and were 
 speedily metamorphosed. 
 
 Anorthosites. The great anorthosite formation of the Laurentian system is described on 
 page 33. In some parts of their distribution, the rocks of this formation 
 are interstratified with orthoclase gneiss ; but great masses, apparently 
 many thousand feet in thickness, are made up of alternating bands of rocks, 
 exhibiting great differences of texture, but composed chiefly of anorthic 
 feldspars. Coarsely granitoid varieties abound, consisting of large cleavable 
 masses of feldspar, aggregated, or imbedded in a granular base. Granular 
 anorthosites of every grade are met with, passing into compact and 
 impalpable varieties with a conchoidal fracture. The crystalline varieties 
 of this rock often exhibit, in great perfection, the striae resulting from the 
 poly synthetic macles of the crystals, which are sometimes beautifully 
 opalescent. 
 
 The foreign minerals of these rocks are few in number. Carbonate of 
 lime is occasionally found disseminated in the granular varieties. Quartz 
 occurs in small portions, but is rare. Grains of red garnet are sometimes 
 found marking the lines of stratification, generally with pyroxene ; and 
 epidote is said to occur with the anorthosites of the -Adirondacks. A 
 brownish-black mica, probably biotite, is met with in small quantities in 
 the granitoid varieties ; but pyroxene is more abundant. It is sometimes 
 dark green and granular, occasionally predominating in small beds, so as 
 to form a pyroxenic rock, in which kernels or little lenticular masses of 
 cleavable feldspar are imbedded. In other cases, where its quantity is 
 smaller, it may be seen passing into a brownish lamellar variety, approach- 
 Hyperetheno. ing in its characters to hypersthene. This mineral, which characterizes 
 certain varieties of these anorthosites, is, however, seldom abundant in 
 these rocks. Its color is generally brownish-black, with bronze reflections ; 
 but a greenish variety, resembling diallage, is sometimes met with. The 
 hypersthene whose analysis is given on page 468, occurs in a remarkable 
 anorthosite in Chateau Richer, which is made up of a finely granular base, 
 
CHAP. XIX.] LAURENTIAN ROCKS. 589 
 
 greenish or greyish-white in color, holding masses of a reddish cleavable chateau 
 feldspar, which are sometimes from one tenth to one half an inch in Richer - 
 diameter ; but they often take the form of large imperfect crystals, with 
 cleavage surfaces which are frequently twelve inches long, and four or 
 five inches wide. Analyses of this feldspar, which has the compo- 
 sition of andesine, have already been given, on page 478, 1, II, III. The 
 hypersthene is irregularly distributed through the rock in flattened masses, 
 which exhibit in their arrangement a general parallelism. These are 
 occasionally four or five inches in breadth, by an inch or more in thickness, 
 and are separated from the granular feldspathic base by a thin film of 
 brownish mica. Ilmenite is also found in this rock in grains and lenticular iimenite. 
 masses, occasionally an inch or two in thickness. These occur in the 
 granular base, and generally near to the hypersthene ; but grains of the ore 
 are occasionally found in the crystalline feldspar. Quartz occurs in the 
 small grains in the iimenite, but nowhere else in the rock. The hyper- 
 sthene equals, in different portions of the mass, from two to five hundredths 
 of the whole, and the iimenite is still less in amount. Iimenite is a 
 characteristic mineral of these anorthosites ; and at Bay St. Paul it occurs 
 in great masses, with rutile, imbedded in an anorthosite rock. 
 
 Characteristic varieties of anorthosite occur in Rawdon and Chertsey. 
 They are often fine-grained and homogeneous, and form an exceedingly 
 tough rock, with an uneven sulb-conchoidal fracture, and a feebly vitreous 
 lustre. This variety is bluish or greyish-white in color, somewhat trans- 
 lucent, and exhibits, here and there, cleavable grains of feldspar. Great 
 masses of this rock are almost free from foreign minerals ; while other 
 portions abound in a green granular pyroxene, arranged with iimenite, in 
 thin interrupted parallel layers. These layers of pyroxene are seldom 
 more than four or five lines in thickness, and occur an inch or two apart ; 
 while the layers of iimenite are still thinner, and are often enclosed in 
 those of the pyroxene, along the limits of which, grains of red garnet are 
 occasionally seen. These different minerals appear in relief upon the 
 white weathered surfaces of the feldspathic rock. Small rounded masses 
 of bluish cleavable feldspar are frequently disseminated in the same planes 
 as the other minerals. In some instances, the pyroxene appears to graduate 
 into, and to be replaced by, hypersthene. The analysis of a white granular 
 homogeneous rock from this locality, is given on page 479, VII. 
 
 The predominant colors of these anorthosites are various shades of 
 blue, passing into greenish, yellowish, and rarely reddish hues : they are 
 sometimes nearly pure white. The lustre of the cleavable feldspars is 
 vitreous; of the granular varieties, waxy or dull. The weathered surfaces 
 are always of an opaque white ; but for which, some of the white 
 granular anorthosites might be mistaken, at first sight, for quartzites. 
 
590 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XIX. 
 
 Triclinic 
 feldspars. 
 
 The specific gravities of the feldspars of these rocks range from 2 67 to 
 .2 * 73, and their composition varies from that of andesine nearly to that of 
 anorthite. Farther descriptions of them will be found as above. From the 
 complete analyses of ten specimens of these feldspars, from different 
 localities, granular, crystallized, and compact, and containing from forty- 
 seven to sixty per cent, of silica, the following mean composition is 
 deduced, giving the oxygen ratios affixed : 
 
 Silica, 
 
 Alumina, 
 
 Lime, 
 
 Soda, 
 
 Potash, 
 
 Magnesia 
 
 Protoxyd of iron, , 
 Water, and loss, . 
 
 56-00 = 29-86 Oxygen. 
 
 27-30 = 12-85 " 
 
 9-42 = 2-69 " 
 
 4-84 = 1-25 
 
 84 = -14 " 
 
 1-60 
 
 Mean com- 
 position. 
 
 100-00 
 
 The proportions between the oxygen of the silica, the alumina, and the 
 protoxyds in the above, are very nearly as 7'0, 3'0, 0-96; the normal 
 ratio between the alumina and protoxyd bases in the feldspars being as 
 3:1. This mean result may be regarded as a close approximation to the 
 composition of the aluminous silicate of these anorthosite rocks. By 
 comparison with analyses to be given farther on, it will be seen that the 
 aluminous sediment which may be supposed to have given rise to these 
 feldspars, was richer in alumina than more recent argillites, and was 
 intermediate in its composition between these and kaolin. The large 
 proportion of soda, as compared to the potash, is a remarkable character ; 
 and the almost complete absence of oxyd of iron throughout great masses 
 of the rock, is equally worthy of notice. But for the universal diffusion of 
 lime throughout these sediments, their alteration might have given rise to 
 feldspathic and micaceous rocks, with simple silicates of alumina. These 
 anorthosite rocks seem, as it were, the complement to the vast masses of 
 orthoclase gneiss, and quartzite, which have been noticed above. In no 
 other series of metamorphic strata, so far as yet known, are these triclinic 
 feldspars developed on such an immense scale as in the Laurentian series, 
 and their investigation is as yet far from complete. 
 
 Pyroxene. The rocks composed chiefly of silicates of protoxyds, are now to be 
 considered. The various forms of pyroxene associated with the lime- 
 stones, have been noticed on page 467. Among the anorthosites, beds 
 are met with in which a dark green granular pyroxene prevails, en- 
 closing, however, small grains and crystals of triclinic feldspar. This 
 pyroxene sometimes assumes the characters of hypersthene ; and by an 
 increase in the amount of feldspar, these rocks pass into the anorthosites 
 already described. Black or dark green hornblende, besides character- 
 
!HAP. XIX.] LAtJRENTIAN ROCKS. 591 
 
 sing parts of the gneiss in the Laurentian series, sometimes forms great 
 >eds of rock, generally associated with a little mica, and sometimes with a 
 riclinic feldspar. A rock composed in great part of wollastonite has already 
 >een described. Talc is of rare occurrence, but a rock chiefly composed 
 >f it has been noticed ; and pyrallolite, or rensselaerite, is more frequent, 
 ill of these will be found described under their respective titles in the 
 seventeenth chapter ; where also are given several analyses of the Lau- 
 .entian serpentines, and the related mineral, aphrodite. The rocks com- serpentine, 
 posed chiefly of serpentine, to which the name of ophiolites is given, 
 ilthough less abundant in this series than in the rocks of the Quebec 
 group, present some varieties worthy of notice. They are generally 
 mingled with more or less carbonate of lime, or dolomite, in which the 
 grains of serpentine are sometimes arranged in bands, marking the strati- 
 fication, and so far predominating in some layers as to form an almost 
 pure serpentine rock. The serpentines of this series are generally pale Ophiolites. 
 yellowish or oil-green, and sometimes sulphur-yellow. Occasionally, how- 
 ever, the ophiolite rock is red and opaque in portions, from an admixture 
 of peroxyd of iron ; and small scales of mica are not unfrequently dissemi- 
 nated. A calcareous ophiolite of this kind, from Burgess, was made up of 
 an olive-green serpentine, somewhat crystalline in texture, and mingled 
 with a little magnesian carbonate of lime ; which, as well as the serpen- 
 tine, was reddish-colored in some parts, from diffused hematite. When pul- 
 verized and digested with boiling acetic acid, the rock gave 6*28 per cent, 
 of carbonate of lime, and 3-27 per cent, of carbonate of magnesia. It was 
 then ignited to decompose any remaining carbonates, and boiled with a 
 solution of nitrate of ammonia ; which dissolved a further portion of mag- 
 nesia, equal to 0-67 per cent, of carbonate. Another portion of the ophi- 
 olite treated in like manner, after ignition, with a boiling solution of nitrate 
 of ammonia, so long as ammonia was given off, gave 5 '90 per cent, of car- 
 bonate of lime, and 3-84 of carbonate of magnesia. The residue from 
 the acetic acid, gave to analysis, silica 42-10, magnesia 38*94, protoxyd 
 of iron 3*69, volatile 14-50 = 99-23. An analysis of an argillaceous 
 ophiolite will be found on page 472. Under the title of lievrite, will be 
 found the reasons for supposing that this species also forms a rock in the 
 Laurentian series. 
 
 The crystalline limestones of the Laurentian series are remarkable for their Limestona*. 
 great extent, and for the variety of crystalline minerals which they contain. 
 They are interstratified with beds of dolomite ; which sometimes contain a 
 portion of carbonate of iron, and enclose serpentine, treinolite, quartzite, 
 and a little white mica, but are generally less abounding in foreign minerals 
 than the pure limestones, hi which the following species have been found : 
 apatite, fluor-spar, heavy-spar, chondrodite, wollastonite, hornblende, pyrox- 
 ene, pyrallolite, serpentine, scapolite, orthoclase, oligoclase, agalmatolite 
 
592 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 or gieseckite, loganite, tourmaline, phlogopite, clintonite, garnet, idocrase, 
 zircon, spinel, corundum, quartz, sphene, magnetite, iron pyrites, copper 
 pyrites, and plumbago. In addition to these, a crystalline hydrate of alu- 
 mina and magnesia, which has been named houghite by Shepard, and is 
 related to volknerite, occurs in the limestones of the Laurentian series in 
 New York. In veins cutting these limestones in Canada, calcite, 
 heavy-spar, and sulphurets of lead and of copper occur ; besides which, 
 fluor-spar and carbonate of strontia are found in a vein in the same rocks 
 in New York. 
 
 These minerals are confined to particular beds of the limestone, and 
 present certain more or less constant associations, which have been noticed 
 in the description of the several species. The crystals of many of these 
 minerals exhibit a rounding of the angles, which has often been remarked 
 elsewhere in crystalline limestones, and is particularly noticeable in the 
 crystals of apatite, pyroxene, chondrodite, and quartz. 
 
 The foreign minerals of these rocks do not differ essentially from those 
 of the crystalline limestones of other regions, and of other geological forma- 
 tions. Most of the characteristic species of the Laurentian limestones are 
 found in those of southern New York, which are regarded by some 
 American geologists as of Lower Silurian age ; and in those of eastern 
 Massachusetts, which are probably Devonian. 
 
 Beds of Several mineral species, besides serpentine, may be mentioned as marking 
 
 apatite. bands in the stratification: among these are apatite, chondrodite, pyroxene, 
 magnesian mica, and graphite. The latter species, besides forming beds, 
 is, like mica, disseminated in small scales through great masses of the lime- 
 stone. The same thing may be said of apatite ; which moreover often forms 
 irregular beds, running with the stratification, and composed of nearly pure 
 crystalline phosphate of lime. 
 
 The following analyses will give some notion of the composition of the 
 dolomites and the magnesian limestones of the Laurentian series : 
 Analyses of I is a white and coarsely crystalline dolomite from the fourth lot of the 
 dolomites, tenth range of Loughborough. It leaves, when dissolved in acids, a resi- 
 due of quartz and serpentine, and contains traces of oxyd of iron, and of 
 phosphates. II is a white dolomite from the first lot of the sixth range 
 of Sheffield. Its cleavage faces present diagonal striae. The specific 
 gravity of this rock is 2-684, and it contains a very little quartz and mica. 
 Ill is a fine-grained white marble from Mazinaw Lake, and is a pure 
 dolomite. IV is a white lamellar dolomite from Grenville, which contains 
 a large proportion of grains of honey-yellow serpentine. The analysis here 
 given is that of the portion soluble in dilute nitric acid. That of the con- 
 tained serpentine will be found on page 472. V is a dolomite from the 
 thirteenth lot of the eighth range of Madoc. It is greyish-white in color, 
 almost compact, with a conchoidal fracture, and a specific gravity of 2-849. 
 This rock contains veins and disseminated grains of quartz. VI is a red- 
 
CHAP. XIX.] LAURENTIAN ROCKS. 
 
 dish granular dolomite from the village of Madoc, having a specific gravity Analyses of 
 of 2-834. Like the previous ones, it contains quartz, and a little oxyd of dolomitea - 
 iron, to which it owes its color. A portion of this however, as in the 
 last, is probably in the state of carbonate of protoxyd. 
 
 I. n. III. IV. V. VI. 
 
 Carbonate of lime, 55-79 52-57 53-90 55-13 46-47 57-37 
 
 " magnesia, 37-11 45-97 45-90 44-87 40-17 34-66 
 
 Peroxyd of iron, traces -24 1-24 1-32 
 
 Insoluble, quartz, etc., 7-10 -60 12-16 7-10 
 
 100-00 99-38 99-80 100-00 100-04 100-45 
 
 A fine grained greyish-white magnesian limestone from the fourth lot of 
 the fifth range of Madoc, has a specific gravity of 2*757, is very silicious, 
 and contains a portion of carbonate of iron. Its analysis gave carbonate 
 of lime 51-90, carbonate of magnesia 11-39, carbonate of iron 4-71, 
 quartz 32.00 = 100-00. 
 
 A magnesian limestone from the sixth lot of the tenth range of Lough- 
 borough is coarsely crystalline, but strongly coherent, snow-white in color, 
 vitreous, and almost translucent. This rock contains small crystals of 
 tremolite, grains of quartz, often rose-colored, bluish and greenish apatite, 
 and scales of yellowish-brown mica. Its analysis gave 4-00 per cent, of 
 insoluble matter, and 7*50 per cent, of carbonate of magnesia, with but a 
 trace of oxyd of iron. Cold dilute acetic acid dissolved the carbonate of 
 lime, with 3-65 per cent of carbonate of magnesia; and the residue, which 
 consisted of a mixture of dolomite with the foreign minerals, gave to 
 hydrochloric acid, 36*70 per cent, of magnesian carbonate. 
 
 The great beds of iron ore in the Laurentian system should be ranked iron ore 
 among its rock-masses. These consist of the magnetic oxyd, and more b< 
 rarely of compact or crystalline red hematite, and will be described in de- 
 tail in the chapter on economic geology. Among the few mineral species 
 found in the magnetic iron ore, may be noticed actinolite and graphite. 
 The latter mineral is disseminated in crystalline scales through a portion 
 of the Hull ore bed, and, by its presence in contact with the oxyd of iron, 
 affords a strong argument against the igneous origin of magnetic iron ore. 
 Apatite, in crystalline grains, is found abundantly disseminated through the 
 magnetic iron ores of this series, in Essex County, New York. The great 
 masses of titaniferous iron ore, or ilmenite, which occur in anorthosite rock 
 at Bay St. Paul, and sometimes enclose grains of rutile, have already 
 been described. 
 
 .OT 
 

 594 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 THE HURONIAN SERIES. 
 
 The rocks of the Huronian series, and their distribution, have been 
 Quartzites. described in the fourth chapter. Quartzite may be said to be the pre- 
 dominant rock. It varies in its color from white to grey and brown, and is 
 occasionally greenish or reddish. It is variable in texture, being sometimes 
 vitreous, and at other times a granular sandstone. It is not unfrequently 
 schistose, and sometimes slightly micaceous or feldspathic ; but no well- 
 characterized gneiss or mica schist have as yet been met with in this 
 series. The quartzites are often conglomerate ; and they contain pebbles of 
 white vitreous quartz, hornstone, and jaspers, of various colors. Bands of 
 chert, interstratified with limestone, are also abundant in this series. Great 
 masses of a greenish slaty rock are met with, varying in hardness and tex- 
 ture, from a silicious slate, passing into hornstone, on the one hand, to 
 Slates. a bluish glossy argillite, or a greenish chloritic slate, which is sometimes 
 epidotic, on the other. These slates frequently include pebbles of crys- 
 talline rocks, which are chiefly feldspathic, and derived from the Lauren- 
 tian strata. With them, however, are mingled others of quartz, and of 
 various colored jaspers. 
 
 The proportion of the pebbles varies very much ; and the rocks pass into 
 what have been designated in the description of this series, as slate con- 
 glomerates. The matrix of these is sometimes an argillaceous or a chloritic 
 slate, and occasionally becomes very quartzose, passing into a quartzite ; 
 so that it is sometimes difficult to draw a distinction between the conglom- 
 erate slates, and the jasper quartzite conglomerates. 
 
 Diorites. The diorites or greenstones of the Huronian series are intercalated in 
 beds, alike with the quartzose, and the argillaceous and chloritic members. 
 They are sometimes coarse grained and crystalline, being made up of dark 
 green hornblende and a greenish feldspar. In other parts, the rock 
 becomes finer, and even compact in its texture, and it is frequently por- 
 phyritic from the presence of crystals of feldspar. Great masses of the 
 diorite become schistose, and are then intermingled with a considerable 
 amount of chlorite, passing into dioritic and chloritic slates, which are 
 often associated with a considerable amount of epidote, generally granular 
 or imperfectly crystallized. In one locality, amygdaloidal strata, holding 
 in their cells, quartz and calcite, are found interstratified with the chloritic 
 and the porphyritic beds (page 58). In some few instances, the feldspar 
 in the coarse grained diorite becomes reddish, and the rock includes a 
 little quartz, passing into a variety of syenite. The Huronian series is 
 traversed, like the Laurentian, by dykes of greenstone trap ; but the great 
 beds of diorite just noticed, are considered to be altered sedimentary rocks. 
 Well-defined lodes cutting these diorites, afford in abundance the ores of 
 
CHAP. XIXJ HURONIAN ROCKS. 595 
 
 copper, sometimes with nickel and arsenic ; and small portions of metallic Metallic 
 sulphurets are occasionally disseminated in the strata themselves. Copper 
 pyrites occurs in this way, in an argillite on Root River ; and the diorites in 
 many places are found to contain grains of the same ore. A diorite of 
 this kind from Whitefish Lake, when crushed to powder and washed, left 
 one two-hundredth of heavy metalliferous matters. Of this, about one half 
 was attracted by the magnet, and consisted of magnetic iron ore, with 
 a little titanium, and a portion of magnetic pyrites, containing a trace of 
 nickel. The non-magnetic portion was chiefly iron pyrites, but contained 
 one hundredth of nickel, and two or three hundredths of copper. These 
 observations show the diffusion throughout the rock, of the metals which 
 are accumulated in the veins. 
 
 In the absence of any other analyses of these greenstones, the results 
 obtained in their examination by Mr. J. D. Whitney are subjoined. A 
 tough light-green colored rock, associated with the stratified iron ores of 
 the Huronian series, in northern Michigan, was made up of a feldspar, 
 seemingly labradorite, and a green lamellar mineral having the appearance 
 of hornblende ; the latter predominating, and having sometimes a bright 
 green color, and a granular texture. The absence of magnesia shows, how- 
 ever, that this mineral must be distinct from hornblende. The analysis of 
 the rock is given under I. A light colored homogeneous feldspathic rock 
 from the Menomenee, was also examined. It was readily fusible before the 
 blowpipe to a colorless glass, and was imperfectly decomposed by acids. 
 Its analysis is given under II. This rock, in some parts of its distribution, 
 is mingled with small portions of a greenish mineral, which is described as 
 resembling serpentine or talc in appearance. At Presqu'isle a dark 
 green, apparently homogeneous rock occurs, consisting essentially of a 
 hydrous silicate of magnesia and iron, which is soluble in hydrochloric 
 acid, and is mingled with minute crystals of magnetite, and with from two 
 to six per cent, of an insoluble silicate, apparently hornblende. The compo- 
 sition of the soluble portion of a specimen is given under III, from which 
 it would seem to be a serpentine, in which a large part of the magnesia is 
 replaced by oxyd of iron. Portions of the same rock from other localities, 
 gave from fifteen to thirty-three per cent, of magnesia. (Geology of Lake 
 Superior, ii, 92.) 
 
 I. IT. in. 
 
 Silica, 46-31 54-54 37-25 
 
 Alumina, 11-14 21-45 
 
 Peroxyd of iron, .... 5-53 6-75 
 
 Protoxyd " 21-69 .... 14-14 
 
 Lime, 9-68 8-40 
 
 Magnesia, traces traces 28-67 
 
 Soda, 6-91 7-54 1-16 
 
 Water, 4-44 2-54 10-89 
 
 100-17 100-00 98-86 
 
I 
 
 596 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 Limestones. The limestones of this series are but small in amount. One band of 
 three hundred feet in thickness has however been traced for considerable 
 distances to the north of Lake Huron. Its colors are chiefly greyish, 
 greenish, or buff, rarely white, and its fracture is conchoidal, and some- 
 times granular. It is often ferruginous and yellow-weathering, very 
 silicious, and somewhat magnesian. Thin silicious layers give to its 
 weathered surface a very uneven aspect ; and it is strikingly contrasted 
 with the Laurentian limestones, by the absence of pure crystalline varieties, 
 and of imbedded crystalline minerals. Two smaller bands in the series 
 consist of similar impure limestones, with regular layers of yellowish chert, 
 the latter predominating. See a section on page 56. 
 
 The analyses of the limestones from the two extremities of Lake Panache, 
 on the Whitefish Eiver, will show their ordinary composition. 
 
 I. n. 
 
 Carbonate of lime, 55-10 41-97 
 
 " magnesia, 6*50 2-40 
 
 Insoluble, sand, and a trace of iron, 38-40 55-63 
 
 100-00 100-00 
 
 iron ores. A small bed of red iron ore occurs with the Huronian rocks at the Wallace 
 mine, on Lake Huron ; and in northern Michigan, the great beds of stratified 
 red hematite, associated with slates, quartzites, and jaspers, appear to 
 belong to the Huronian series. It is doubtful as yet how far the crystalline 
 rocks to the north and the west of Lake Superior, as described by Drs. 
 Bigsby and Owen, belong to the Laurentian, and how far to the Huronian 
 series. The same question also arises with regard to the azoic strata of 
 Arkansas and Missouri (see page 65). The rocks of these various 
 localities exhibit crystallized mineral species which have not been found 
 in the Huronian strata in Canada ; and some of the species, such as stauro- 
 tide and chlorite, are as yet unknown to the Laurentian series. The rocks 
 of the Huronian system in Canada, seem, from Mr. Macfarlane's compari- 
 son above cited, to correspond with what he has called the Quartzose 
 Division of the Primitive Slate formation of Norway, the Tellemarken 
 Quartz formation of Naumann. The predominance of quartzites, of strat- 
 ified diorites, of conglomerate quartzites holding jasper, of slate conglom- 
 erates, and of chert beds ; the absence of the characteristic gneiss and 
 mica-slate of the Laurentian series, and the rarity of limestones, are so 
 many features which are common alike to the Norwegian formation, and to 
 the Huronian series, which occupies the same stratigraphical horizon. 
 
CHAP. XIX.] EASTERN PALAEOZOIC ROCKS. 597 
 
 THE PALEOZOIC SERIES. 
 
 In describing the Quebec group, on page 234, it has been shown that a Palaeozoic 
 series of great dislocations, with upthrows to the east side, traverse eastern 
 North America, one of which is traced from near Lake Champlain to 
 Quebec, and, thence passing along the island of Orleans, appears again 
 along the northern shore of Gaspe*. An effect of this immense break, or 
 series of breaks, has been to bring up a great mass of lower strata, causing 
 them to overlie the Trenton, Utica, and Hudson River formations. For 
 the present purpose, it will be convenient to consider this line of disloca- 
 tion as one separating the palaeozoic rocks of Canada into an eastern and 
 a western district. In the latter, which also extends eastward as far as TWO divi- 
 Anticosti, to the north of the line, there are found the various members 610ns * 
 of the palaeozoic series, from the Potsdam formation to the Devonian sys- 
 tem inclusive, presenting the characters by which they are generally known 
 to American geologists, and unaltered and nearly horizontal in position. 
 
 In the eastern district, on the contrary, is found a vast series of strata, 
 consisting of what has been described as the Quebec group, with its under- 
 lying strata of the primordial zone, and regarded as the stratigraphical 
 equivalents of the Potsdam and Calciferous formations, perhaps with the 
 addition of the Chazy. The higher members of the Lower Silurian series 
 are here wanting; but, to the eastward, rocks of Upper Silurian and 
 Devonian age are found reposing on those of the Quebec group. It is 
 proposed to describe separately the lithological characters of the rocks of 
 the eastern and those of the western district. 
 
 PALAEOZOIC KOCK8 OF THE EASTERN DISTRICT. 
 
 The rocks of this district have been described in the chapter on the Quebec 
 Quebec group, and in that on the Gaspe* formations. The first, and the most gr l 
 important to be considered, are those of the Quebec group, of which a sec- 
 tion, showing a large portion of the series, has been given on page 227. 
 These rocks are there seen in an unaltered condition, and consist of alter- 
 nations of limestones, dolomites, sandstones, and shales ; from which issue, 
 in various localities, saline and alkaline springs. The whole of these 
 rocks are however much contorted, and, with the exception of a narrow 
 belt along the north and west limits of the district, are in a metamorphosed 
 condition, and are included in that great belt of altered rocks which forms 
 the Appalachian chain, and stretches from Gasp^ to Alabama. As already 
 remarked on page 585, the metamorphism has comprehended not only the 
 strata of the Quebec group, but those of the Upper Silurian and Lower De- 
 vonian series to the east of them ; and in Massachusetts, it has included the 
 
598 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 rocks of the Carboniferous system ; of which the shales have become crystal- 
 line, and the coal is changed into graphite. It is moreover probable that 
 the rocks of New Hampshire, including the White Mountains, are altered 
 strata of Devonian age. It is however chiefly to the rocks of the Quebec 
 group that the present descriptions will be confined, as the higher strata in 
 the eastern district, so far as yet studied, have not presented many marked 
 mineralogical characteristics. 
 
 Notre Dame ^ e roc ^ s ^ ^ ne Q ue h ec group, in their altered state, compose the Notre 
 Mountains. Dame and the Shickshock Mountains, which are a continuation of the 
 Green Mountains of Vermont. In describing successively the lithological 
 groups of the altered region, their unaltered equivalents will be noticed at 
 the same time. It will be observed, that, although the mineral species of 
 these palaeozoic rocks are in great part identical with those of the Lauren- 
 tian system, they nevertheless present such variations in composition, 
 arrangement, and structure, that the several classes of rocks are, for the 
 most part, very distinct from their equivalents in the older series. This is 
 due, in part, to original differences in the composition of the sediments, 
 and in part, probably, to a less energetic metamorphism. 
 
 Quartzites. ^ ne silicious rocks of the eastern district offer but few peculiarities. 
 The sandstones of the unaltered portions are sometimes nearly pure 
 quartzites, and at other times contain an admixture of calcareous, dolo- 
 mitic, or argillaceous matter. This latter characterizes the sandstones of 
 the Sillery formation, which vary from a fine grained rock to a conglome- 
 rate holding small pebbles, and sometimes contain scales of graphite and of 
 mica. The argillaceous admixture is generally greenish ; but in some cases, 
 it is red from diffused peroxyd of iron, which is occasionally accumulated in 
 the form of small layers and masses of red hematite. These greenish sand- 
 stones are sometimes slightly calcareous ; and they not unfrequently contain 
 a little carbonate of manganese, which causes them to become blackish-brown 
 on the weathered surfaces. In some cases, the coloring matter of these 
 sandstones is allied to glauconite in composition : see the analyses of the 
 suiery sand- soluble elements of such a rock, on page 487. A green sandstone from 
 stone. Sillery was attacked by boiling sulphuric acid, which left 71 '45 parts of 
 quartz sand: the decomposed portion yielded silica 9 * 00, alumina and oxyd 
 of iron 13 00, magnesia 69. These sandstones have not yet been farther 
 analyzed; but the red sandstone of Charlotte, in Vermont, which belongs to 
 some part of this series, was examined by Prof. G. F. Barker. A speci- 
 men, which was said to be more than ordinarily silicious, had a specific 
 gravity of 2-65, and gave by analysis, silica 83-30, alumina, with some oxyd 
 of iron, 8-70, lime 1*12, magnesia -10, potash 4*59, soda '45, volatile '80 
 = 99-06. (Geology of Vermont, page 707.) From this analysis, it would 
 seem that the argillaceous matter of this sandstone contains as much potash 
 as is required to convert it into orthoclase. 
 
CHAP. XIX.] EASTERN PALEOZOIC ROCKS. 599 
 
 The metainorphic portions of this region often contain white vitreous 
 quartzites, which are interstratified with, and pass into quartzose mica- 
 schists and gneiss. These quartzites are not unfrequently conglomerate ; 
 and in Vermont, they are said to contain, in some parts, crystals of 
 magnetite, and small quantities of plumbago. It will, however, be evident 
 from the descriptions given in the chapter on the Quebec group, that 
 quartzites are found at several horizons in this series. 
 
 Beds of jasper occur at various places in this series. At RiviSre Ouelle, Jasper, 
 there is a band of red and green jasper, interstratified with unaltered 
 shales of the Quebec group. It contains veins of chalcedony ; and it 
 appears to owe its red color to disseminated hematite. Near to Sher- 
 brooke, in the metamorphic region, there is also a bed of red jasper, 
 which contains hematite, and passes into jaspery red iron ore. 
 
 Beds of a peculiar fine grained quartzo-feldspathic rock occur in various Feidspattnc 
 localities in this series. Near to the falls of the Etchemin at St. rt 
 Henry, is a mass of this kind, fifty feet in thickness, and divided into 
 layers of from two to twelve inches, by films of interposed shale, which are 
 sometimes bright green in color. This is succeeded by a smaller mass of 
 fifteen feet ; the whole interstratified with greenish and greyish shales, in 
 an unaltered region. Thin beds of a similar rock occur, under like condi- 
 tions, at St. Anselm. This substance is finely granular, sub-conchoidal in 
 its fracture, tough, with the hardness of feldspar, and translucent on the 
 edges. Its color varies from pale greenish-white to olive-green, with 
 clouds of a darker green. A similar rock occurs in the metamorphic 
 region, associated with serpentines, on the sixth lot of the sixteenth range 
 of Orford. It is homogenous, somewhat translucent, and does not become 
 opaque on the weathered surfaces. It is compact, very tough, has a scaly, Petrosiiex. 
 conchoidal fracture, a greenish or greyish-white color, and a dull, waxy 
 lustre. The hardness of this rock is equal to that of feldspar, and its 
 specific gravity is 2-64. Its analysis is given under I, and that of a 
 specimen from St. Henry under II. 
 
 I. II. 
 
 Silica, 78 -40 71-40 
 
 Alumina, 11-81 13-60 
 
 Soda, 4-42 3-31 
 
 Potash, 1-93 2-37 
 
 Lime, -84 -84 
 
 Magnesia, - 77 2-40 
 
 Protoxyd of iron, ' -72 3-24 
 
 Volatile, '90 2-50 
 
 99-79 99-66 
 
 A second portion of the Orford rock gave silica 77-70. When that 
 from St. Henry was treated with a boiling dilute solution of soda, 6-1 
 per cent, of silica, and only traces of alumina, were dissolved. Acids 
 

 600 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 have but little action on these rocks. The oxygen ratios for the alumina 
 and the alkalies in I are as 5*52 : 1-47, and in II as 6-35 : 1-25. 
 
 These rocks have the composition of intimate mixtures of feldspar and 
 quartz ; but it is worthy of note, that even in the metamorphic region they 
 do not seem to have become crystalline. They approach in composition 
 to what has been called petrosilex, and to the krablite of Iceland, which, 
 according to Genth and Von Walterhausen, is a distinct species of feldspar. 
 
 Many of the quartzo-feldspathic rocks of the eastern district, however, 
 assume the form of true gneiss ; which is sometimes highly quartzose and 
 micaceous, passing into mica-schist. At other times, great masses of 
 granitoid orthoclase gneiss are met with ; but these are generally finer 
 grained and more quartzose than the gneiss of the Laurentian system, 
 with which the practised observer can scarcely confound them. The coarse 
 , . grained and porphyritic white and reddish varieties common to the latter, 
 
 are never met with in the rocks of the eastern district, where the gneiss 
 is generally of pale greyish and greenish hues. In some cases, great 
 portions of it are so destitute of marks of stratification, that, but for their 
 relations to the adjacent beds, they might be taken for intrusive rocks. 
 The mica is generally white, and in small quantity. Examples of this 
 granitic gneiss occur in St. Joseph, in Shipton, and in Sutton Mountain. 
 Argillites. In the next place may be considered the argillites, and some related 
 aluminous schistose rocks, which occur in the altered region. A great pro- 
 portion of the argillites have however undergone no apparent change, but 
 are found in the immediate vicinity of the serpentines and steatites, earthy 
 in texture, and with no appearance of alteration. I is a roofing slate from 
 the Kingsey quarries, purplish-blue in color, and having a specific gravity 
 of 2*88. II is a similar roofing slate, from Walton's quarries in Mel- 
 bourne. Ill is a red shale from the Etchemin River, two miles above St. 
 Anselm. IV is a tender greyish-green shale, from the island of Orleans ; 
 and V is a black shale, yielding a white powder, and forming a layer one 
 fourth of an inch thick in IV. 
 
 I. II. III. IV. V. 
 
 Silica, 54-80 64-20 66-00 60-85 58-20 
 
 Alumina, 23-15 16-80) 24 . 6Q (15-80 21-20 
 
 Protoxydofiron,. 9-58 4-23$ 5-94 4-23 
 
 Lime, 1-06 -73 traces 1-92 1-23 
 
 Magnesia, 2'16 3-94 " 4-10 2-48 
 
 Potash, 3-37 3-26 3<67 4-34 3-86 
 
 Soda, 2-22 3-07 2-22 1-22 1-43 
 
 Volatile, 3-90 3-40 3-00 4-90 5-30 
 
 100-24 99-63 99-49 99-07 97'93 
 
 III holds traces of manganese ; and it doubtless contains a portion of 
 iron as peroxyd, to which it owes its red color. 
 
CHAP. XIX.] EASTERN PALAEOZOIC ROCKS. 601 
 
 It is worthy of notice, that some of these argillaceous rocks contain small Magnesia 
 portions of magnesia. Thus the argillite IV, from the island of Orleans, m 6hales 
 contained no carbonates, but gave to the action of sulphuric acid 2-00 per 
 cent, of magnesia, with but a trace of lime. A green band imbedded in 
 the red shale of St. Henry, and in immediate contact with the native copper 
 of this locality, did not effervesce with acids ; and when boiled with a solu- 
 tion of nitrate of ammonia, after ignition, it gave only traces of magnesia 
 and lime. When decomposed by heating with sulphuric acid, however, it 
 yielded of alumina, with a little peroxyd of iron, 16-1 per cent., and of 
 magnesia 5*5 per cent., besides traces of linie and copper. A similar 
 green shale from Sillery, which contained small flakes of green carbonate 
 of copper, gave in like manner 14*8 per cent, of alumina and oxyd of iron, 
 with 2-5 per cent, of magnesia, and a trace of lime. The magnesia in 
 these unaltered shales evidently exists in the form of a readily decomposible 
 silicate, which may probably be sepiolite or an analogous compound. Not 
 unfrequently, however, the argillites contain admixtures of both lime and 
 magnesia, in the form of carbonates. A yellow-weathering green shale 
 from the island of Orleans, was attacked with effervescence by dilute nitric 
 acid, which removed, besides a little oxyd of iron and alumina, carbonate 
 of lime 11-05, and carbonate of magnesia 9-75, equal to 20' 80 per cent, 
 of dolomite. 
 
 In some parts of the metamorphic region the argillites are found to Taicoseor 
 assume a talcose aspect. This is especially true of the red and green 
 shales of the Sillery formation. These at Ste. Marie, Beauce, are much 
 intersected by veins of quartz, and are very soft and fissile, exfoliating by 
 the action of the weather, and becoming converted, when moistened, into 
 a pasty mass, which is very unctuous to the touch, and has a silvery glim- 
 mering lustre. The green beds retain their color, and the red ones have 
 a pale purplish or lilac color, being occasionally spotted on their cleavage 
 surfaces with scales of a greenish mineral resembling chlorite in appearance. 
 A characteristic specimen of this red slate, from a locality in Ste. Marie, 
 where explorations have been made for copper pyrites, which is found 
 there in small quantities, was selected for analysis, and the unctuous mate- 
 rial having been separated by eleutriation from grains of quartz, and 
 dried at 212 F., yielded on analysis the result I. Similar rocks from 
 Vermont, belonging apparently to the same series, have lately been analysed 
 by Prof. G. F. Barker (Geology of Vermont, page 707), whose results are 
 here cited for comparison. II is from Irasburgh, and is designated as 
 novaculite slate. It is described as very unctuous, apparently homogene- 
 ous, translucent, of a dirty grey color, infusible before the blowpipe, and 
 with a specific gravity of 2.65. Ill is a greenish-grey friable talcose 
 schist from Roxbury, with a specific gravity of 2.73. IV is an olive-green 
 talcose schist from Middlesex. V is a soft unctuous rock from North 
 
I 
 
 602 GEOLOGY OP CANADA. [CHAP. XIX 
 
 Carolina, which is ground to powder and employed in the arts instead of 
 steatite. Its analysis is by Dr. Charles T. Jackson : 
 
 I. II. III. IV. V. 
 
 Silica, 66-70 78-70 69-90 64-10 75-00 
 
 Alumina, 16-20 12-80) 20 . 00 23 . 5Q (18-75 
 
 Protoxyd of iron, . 6-90 traces,? I traces 
 
 Lime, -67 1-23 1-51 '84 , 
 
 Magnesia, 2-65 traces 1-80 1-98 
 
 Potash, undet. -89 1-45 3-70 2-00 
 
 Soda, " 5-57 2-33 2-20 
 
 Volatile, 3-10 -60 2-40 3-60 3-50 
 
 99-79 99-39 99-92 99'25 
 
 The analysis II gives for the oxygen ratio between the silica, alumina, 
 and protoxyd bases, very nearly 21 : 3 : 1. It is evident from the analyses, 
 that these rocks, which are generally called talcose slates, do not owe 
 their softness and unctuosity to talc, or to any other magnesian mineral, but 
 to an admixture of some soft foliated aluminous silicate, which may be 
 either pyrophyllite, pholerite, or a hydrous mica. They have therefore 
 for distinction sometimes been called nacreous slates. A somewhat 
 unctuous schistose rock from Shipton, made up of minute scales, and 
 resembling chlorite slate in aspect, has been described on page 494 : it 
 differs from a hydrous mica chiefly in the smaller proportion of alkalies. 
 Some of the black slates of this series contain a small amount of carbon in 
 the form of plumbago, and have been noticed on page 528. 
 
 Agaimato- Under the title of agalmatolite, on page 484, has been described a 
 class of rocks found among the shales of St. Nicholas, with similar schistose 
 rocks in Vermont, and the agalmatolites of St. Francis and Stanstead. 
 These substances are remarkable for the small amount of silica, and the 
 large proportion of potash, which they contain. In their softness and 
 unctuosity, they approach to some of the more silicious rocks just described, 
 but resemble still more serpentine and steatite. 
 
 Rocks composed in great part of triclinic feldpars are common in this 
 series, and represent the anorthosites of the Laurentian system. They are 
 seldom, however, coarsely crystalline, and are often compact. The feld- 
 spar in some cases approaches to albite, or to oligoclase in composition. 
 
 Diortte. Through an admixture of hornblende, these feldspar rocks pass into diorite ; 
 in different varieties of which, the one or the other mineral predominates. 
 These compound rocks are often so finely granular as, at first sight, to 
 appear homogeneous ; at other times they are rather coarse grained, and are 
 sometimes porphyritic from the presence of large crystals of feldspar in a 
 fine grained greenish base. Varieties of these diorites at Drummondville 
 and in Potton are described on pages 243 and 250. At the latter locality, 
 portions of the rock are a nearly pure anorthosite ; while other parts assume 
 
CHAP. XIX.] EASTERN PALAEOZOIC ROCKS. 603 
 
 a conglomerate character, holding grains of quartz, and fragments of indu- 
 rated shale. The imbedded hornblende crystals are occasionally of con- 
 siderable size, and dark green in color. In some parts, the hornblende is 
 replaced by pyroxene, or by diallage. At Drummondville, parts of the Amygdaloid. 
 rock are porphyritic ; while others are amygdaloidal, holding portions of 
 calcite and nodules of agate. 
 
 A variety of this diorite, from Brompton Lake, in the second lot of the 
 sixteenth range of Orford, was examined. Its color is white, with a 
 greenish or yellowish-grey tinge, evidently due to some disseminated 
 mineral, which turns yellowish-brown by ignition, while the base becomes 
 whiter and more opaque, and is then seen to consist of grains of crystalline 
 feldspar, sometimes with striated cleavage planes. The rock has a waxy 
 lustre, is sub-translucent, and has a somewhat conchoidal fracture. Its 
 hardness is about that of feldspar, and its specific gravity from 2-75-2-76. 
 Its powder is not acted upon by nitric acid. The analysis of this rock is 
 given under I. A second determination gave silica 63-60 and lime 7*28. 
 A similar rock from St. Francis, Beauce, was more coarsely crystalline 
 than the last, and had a pale bluish-green color, from the admixture of an 
 imperfectly crystallized hornblende with a somewhat translucent cleavable 
 feldspar. The hornblende turns dark olive-brown by ignition, and the 
 structure of the rock is then very evident. Its lustre is feeble and waxy, 
 and its specific gravity from 2-71-2*72. The pulverized rock yields to 
 dilute nitric acid, a trace of alumina, and a little lime. Its analysis is 
 given under II. 
 
 I. Oxygen. II. Oxygen. 
 
 Silica, ........... 63-40 = 33-81 6,3-60 = 33-92 
 
 Alumina, ......... 12-TO = 5-93 14-20 = 6-63 
 
 = 2-07 = 2-01 
 
 Potash, .......... -13 4-13 S 
 
 Lime, ............ 7-50 = 2-14 4-37 = 1-22 
 
 Magnesia, ........ 3-37 = 1-35 6-84 = 2-73 
 
 Protoxydof iron,.. 423 = -94 1-92 = -43 
 
 Volatile, ......... -40 -70 
 
 99-68 100-85 
 
 In the analysis I, the oxygen ratio of the alumina and alkalies is very 
 nearly as 3 : 1 ; and if to these be added the silica necessary to form a 
 soda feldspar, we have the elements of 64-0 parts of albite. The remain- 
 ing silica, and the other bases, afford the oxygen ratio 9-81 : 4*43, showing 
 a little excess of silica over that required to form hornblende. In analysis 
 II, there is a slight deficiency of alkalies ; and 0-71 parts of lime may be 
 supposed to enter into the composition of 73-81 parts of albite. The oxygen 
 of the silica and of the remaining bases, gives the ratio 7-43 : 4-18, or a 
 slight deficiency of silica ; rendering it not improbable that the rock may 
 
604 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XIX. 
 
 contain oligoclase, or a mixture of some more basic feldspar with ortho- 
 clase, which is indicated by the large amount of potash. 
 
 Greenstone. Other varieties of these diorites are much darker in color, and heavier, 
 from a larger admixture of hornblende. These closely resemble in their 
 aspect many intrusive greenstones. A portion of such a rock from near 
 the copper mine in Acton, has a specific gravity of 3'04-3'OT, and is 
 
 Acton. geen to consist of fine grains of greenish-white feldspar, sometimes showing 
 cleavage planes, mingled with a blackish-green amorphous mineral. Its 
 powder did not effervesce with strong acetic acid ; but nitric acid attacked 
 a small portion of pyrites, which is disseminated in the rock, and dissolved 
 moreover a considerable portion of alumina. A few scales of a brown 
 mica were visible in the residue after the action of the acid. The results 
 of two analyses of the rock are given under III and IV. A specimen of 
 a similar fine grained diorite from near the copper mine in Upton is 
 
 Upton. greenish-grey in color, but weathers to a reddish-yellow. Its powder was 
 attacked with slight effervescence by acetic acid, which removed portions 
 of carbonates of lime, magnesia, and oxyd of iron, equal to about three 
 per cent. The pale green residue became reddish-brown by ignition, and 
 gave by analysis the result V. The fissures of this rock contained thin 
 layers of a soft greenish, amorphous, translucent substance, resembling 
 serpentine in appearance. This was partially decomposed by sulphuric 
 acid, leaving an insoluble residue. It contained no lime nor carbonates, 
 and gave by the analysis of -581 grams : silica -141, alumina -065, mag- 
 nesia -047, protoxyd of iron -148, volatile '055, insoluble '125 = 581. 
 The composition of the soluble portion, calculated for 100 parts, is given 
 under VI. 
 
 rior - 
 
 III. 
 
 Silica, .......... 49-45 
 
 Alumina, ....... . 14-80 
 
 Potash, ......... 1-15 
 
 Soda, ..... . ..... 2-96 
 
 Lime, ...... ..... 11-10 
 
 Magnesia, ....... 8-85 
 
 Protoxyd of iron, .. 9-90 
 
 Water, .......... 2-60 
 
 100-81 
 
 IV. 
 
 49-95 
 
 undet. 
 
 " 
 
 " 
 11-20 
 
 8-70 
 
 .... 
 
 3-10 
 
 V. 
 
 51-80 
 11-30 
 undet. 
 
 ." 
 
 3-25 
 
 7-80 
 13-14 
 
 4-40 
 
 VI. 
 
 30-90 
 14-20 
 
 100-00 
 
 ^ ^ interesting to compare with these analyses, the similar results 
 obtained by Mr. J. D. Whitney with the greenstones from the Upper 
 Copper-bearing rocks of Lake Superior. These, as has already been 
 pointed out in preceding chapters, are the stratigraphical equivalents of 
 the Quebec group, which they resemble, both in their metallic contents 
 and their lithological characters. A specimen of the fine grained and 
 apparently homogeneous greenstone from Eock Harbor on Isle Royale, 
 gave, on analysis, the result I. Another variety from the Cliff Mine was 
 
CHAP. XIX.] EASTERN PALEOZOIC ROCKS. 605 
 
 dark greenish in color, and compactly crystalline, and showed, under the Whitney' 
 microscope, three distinct minerals, a feldspar, which was colorless or analyses 
 slightly greenish, a dark green substance resembling chlorite, and a 
 third element, .which was apparently pyroxene or hornblende. Small 
 crystals of magnetic iron are also occasionally disseminated. The pulver- 
 ized rock was partly decomposed by long digestion with hydrochloric acid, 
 nearly at the boiling point. This dissolved 21 -17 per cent., leaving a 
 residue of silica and undecomposed mineral. The analysis of the rock 
 as a whole, is given under II, that of the soluble portion under III, and 
 that of the residue under IV. 
 
 I. Oxygen. II. Oxygen. III. IV. 
 
 Silica, 47-97=24-93 50-20=26-08 64-58 (by loss.) 
 
 Alumina, 15-56=7-28 15-43=7-22 30-95 11-67 
 
 Soda, 6-24=1-61 4-75=1-22 11-26 3-14 
 
 Lime, 7-07=2-02 5-47=1-56 9-36 4-57 
 
 Magnesia, 8-28=3-21 8-62=3-34 15-96 6.86 
 
 Protoxyd of iron,... 12-41=2-75 13-79=3-06 32-47 9-18 
 
 Water, 2-46=2-18 1-74=1-55 
 
 99-99 100-00 100-00 100-00 
 
 Mr. Whitney supposes that the alumina in these rocks exists in the 
 form of labradorite. On deducting from the above two analyses the 
 alumina and soda, together with the lime and silica necessary to form 
 labradorite with these, there remains, in both cases, a large excess of bases 
 over the amount required for hornblende or pyroxene. This excess, and 
 the presence of water, are explained by the admixture of magnetic iron and 
 of the chlorite-like mineral noticed in the rock from the Cliff Mine, which 
 may, probably, be similar in composition to the silicate separated from the 
 diorite of Upton. (Whitney, Geol. of Lake Superior, ii, 87.) 
 
 It is not easy to determine the mineralogical composition of these 
 hydrated greenstones of the Quebec group, from Lake Superior and from 
 the eastern district. In the latter region, while they graduate on the 
 one hand into pure feldspar rocks, they appear in other cases to contain 
 a variety of diallage ; and this, from the analyses given hi page 469, is 
 often a hydrated mineral very distinct from pyroxene ; so that it is not 
 improbable that in the hydrated rocks in question, either this diallage, or 
 chlorite, or something like the mineral from Upton, just described, may, 
 wholly or in part, replace the hornblende. 
 
 On Isle Roy ale, and elsewhere on Lake Superior, according to Mr. Epidotic 
 Whitney, epidote enters very largely into the composition of these dio- rocks< 
 rites, and even forms beds of considerable extent. This epidotic rock 
 sometimes becomes amygdaloidal, and then often contains quartz. Epidote 
 characterizes great masses of the altered rocks in the eastern district. In 
 some cases, it is found as a fine-grained and apparently homogeneous mix- 
 
606 GEOLOGY OF CANADA. [CHAP. XIX, 
 
 ture of pale yellowish-green epidote with a portion of quartz. The descrip- 
 tion and analysis of a variety of this epidosite are given on page 497, 
 In some portions of the rock the two minerals occur in distinct grains. 
 More frequently the epidote occurs in rounded masses, sometimes an inch, 
 or even several inches in diameter, composed of radiating crystals, and 
 imbedded in a fine-grained micaceous quartzite or mica-schist, which is 
 either greyish in color, or greenish from disseminated scales of chlorite. 
 The laminae of the schist are often seen conforming to the masses of 
 epidote, which are elongated in the direction of the layers. They some- 
 times make up the greater portion of the rock, and give to its surface a 
 
 Feldspar, curiously knotted aspect. Not unfrequently the nodules of epidote are 
 accompanied by vitreous quartz, which sometimes surrounds the epidote, 
 and occasionally forms little masses by itself. A feldspar, having the 
 characters of orthoclase, is sometimes found in these nodules, with the 
 quartz ; and small radiating masses of actinolite are occasionally met with, 
 
 chlorite, sometimes with scales of graphite. Chlorite is very often associated with 
 epidote, and some bands consist of a fine grained mixture of epidote and 
 chlorite, often with quartz, and with small crystals of specular or magnetic 
 iron ore. Very great variations exist in the proportions and the arrange- 
 ment of these minerals, from the homogeneous epidote rock above de- 
 scribed, to pure slaty chlorite, and to schists in which specular iron pre- 
 dominates, with a mixture of quartz and chlorite. Most of these varieties 
 are well seen in Button and St. Armand, as noticed on page 246. Epi- 
 dote is found crystallized with chlorite, quartz, calcite, and talc, in the red 
 concretionary argillite rock of St. Joseph, described on page 255. 
 
 Orthoclase Orthoclase, besides occurring crystallized in the quartzose epidotic strata 
 
 m argiiiite. a ]j y e no ticed, is found under remarkable conditions among argillaceous 
 rocks at the St. Francis copper-mine in Cleveland. Here are beds of a 
 soft fine-grained somewhat schistose dark bluish-grey argillite, enclosing 
 small ovoidal or elongated masses of crystalline feldspar, which have a 
 general parallelism, and are oblique to the divisional planes of the rock. 
 The laminae of this conform to the feldspathic masses, which give a knotted 
 surface to the exterior of the rock. These are in some portions from one 
 eighth to one tenth of an inch in diameter, and are nearly spherical, or 
 elongated two or three diameters. In other portions of the rock, they are 
 an inch or more in length, and more irregular, though always rounded in 
 outline. The exterior of the nodules is a white or pink feldspar ; but in the 
 centre of some, especially of the larger nodules, white translucent and vit- 
 reous quartz occasionally occurs ; and these not unfrequently are composed 
 of this mineral, with only a thin envelope of feldspar. In some parts, the 
 feldspar is seen to extend from the nodules, in thin layers among the 
 laminae of the slate, giving to such portions a gneissoid aspect. In most 
 cases however the rock has completely the aspect of an amygdaloid ; espe- 
 
CHAP. XIX.] EASTERN PALAEOZOIC ROCKS. 607 
 
 cially in sections, which exhibit the feldspar surrounding the quartz, in the 
 ovoidal masses. In the immediate vicinity of this rock, is another in which 
 a brick-red orthoclase has filled and penetrated in an irregular manner 
 a bluish-black argillite. Much of the rock in this vicinity is however 
 chloritic, and assumes the character of a chloritic slate. In one portion in 
 which the slaty structure is scarcely apparent, and which resembles rather 
 a soft chloritic greenstone, small nodules of crystalline quartz are dissemi- 
 nated, as in the argillite, but without feldspar, and give to this rock also 
 the aspect of an amygdaloid. A somewhat similar chloritic and schistose 
 rock from Orford contains great numbers^of spheroidal masses, sometimes 
 half an inch hi diameter, and arranged like those just described. They 
 are fine grained, compact, nearly as hard as quartz, and are yellowish- 
 green in color, often purple at the centre. They become soft and decom- 
 posed on the weathered surfaces, and, from their hardness and specific 
 gravity, appear to be feldspathic. A similar amygdaloidal character is also 
 well marked in portions of the reddish and greenish epidotic argillite of St. 
 Joseph above mentioned, which contains numerous almond-shaped cavities 
 filled with calcite ; and in the diorites of Acton, St. Flavien, and Drum- 
 mondville, which at the latter place hold agate as well as calcite. 
 
 The occurrence of orthoclase in veins with quartz, chlorite, and specular Feldspar in 
 iron, in these rocks, has already been noticed on page 476. These veins - 
 minerals occur both in the epidotic quartz-slates of Sutton, and in the 
 argillites ; and, like the quartz, feldspar, and epidote met with in nodules 
 in both of these rocks, indicate that during metamorphism these minerals 
 were in solution, and were deposited, either in fissures, or in concretions in 
 the midst of the sediments. Quartz is still more abundant than feldspar 
 in the veins cutting these slates, and is sometimes associated with white 
 mica, and not unfrequently with bitter spar, talc, and chlorite ; besides 
 which, these veins hold, not only metallic sulphurets, but rutile, specular 
 iron, and native gold. 
 
 The chloritic slates of Cleveland are traversed by small veins, from one chlorite 
 tenth to one fourth of an inch in diameter, which are perfectly well defined, 6lates - 
 and are filled with pure scaly chlorite, sometimes intersected by seams of 
 quartz, and evidently analogous to the larger veins just mentioned. In some 
 cases, the slates themselves are a pure chlorite or potstone. A rock of this 
 kind, from the twenty-sixth lot of the sixth range of Potton, was of a pale 
 greenish-grey color, unctuous to the touch, and was composed of lamellae 
 of chlorite, so arranged as to give a schistose structure to the mass. Its 
 analysis gave silica 29-60, magnesia 25*95, protoxyd of iron 14-49, alu- 
 mina 19-70, water 11-30 = 101-04. A partial analysis of another spe- 
 cimen of the same rock yielded to Delesse, silica 29-88, water ll-50,lime 
 0-77, besides traces of oxyd of chrome. 
 
608 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 Garnet- After the epidotic rocks, may be mentioned those consisting chiefly of 
 ^ garnet. A compact white garnet has been described on page 496, as 
 forming a rock, with a little intermingled serpentine ; or as intimately 
 mixed with a silicate approaching to pyroxene in composition, and forming 
 a hard heavy white rock, which in some portions is penetrated by feld- 
 spar, and by a coarsely crystalline hornblende. Red garnet occurs but 
 sparingly in the crystalline rocks of the eastern district in Canada, but is 
 found massive in Chester in Vermont. It also abounds, with kyanite and 
 staurotide, in a very quartzose mica-slate in Cavendish ; and with grey 
 actinolite, and a little chlorite, it forms a bed in Plymouth in the same state. 
 In similar associations in Canada, epidote and chloritoid seem to replace 
 
 Chioritoid. garnet. Chloritoid, as has already been described on page 498, occurs 
 abundantly in grey quartzose micaceous schists. 
 
 The minerals consisting chiefly of silicates of protoxyd, occupy an impor- 
 tant place among the metamorphic rocks now under consideration. Black 
 
 Hornblende, crystalline hornblende schists, holding small red garnets, occur in beds 
 with the serpentines of Mount Albert ; and actinolite, either alone or 
 mingled with talc, forms large beds, as described on page 466. Analyses 
 and descriptions of the diallage rocks which are associated with the 
 serpentines, are given on page 469 ; and the large proportion in which 
 hornblende enters into the composition of the diorites of this region, has 
 
 steatite. been noticed above. The chemical composition of the beds of talc or 
 steatite which abound in this series, has been given on page 470 ; and it 
 now remains to speak of the serpentines. 
 
 serpentine. Those rocks which have serpentine for their basis are conveniently desig- 
 nated by the title of ophiolites. Many facts with regard to their structure 
 
 ophiolites. and distribution will be found on pages 248 and 266. The simple or nor- 
 mal ophiolites are nearly pure massive serpentine ; while others are mixtures 
 of this mineral with variable proportions of carbonate of lime, carbonate of 
 magnesia, or dolomite. All of these varieties are met with in Canada, or in 
 the adjacent state of Vermont. These compound ophiolites are sometimes 
 porphyritic from an admixture of diallage. At other times, they have the 
 aspect of conglomerates, and exhibit rounded or angular masses of pure 
 serpentine of various sizes, imbedded in a dolomitic paste, which is itself 
 more or less colored by intermingled serpentine. A magnesitic ophiolite 
 from Vermont has a gneissoid structure, due to an admixture of crystalline 
 magnesite spar, with scales of talc, apparently showing planes of stratifica- 
 tion. The ophiolite of Mount Albert is marked with red and with green 
 bands, having the aspect of sedimentary layers, page 266. The relations 
 of the serpentine throughout this series, where its out-crop has been traced 
 for hundreds of miles, are always those of an inters tratified deposit, and 
 not of an erupted rock. It occurs with argillite, dolomite, magnesite, 
 diorite, and steatite, with each of which it has been found in contact, and 
 
CHAP. XIX.] EASTERN PALAEOZOIC ROCKS. 609 
 
 it seems occasionally to replace other magnesian rocks. The colors of 
 these ophiolites are of various shades of green, generally much darker 
 than those of the Laurentian series. The pure serpentines are sometimes 
 curiously chequered by veins or seams, as described on page 248 ; and 
 a dark red color occasionally occurs in spots or bands, or pervades the 
 whole mass, which in some cases, at least, is due to diffused hematite. 
 Foliated and fibrous varieties of serpentine often occur in these ophiolites, 
 constituting the varieties called baltimorite, picrolite, and chrysotile, as 
 described on pages 248 and 473. Chromic iron is also a characteristic 
 mineral, both in grains and in interstratified beds and lenticular masses. 
 Magnetic iron ore occurs in these rocks under similar conditions, some- 
 times with ilmenite : see under these titles for further details. The facts 
 with regard to the general distribution of chrome and nickel among the 
 serpentines and other magnesian rocks of this series, will be found under 
 the head of these metals, in the seventeenth chapter. 
 
 Besides the analyses of the serpentines from these ophiolites, which 
 have been given on page 472, a description of some of the principal varie- 
 ties of the rock, and the results of their chemical examination, are sub- 
 joined. A calcareous ophiolite, which occurs on the tenth lot of the sixteenth 
 range of Orford, is fine grained and sub-crystalline, with a somewhat con- 
 dboidal fracture. It is translucent on the edges ; and except in its color, caicareotw 
 which is a mottled greenish-grey, with occasional purple stains, it resembles 
 some common varieties of lime&tone. When in powder, the rock effervesced 
 even in the cold, with acetic acid, which by the aid of heat removed 57-0 
 per cent., consisting of carbonate of lime 91*33, carbonate of magnesia, 
 with traces of iron, 8.67 = 100.00. The remainder was attacked with effer- 
 vescence by dilute nitric acid ; which, by the aid of a gentle heat, dissolved 
 10*76 per cent, of a ferruginous dolomite, consisting of carbonate of lime 
 49*45, carbonate of magnesia 43*68, carbonate of iron 6*87 = 100*00. 
 The residue from nitric acid, when dried at 212 F., equalled 32*00 per 
 cent., indicating a loss of *24 per cent. It was decomposed by heated 
 sulphuric acid, without any effervescence, and was a nearly pure serpen- 
 tine, giving silica 41*20, magnesia 32*16, protoxyd of iron 11*16, lime 
 65, alumina 2*67, water 12*70 = 100*54. The action of acetic acid re- 
 moves all the free carbonate of lime ; attacking at the same time a portion 
 of the dolomite, the remainder of which is afterwards dissolved by the nitric 
 acid. This ophiolite is thus shown to consist of a mixture of serpentine and 
 some aluminous silicate, mingled with carbonate of lime and a little dolomite. 
 
 A dolomitic ophiolite from the shore of Brompton Lake, on the seventh 
 lot of the thirteenth range of Orford, is fine grained and greenish-grey, like i >biolite - 
 the last ; but it is somewhat darker in color, and weathers to a yellowish- 
 brown ; while the pure ophiolites are white on their weathered surfaces. 
 Its fracture is uneven, presenting grains of a crystalline spar ; and it has a 
 
 oo 
 
610 GEOLOGY OP CANADA. [CHAP. XIX. 
 
 fibrous coating in the joints of the rock. Its hardness is a little greater 
 than that of limestone. When reduced to powder, it did not, like the 
 calcareous ophiolite, effervesce with acetic acid ; but it was readily attacked 
 by dilute nitric acid, which removed carbonates of lime, magnesia, and 
 oxyd of iron, with traces of nickel and manganese, and left a residue of 
 51* 9 per cent, of serpentine. The analysis of this gave silica 43-20, 
 magnesia, by difference, 36*11, protoxyd of iron, with nickel, 8-29, water 
 12-40 = 100-00. The soluble portion consisted of carbonate of lime 
 49-58, carbonate of magnesia 46*32, carbonate of iron, with manganese, 
 4*10 = 100*00. The rock is thus a mixture of serpentine and dolomite, 
 congiome- Another dolomitic ophiolite, also from Brompton Lake, on the twelfth lot 
 of the eighteenth range of Orford, is a breccia, or a conglomerate, holding 
 masses of serpentine from a line to an inch or two in diameter, and more or 
 less rounded, although angular in form. These are imbedded in a greenish- 
 white base, and are of various shades of dark green, sometimes appearing 
 nearly black when polished. The analysis of one of these has been given 
 on page 472, II. The rock contains nickel and grains of chromic iron ore. 
 The nature of the cement varies in different parts. A portion having 
 been pulverized, it was attacked with effervesence in the cold, by acetic 
 acid ; which, with the aid of heat, took up twenty per cent, of carbonates, 
 consisting of carbonate of lime. 88 -30, carbonate of magnesia, with a 
 trace of oxyd of iron, 11 70 = 100 * 00. The residue was digested with 
 nitric acid, which dissolved no lime, but a portion of magnesia, and some 
 oxyd of iron and alumina, due to a partial decomposition of the serpentine. 
 This then gave silica 45*10, magnesia, by difference, 34*68, protoxyd of 
 iron 6 * 12, alumina * 80, water 13 * 30 = 100 * 00. A portion from another 
 part of the conglomerate ophiolite, was finely pulverized, and digested 
 for some tune with boiling acetic acid, which dissolved carbonate of 
 lime 7 * 35, carbonate of magnesia 7 * 72, carbonate of iron 1 * 78 = 16 * 85. 
 The residue from this treatment still retained carbonate of magnesia ; for 
 on igniting a portion, and boiling- it for some time with a solution of 
 nitrate of ammonia, which is without action on calcined serpentine, there 
 were dissolved, lime equal to * 3 per cent., and magnesia equal to 3 * 26 per 
 cent, of carbonate. The residue,, still retaining this admixture of carbonates, 
 gave silica 43*93, magnesia, by difference, 35*64, protoxyd of iron 
 7*83, lime, traces, water, and carbonic acid, 12*60 = 100*00. A 
 further trial was made by igniting a portion of this last specimen of the 
 conglomerate, and boiling it with a solution of nitrate of ammonia so long 
 as an odor of ammonia was perceptible, when there were dissolved carbonate 
 of lime 6 * 50, carbonate of magnesia 7 * 65. From these experiments, it is 
 evident that while portions of this conglomerate approach to a calcareous 
 ophiolite in containing a somewhat magnesian carbonate of lime, other por- 
 tions hold a mixture of dolomite and carbonate of magnesia. Veins of from 
 
CHAP. XIX.] EASTERN PALJEOZOIC ROCKS. 611 
 
 four to six lines in breadth are common in this conglomerate. Their walls veins im 
 are covered with a layer of a pale green serpentine, having a fibrous structure 
 perpendicular to the walls of the vein. Upon this is deposited a bluish- 
 white fine grained dolomite ; while in the middle, a nearly pure cleavable 
 calcite occurs. A portion of this dolomite gave carbonate of lime 59*32, 
 carbonate of magnesia 34*15, carbonate of iron 4*83 = 98 '30. The 
 stratified origin of these ophiolites is very evident hi some of the conglom- 
 erate varieties, where bands of different texture and color are seen to 
 alternate. This is very well shown in a calcareous conglomerate ophiolite 
 from Melbourne, which, like that from Orford, has been wrought for orna- 
 mental purposes. 
 
 The predominence of the carbonate of magnesia over the lime, is seen 
 in the example just described ; and in some of the ophiolites of Vermont, 
 carbonate of lime is altogether wanting, being replaced by magnesite. 
 This, according to Drs. Jackson and A. A. Hayes, is the ease with the 
 ophiolites of Lynnfield, Cavendish, and Roxbury, In this, according to 
 the latter observer, fragments of talcose schist and argillite are sometimes P hiolite - 
 imbedded with serpentine in the magnesite, which equals, on an average, 
 38*0 per cent. The results of an examination of the magnesitic ophiolite 
 from Roxbury, undertaken for comparison with the preceding, may here 
 be given. Some specimens of the rock are granular, with an uneven 
 fracture, and are mottled with light and dark green. * Other portions are 
 white and crystalline, with greenish-grey parallel layers of talc and serpen- 
 tine, giving the rock a gneissoid aspect. The white portions are carbonate 
 of magnesia, containing about three per cent, of carbonate of iron, and 
 having a hardness of 4 0, and a specific gravity of about 3*0. The green 
 granular portion of the rock effervesces when boiled with dilute nitric acid ; 
 which removes magnesia, oxyd of iron, manganese, and a trace of nickel, 
 but no lime. The residue was then boiled with a solution of carbonate of 
 soda, which dissolved a portion of silica from the decomposed serpentine, 
 and left a green granular residue, mixed with scales of talc. A portion 
 of this residue, when ignited and boiled with nitrate of ammonia, was 
 found still to contain 1 21 per cent, of carbonate of magnesia. It was 
 however decomposed by sulphuric acid ; and the silica was separated by 
 carbonate of soda from the insoluble talc, which equalled 6*8 per cen k . 
 Deducting this, and the small portion of carbonate of magnesia, the 
 composition of the serpentine, dried at 250 F., was silica 43*34, mag- 
 nesia 39 * 55, protoxyd of iron 5 * 32, oxyd of nickel, traces, water 11 * 79 
 = 100*00. The insoluble talc, separated as above, gave by analysis, 
 silicia 62*60, magnesia 31*30, alumina and oxyd of iron 4*06, water and 
 loss 2 * 04 = 100 00. This ophiolite is thus shown to be an admixture of 
 serpentine, talc, and ferriferous carbonate of magnesia. 
 
612 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 In the preceding analyses, it will be seen that only traces of alumina 
 occur in these ophiolites. A nearly opaque greyish-green rock from the 
 twentieth lot of the first range of Ireland, which resembled serpentine in 
 appearance, and had a specific gravity of 2*65, gave on analysis, silica 
 43*70, magnesia 23'46, alumina with peroxyd of iron 23-00, water 11-57 
 = 101-73. In this rock, the iron exists as protoxyd, and the mineral is 
 like that from the Laurentian series, at the Calumet, described on page * 
 474, an ophiolite mixed with some aluminous mineral. In many cases, the 
 ophiolites of the eastern district include diallage, and pass into the hydrous 
 diallage-rock described on page 469, which contains 6-80 per cent, of alu- 
 mina. Through this, there is an apparent passage to feldspathic rocks 
 containing diallage, and to others holding hornblende, or, as in the diorites 
 of Acton and Upton, more basic silicates, approaching to chlorite in com- 
 position. Both the serpentines and the diorites sometimes become schis- 
 tose ; and the latter seem to graduate into chloritic slates and epidosites, on 
 the one hand, and into hornblendic slates on the other ; so that it is difficult 
 to resist the conclusion that the whole series of rocks just named, from dio- 
 rites, diallages, and serpentines, to talcs, chlorites, and epidosites, have been 
 formed under similar conditions. 
 
 Limestones. ^ ne limestones, dolomites, and magnesites of this series are next to be 
 described. Great masses of pure compact limestone occur in the Quebec 
 group ; but they seem, like the associated dolomites, to be irregular, and 
 interrupted in their distribution, in some parts attaining a considerable 
 thickness, and in others appearing to thin out, or to be replaced by sand- 
 stones. These limestones frequently form masses of many feet in thick- 
 ness, which are without visible marks of stratification, and are destitute of 
 organic remains. The rock is in these cases compact, conchoidal in fracture, 
 and sub-translucent; and it exhibits a banded agatized structure, which 
 leads to the conclusion that it is a travertine, or a chemical deposit from 
 water. Masses several inches in diameter, of a crystalline fibrous carbo- 
 nate of lime, arranged in concentric layers, and closely resembling the 
 modern deposits from calcareous springs, are often imbedded in this lime- 
 
 Travertinee. stone, and have been described on page 445. These travertines are 
 pearl-grey, dove-grey, or occasionally of a pale greenish color, and weather 
 smooth and white. Their analysis shows them to be pure carbonate of 
 lime. Sometimes however this material includes grains of sand, or is the 
 cement of a conglomerate. Such a specimen gave 9-30 per cent, of sand, 
 and -75 per cent, of carbonate of magnesia. The microscopic examination 
 of thin sections of this rock shows it to be finely and uniformly crystal- 
 line, often without any traces of organic remains. 
 
 Dolomites. Interstratified with these travertines, however, are beds of finely granular, 
 opaque limestones, weathering bluish-grey, and holding in abundance the 
 remains of trilobites, and other fossils of the Quebec group. These fossils 
 
CHAP. XIX.] EASTERN PALEOZOIC ROCKS. 613 
 
 are often replaced by a yellow-weathering dolomite. In some other por- 
 tions of the Quebec group, pure grey limestones are met with, as near 
 Missisquoi Bay. Here, as at Quebec, they are interstratified with yellow- 
 weathering dolomites, which, throughout the eastern district, are more 
 abundant than the pure limestones. They are generally mixed with a con- 
 siderable portion of silicious matter, and more rarely with clay ; and they 
 commonly contain a portion of carbonate of iron in their composition, which 
 causes them to weather yellowish or reddish-brown, and to become friable 
 to a considerable distance from the surface. They are, besides, very gener- 
 ally traversed by narrow veins of white quartz, or of calcareous spar, which 
 intersect each other, giving to the surface of the rock a chequered appear- 
 ance. These veins are found alike in the metamorphosed region ; and in 
 the vicinity of Quebec, where the dolomites are unaltered, and slightly 
 bituminous. They often contain small masses of crystalline calcite filling 
 cavities, which, at other times are lined with crystals of calcite or of quartz, 
 forming small geodes, as near Missisquoi Bay, where the dolomite also 
 encloses masses of black and grey chert or hornstone. 
 
 These dolomites in many parts, especially in the vicinity of Quebec, as congiomer- 
 described in the section on page 227, include conglomerate beds, which ate8t 
 hold, in a red-weathering sandy dolomitic base, grains and rounded masses 
 of pure limestone, often resembling the travertines of the series ; besides, 
 more rarely, fragments of quartz, of shale, and also small masses of a 
 nearly pure crystalline dolomite. These last are perhaps concretionary 
 in their origin, and not imbedded fragments. 
 
 The following are some analyses of the dolomites of this series : I is a Analyses of 
 fine grained variety from the island of Orleans, of which the insoluble dolomites - 
 residue contains a little clay. II is associated with the travertine at the 
 lime-quarry at Point Levis. It is highly crystalline, and shows in its 
 fracture broad surfaces of cleavage, like the Eontainebleau sandstone : 
 the insoluble portion is pure quartz. Ill is a white-weathering dolomite 
 from Philipsburg, enclosing a large quantity of quartz sand. IV is a 
 greyish, granular dolomite from the ninth lot of the ninth range of Sutton, 
 which contains, in some parts of the bed, thickly disseminated octahedral 
 crystals of magnetic iron, with chlorite, and weathers brownish-black, from 
 the presence of a large proportion of manganese. The insoluble residue 
 was nearly pure quartz. 
 
 I. II. III. IV. 
 
 Carbonate of lime, 45-06 53-04 25-60 40-10 
 
 " magnesia,..., 31-81 31-96 19-40 20-20 
 
 " iron, 10-31 5-80 10-65 
 
 " manganese traces .... 7-65 
 
 Insoluble, 13-80 8-80 55-00 21-40 
 
 100-98 99-60 100-00 100-00 
 
614 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XIX. 
 
 Chrome and 
 nickel. 
 
 Titanium. 
 
 The presence of about twenty per cent, of dolomite in some of the 
 yellow-weathering green shales of the island of Orleans has been noticed 
 above. A bed of compact earthy rock, interstratified with the shales at 
 Point Levis, and decomposing to a yellow earth, gave to acids about fifty 
 per cent, of ferriferous dolomite. The insoluble residue was chiefly a clay, 
 holding about four per cent, of alkalies, of which two thirds were 
 potash. One of the small masses of dolomite from the magnesian con- 
 glomerate of Point Levis gave of carbonate of lime and a little iron, by 
 difference, 61-6, carbonate of magnesia 33-8, silicious sand 4-6 = 100-00. 
 
 A black, thin-bedded compact dolomite, which weathers reddish-yellow, 
 occurs among the black shales of this series on the Magdalen River, and is 
 noticed on page 268. The surfaces of the beds are marked by thin crys- 
 talline crusts of calcite. The analysis of this limestone gave carbonate 
 of lime 43*17, carbonate of magnesia 32-12, alumina with oxyd of iron, 
 the latter in part as carbonate, 4-10, insoluble 20-30 = 99-69. The 
 insoluble residue is a fine clay ; and the rock, which by calcination assumes 
 a pale buff color, makes a superior cement, which hardens in a few minutes 
 under water. 
 
 The above dolomites were all examined for chrome and nickel without 
 success ; but both of these metals are frequent in the dolomites of the 
 metamorphic region, and in one case were met with in an impure, some- 
 what magnesian limestone from the unaltered strata of the Quebec group 
 at Granby, noticed on page 245. This rock, which is interstratified with 
 red and greenish shales, and green sandstones holding scales of mica and 
 graphite, was digested with acetic acid, which attacked it with strong 
 effervescence. A little hydrochloric acid was added towards the close of 
 the operation, and there were dissolved carbonate of lime 30-08, mag- 
 nesia, calculated as carbonate, 3-68, oxyd of iron and alumina 5-45, oxyd 
 of manganese -58 = 39-79. The residue gave on analysis, silica 53-20, 
 titanic acid 6-20, alumina 7-90, peroxyd of iron 15*75, magnesia 8-79, 
 oxyd of chrome *10, oxyd of nickel *15, volatile 4-80, with alkalies, oxyd 
 of manganese and loss 3*11 = 100-00. In another trial, 5*3 per cent, of 
 titanic acid were obtained from this rock. 
 
 In the analyses of the various magnesian limestones hitherto given, the 
 amount of carbonate of magnesia does not exceed that required to form 
 a dolomite with the carbonate of lime, the proportions being 54-35 of 
 carbonate of lime to 46*65 of the carbonate of magnesia, or one equiva- 
 lent of each. Any excess of carbonate of lime is present in an uncom- 
 bined state, and may be separated by dilute acetic acid, in which the 
 dolomite is much less soluble than the simple carbonate. The carbonates 
 of iron and manganese, which these dolomites so often contain, generally 
 replace a portion of the magnesian carbonate, so that the lime still 
 amounts to an equivalent. In some cases however the carbonate of mag- 
 
CHAP. XIX.] EASTERN PALEOZOIC ROCKS. 615 
 
 nesia predominates ; and an example of a dolomite with an excess of magne- 
 sian carbonate, has been lately described by Prof. G. F. Barker from 
 rocks supposed to belong to this series in Brandon, Vermont. It gave 
 to analysis carbonate of lime 40-38, carbonate of magnesia, 51-40, carbo- 
 nate of iron 3-67, insoluble, quartz, etc. 3-44 = 99-89. (Geology of 
 Vermont, 769.) 
 
 In this rock, after excluding the carbonate of iron, there are about 
 three equivalents of carbonate of magnesia to two equivalents of car- 
 bonate of lime ; and this composition shows a passage towards the mag- 
 nesites which are found in this series, and which occasionally contain a little 
 carbonate of lime, probably as dolomite. These rocks have already been 
 described on page 457 ; where it has been shown that they occur in Sut- 
 ton in mica-schist, and in Bolton interstratified between steatite and an 
 impure serpentine, which passes into diorite ; in both cases, weathering 
 yellow from the presence of a large proportion of carbonate of iron, colored 
 green by a chromiferous mica, and containing a portion of oxyd of nickel. 
 In the latter township, it also occurs in argillite, aa a compact uncrystal- 
 line rock resembling the magnesian limestones of the region, for which it 
 may perhaps have been mistaken in many different localities. A bed of 
 steatite, stained green with oxyd of nickel, which occurs at the falls of the 
 river Bras, in St. Francis, Beauce, is filled with crystalline grains of car- 
 bonate of magnesia. In many other localities however, the steatites of this 
 series contain a ferruginous bitter-spar or dolomite. 
 
 The mineral species found in the altered limestones, dolomites, and iron ores, 
 magnesites of the Quebec group in Canada, are few in number. Among 
 them may be mentioned serpentine, since some of the ophiolites pass into 
 limestones and dolomites. To these may be added small portions of talc, 
 chlorite, and chromiferous mica. Crystals of garnet have been observed 
 in a few localities in the dolomites ; and the remarkable locality of chrome- 
 green garnets and crystallized pyroxene, found near the serpentine of 
 Oxford, should probably be regarded as pertaining to the calcareous por- 
 tion of the series. 
 
 The beds of iron ore found in this series consist chiefly of iron slates, itabirite. 
 composed of fine grains of specular iron, more or less mingled with 
 quartz, and often with chlorite ; so that they offer various grades, from a 
 nearly pure compact or micaceous red oxyd, to chloritic and quartzose 
 schists, very poor in iron. They have been noticed on page 245, by the 
 name of specular schists, and are identical with the itabirite of Brazil. 
 Some analyses of these specular schists from Sutton, and from Brome, 
 gave from fifty to seventy per cent, of peroxyd of iron ; the insoluble matter 
 being in some parts chiefly quartz, and in others containing an admixture 
 of chlorite. In many cases, the ore takes the form of magnetite, and is 
 imbedded in chloritic slate, or in a chloritic dolomite like that described 
 
I 
 
 V 
 
 616 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 on page 613. Both of these ores are known in Vermont, and also in 
 South Carolina, where they occur in the same associations as in Canada, 
 and have been carefully studied by Lieber. These ores sometimes con- 
 tain small portions of titanium; and the same is true of the massive 
 magnetite which is found in St. Francis, in serpentine. The chromic iron 
 ore also forms beds, which may be looked upon as belonging to the rock- 
 Chrome ore. masses of these series. The variable and often considerable portions of 
 alumina and magnesia which occur in combination with the oxyds of chrome 
 and iron in this ore, suggest that the elements of it have been deposited from 
 solution, under conditions somewhat similar to those which have given rise 
 to the oxyds of iron, manganese, and aluminum found elsewhere in strati- 
 fied rocks. The part which the sulphurets of copper play in the beds of the 
 Quebec group, as described on page 515, is such, that they may be also 
 regarded as forming part of the stratified rocks of this series. 
 
 The group of rocks just described, is recognized by its mineralogical 
 characters throughout the Appalachian chain. Among its most constant 
 marks are the frequency of serpentines, steatites, and other magnesian 
 rocks, containing chrome and nickel, often with titanium. To this may 
 be added the frequent occurrence of gold with the so-called talcose 
 schists of the series, sometimes in veins, but occasionally disseminated, like 
 the copper, in beds. Similar mineralogical associations occur in California, 
 where serpentines and magnesites, with both chrome and nickel, occur, 
 resembling those of Canada. Serpentines and steatites of like characters 
 occur in Newfoundland ; and beyond the sea, in the Highlands of Scotland, 
 in a series of rocks resembling those of the Notre Dame Mountains. In 
 Norway, what is called the schistose division of the Primitive Slate forma- 
 tion, as developed about Drontheim and in the Dovrefield Mountains, 
 exhibits a marked correspondence with the crystalline strata of the Quebec 
 group, as shown by Mr. Macfarlane in his memoir already referred to on 
 page 586. These rocks are, by the Swedish geologists, placed at the base 
 of the Silurian series ; into the fossiliferous strata of which, according to 
 Keilhau, they appear to graduate, through a series of slates and sand- 
 stones. The similar strata in Scotland are by Murchison and Ramsay 
 regarded as Silurian, and as newer than the oldest fossiliferous strata. 
 Mineralogical associations like those of the Quebec group, are met with in 
 strata in Cornwall, in the Vosges, the Alps, and the Urals, and many other 
 regions ; but it remains to be seen how far all these strata are of the age 
 of the similar rocks of Norway and of eastern North America. 
 Higher As regards the Upper Silurian and Devonian rocks of the eastern dis- 
 
 rocka. trict, little can at present be added to the facts already detailed in the 
 sixteenth chapter. On the Chaudiere and St. Francis Rivers, and their 
 tributaries, and on Lake Memphramagog, these rocks are seen in an altered 
 condition ; and, as described on page 428 and the succeeding pages, they 
 
CHAP. XIX.] EASTERN PALAEOZOIC ROCKS. 617 
 
 consist of quartzites and feldspathic sandstones, interstratified with argil- 
 lites, and with micaceous schists. In one place, strata abounding in black 
 hornblende, and containing small garnets, are met with. Occasionally, 
 as on Lake Memphramagog, black calcareous schists are found, containing 
 disseminated finely divided plumbago. 
 
 The argillites of these upper strata have, in some parts, the character of 
 roofing slates. One of these, from the township of Westbury was greenish- 
 blue in color, with a silky lustre on the cleavage surfaces. It was trans- 
 lucent on the edges, and had a specific gravity of 2' 77. Its analysis 
 gave silica 65*85, alumina 16-65, protoxyd of iron 5-31, lime *59, magnesia 
 2-95, potash 3*74, soda 1-31, manganese, traces, volatile 3-10 = 99-50. 
 A variety of argillaceous rock on Lake St. Francis is dark bluish-grey, 
 earthy in texture, and has an imperfect slaty cleavage. It contains 
 crystals of andalusite, which vary from one twentieth to one fourth of an 
 inch in diameter ; besides small scales of a black micaceous mineral, 
 irregularly disseminated, and in no particular plane. In this locality, the 
 andalusite is only seen near to a mass of intrusive granite ; but elsewhere 
 in the vicinity, it appears to be a result of regional metamorphism. 
 
 The altered limestones of this series are often micaceous, and sometimes 
 fissile from the presence of thin films of brownish or yellowish mica between 
 the layers. In some parts of their distribution, they become interstratified 
 with micaceous schists, which are themselves calcareous ; and in their south- lu 
 ward extension, these rocks constitute the calcareo-micaceous slate forma- 
 tion of the Vermont geologists. The limestone strata at Dudswell are 
 characterized by the fossils enumerated on page 433. These, which are 
 sometimes nearly black in polished sections of the stone, are imbedded in a 
 yellow crystalline magnesian limestone. In other beds, the structure seems 
 to show that thin layers of a grey fossiliferous limestone have been broken, 
 and cemented with the yellow magnesian paste, which itself sometimes 
 forms layers half an inch in thickness. Analysis shows that the fossils, 
 and the grey limestone which frequently envelops them, are nearly pure 
 carbonate of lime. The yellow magnesian portion, on the contrary, gave 
 on analysis, carbonate of lime 56-60, carbonate of magnesia 11-76, carbon- 
 ate of iron 3-23, insoluble 26-72 = 98-31. This, however, contained a 
 mixture of dolomite and of carbonate of lime ; and on treating the rock 
 with cold dilute acetic acid, the latter was removed, together with 4-0 
 per cent, of carbonate of magnesia. The residue, treated with dilute 
 hydrochloric acid, left undissolved 52-0 per cent, of sand and pyrites ; and 
 the soluble portion consisted of carbonate of lime 51-75, carbonate of mag- 
 nesia 35-73, carbonate of iron 12-52 ; being a yery ferruginous dolomite. 
 These limestones have been polished as marbles. In the arrangement of 
 their colors, they resemble the Portor marble from Italy, which is like 
 
veins. 
 
 618 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 them in composition ; the black parts in this also being a nearly pure 
 limestone, while the yellow veins are a ferruginous dolomite. 
 
 Mineral The veins of infiltration and segregation which are found in the eastern 
 
 district have already been noticed in the previous portion of this volume. 
 Those which contain feldspar, with quartz and mica, are described on page 
 476 ; and others, in which quartz and bitter-spar are the gangue of 
 sulphurets of copper, on pages 257 and 515. Small veins of calcite, 
 purple fluor-spar, and galena, occur in the black slates at Quebec ; and a vein 
 of heavy-spar is found in serpentine, on the river Bras, in St. Francis, 
 Beauce. All the above, so far as known, are confined to the strata of the 
 Quebec group ; but veins of quartz, sometimes holding ores of arsenic, 
 zinc, lead, silver, and gold, are found, both among the rocks of the Quebec 
 group and the argillites of the Upper Silurian and Devonian series. The 
 quartzites and micaceous schists of the same series hold other quartz veins, 
 containing ores of copper, with mica and crystallized apatite (see pages 
 437 and 517). The veins of calcite holding galena, which have been 
 described at page 400, as occurring in the Gasp^ limestones, may also be 
 mentioned in this connection. 
 
 BOOKS OF THE WESTERN PALAEOZOIC DISTRICT. 
 
 It has already been explained that in the western district of palaeozoic 
 rocks, are included those to the west and the north of the great line of break, 
 which brings up the lower rocks that form the western portion of the 
 eastern district. The Upper Copper-bearing rocks of Lake Superior, which 
 are regarded as the equivalents of these last, are however excluded from 
 the present description of the western district, which comprehends all the 
 formations from the Potsdam to the Portage and Chemung group, both 
 inclusive, as they have been described in preceding chapters of this volume. 
 
 The strata of this great district have nowhere been exposed to violent 
 undulations, and are for the most part nearly horizontal. They are every- 
 where unaltered, except in the immediate vicinity of some of the intrusive 
 masses, which abound in the eastern part of the district. The strata are 
 moreover generally impregnated with soluble saline and alkaline salts, and 
 give rise to great numbers of mineral springs, whose history and relations 
 to the different groups of strata have been discussed in a preceding chap- 
 ter. It is proposed in the following pages to notice the most important 
 chemical and mineralogical facts in the history of these various formations, 
 taken in ascending .order. The observations of the New York geologists, 
 and the more recent and important chemical researches of Mr. J. D. 
 Whitney and others, on the palaeozoic rocks of Michigan, Iowa, and Wis- 
 consin, will also be referred to in this connection. 
 
CHAP. XIX.] WESTERN PALEOZOIC ROCKS. 619 
 
 The Potsdam formation, which appears at the base of the series, is in Potsdam 
 this western division, for the most part, a pure quartzose sandstone, or hard formation - 
 vitreous quartzite, made up of sharp, angular grains. Occasionally it is 
 feebly coherent, and crumbles to sand at the outcrop ; and not unfrequently 
 it is a conglomerate, holding pebbles of quartz, grains of feldspar, or, more 
 rarely, fragments of green and black shale. In many localities, it is so sandstone, 
 pure as to be fitted for the manufacture of glass ; while in some parts, it is 
 colored red by oxyd of iron, which occasionally appears in the form of 
 little masses and layers of red hematite, as described on page 93. Some 
 beds of the sandstone contain small portions of carbonate of lime, or are 
 magnesian, indicating a transition to the mineralogical characters of the 
 overlying division, to which the name of the Calciferous formation is given ; Calciferous 
 although, as has already been described, its lower part is chiefly a bluish- fo 
 grey crystalline dolomite, often slightly ferruginous, and weathering yel- 
 lowish-brown. It generally exhibits small geodes, filled, for the most part, Dolomite, 
 with calcite ; but in some parts lined with quartz crystals, or holding crys- 
 tallized sulphates of baryta and strontia, or more frequently gypsum, as 
 described on page 459. The upper portion of this series is a calcareous Gypsum, 
 argillite, sometimes curiously concretionary in its structure, as noticed 
 on page 113. The dolomite of this formation at Mingan is nearly pure. 
 A variety from Beauharnois, which holds masses of gypsum, and is shaly, 
 contains a considerable amount of insoluble matter. A specimen of the 
 compact bluish-black dolomite from Rigaud, holding masses of calcite, gave 
 carbonate of lime 33*70, carbonate of magnesia 27*00, oxyd of iron and 
 alumina, by loss, 2*40, sand and clay 36*90 = 100*00. 
 
 The Chazy formation includes in its lower portion a considerable amount chazy for- 
 of shales and sandstones, together with impure magnesian limestones ; but ma ? on - 
 towards the summit pure limestones prevail. This formation is thus, litho- 
 logically, a passage from the silicious and magnesian rocks beneath, to the 
 pure limestones of the Trenton group. Geodes of calcite and of sulphate 
 of strontia, which characterize the rocks of the Calciferous formation, are 
 met with in strata supposed to belong to the Chazy at Kingston, and in its 
 vicinity (page 459) ; and the argillaceous magnesian beds at Nepean, used 
 for the fabrication of the Hull hydraulic cement, are also geodiferous. A 
 specimen from this locality gave to the analysis of Delesse, carbonate of 
 lime 45*30, carbonate of magnesia 12*77, alumina and oxyd of iron 12*52, 
 insoluble argillaceous residue 19*77, water and loss 9*64 = 100*00. 
 
 The dark colored compact fossiliferous limestone of the Chazy formation 
 near the St. Lawrence toll-gate, Montreal, contains between its beds, thin 
 interrupted layers, occasionally an inch or more in thickness, of a yellow 
 crumbling material, which holds great numbers of fragments of encri- 
 nal stems. The analysis of a portion of this matter, from which the 
 fossils had been separated, gave carbonate of lime 40*95, carbonate of 
 
620 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 magnesia 24-19, carbonate of iron 27-03, silickms sand 9-01 = 101-18. 
 This is evidently a very ferruginous dolomite in a state of partial decom- 
 postion. A portion of the grey limestone, about an inch from the magne- 
 sian layer, yielded 18*4 per cent, of insoluble argillaceous matter, and 
 only 1-09 of carbonate of magnesia. Other reddish, pulverulent layers, 
 among the strata of this locality, contain carbonate of lime with a large 
 amount of hydrous peroxyd of iron, but no magnesia. Such a material in 
 one instance forms the cement of a breccia of fragments of dark blue lime- 
 stone. It was perhaps originally a double carbonate of lime and protoxyd 
 of iron, now partially decomposed. In some of the black fine grained beds 
 in the vicinity, the organic remains are replaced by a coarsely crystalline 
 yellow-weathering dolomite, which forms a solid mass having the external 
 
 Doiomitic form of the fossil. This rock, which is nearly free from magnesia, dis- 
 solves in hydrochloric acid with evolution of a little sulphuretted hydro- 
 gen, and leaves an argillaceous residue, mixed with pyrites, and colored 
 with a carbonaceous matter. 
 
 Trenton These dolomitic casts of fossils are also found in the same formation at 
 
 group. Mingan, and in the limestones of the Trenton group at Ottawa. Here 
 the limestone is compact and dark bluish-grey. It gave by solution in 
 acids, 3-9 per cent, of clay and sand, and 0-6 per cent, of oxyd of iron 
 with alumina, without any magnesia. The fossil casts are those of the 
 interior of species of Orthoceras, Pleurotomaria, Murchisonia, and perhaps 
 other genera. They are very abundant, coarsely crystalline, and bluish- 
 white within ; but on the weathered surface of the rock they appear in 
 high relief, and are weathered to a reddish-brown. Dilute acids remove the 
 limestone matrix, and the fossil is then seen to be in many cases but par- 
 tially replaced by the dolomite. That portion which was uppermost in the 
 stratum is often filled by the limestone, in some instances to the extent of 
 one third or one fourth of the whole, while in other specimens the entire 
 mould is filled with dolomite. Both here and at Montreal small veins of 
 dolomite, no thicker than paper, are found cutting the rock, and running 
 from the fossils. In the interior of some of the larger casts, are found 
 drusy cavities lined with crystals of dolomite and of quartz. An analysis 
 of a specimen from this locality has been given on page 457. The 
 limestones of the Trenton group moreover contain, in other localities, 
 small concretions or grains of a yellow-weathering dolomite, which perhaps 
 replace organic remains, and may be seen at Montmorenci Falls, and on 
 the Jacques Cartier River. Apart from these, however, the limestones of 
 this group, so far as examined, are nowhere magnesian. That from 
 
 umeetoaee. Ottawa, as just stated, gave no trace of magnesia on analysis. I is a fine 
 grained, almost black limestone, from Ste. Rosalie, near St. Hyacinthe, 
 yielding a very pure lime ; and II is a coarser grained limestone from the 
 same vicinity, which is penetrated by seams of shale and grains of pyrites, 
 
CHAP. XIX.] WESTERN PALAEOZOIC ROCKS. 621 
 
 and gives an inferior lime. It is not certain whether these specimens 
 belong to the Chazy or to the Trenton group. 
 
 Carbonate of lime 
 
 magnesia,, 
 
 Oxyd of iron and alumina, . 
 Insoluble, 
 
 100-20 100-10 
 
 The first of these limestones, when gently ignited, became nearly white, 
 and lost only -3 per cent, of its weight. When dissolved in hydrochloric 
 acid, it gave off a trace of sulphuretted hydrogen. 
 
 The insoluble portion of these limestones is generally a very fine argil- insoluble 
 laceous matter, with a large proportion of silica and potash, and approaches m 
 to orthoclase feldspar in composition. The analysis of the residue 
 from a specimen of the Chazy limestone from Montreal is given on page 
 582. The compact brown limestone from Paquette's Rapids, which holds 
 silicified fossils, left on solution 7*0 per cent, of impalpably fine feldspathic 
 matter, with a few grains of pyrites, which were separated by nitric acid. 
 The residue gave to dilute soda ley, traces only of silica ; and after ignition, 
 it yielded by an incomplete analysis, silica 77*2, alumina 15-2, and potash 
 8-5 = 95*9. In an examination of the buff-colored magnesian limestone 
 which lies at the base of the Trenton formation in Wisconsin, Mr. Whitney 
 obtained twenty-two per cent, of insoluble matter, whose analysis gave 
 silica 63-7, alumina 14-7, peroxyd of iron 3-5 ; the remainder being alkalies, 
 chiefly potash, with a little magnesia, A dove-colored limestone of the 
 Black River formation, from Lake Couchiching, is fine grained, homogenous, 
 compact, with a conchoidal fracture, is translucent ont he edges, and re- 
 sembles in aspect some hornstones. It is a nearly pure carbonate of lime, 
 containing however 1-27 per cent, of carbonate of magnesia, and 1-17 per 
 cent, of insoluble matter, of which *8 per cent, is soluble silica. 
 
 The limestones of the Chazy and the Trenton groups almost always 
 give off a characteristic odor of bitumen, when struck or dissolved in 
 acids ; but the bituminous matter in these is generally very minute in 
 quantity. In some cases, however, mentioned on page 521, its amount is 
 more considerable . Small grains of pyrites , of yellow blende , and of galena, 
 are found in many localities disseminated in these limestones. 
 
 The upper portion of the Trenton limestone becomes interstratified with utica for- 
 thin layers of black shales, which form a transition to the black pyroschists mation< 
 of the Utica formation. Similar black bituminous shales are interstratified 
 a little higher up in the series, among the grey and green shales and sand- 
 stones which constitute the Hudson River formation. These black shales, 
 in Canada, are highly calcareous, and often pass into impure limestones. 
 
622 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 Of two specimens of this kind from Collingwood, one gave to dilute acids 
 fifty-three, and another fifty-eight per cent, of carbonate of lime, with a 
 little magnesia and oxyd of iron. The insoluble snuff-brown argillaceous 
 residue from the former, when ignited in a close vessel, gave off 12-6 per 
 cent, of volatile combustible matter, leaving a coal-black carbonaceous 
 residue, which, when calcined in the open air, lost 8-4 per cent, additional, 
 and became ash-grey. The insoluble residue from the second specimen 
 was digested for some time with heated benzole, which took up from it 
 about one per cent, of a solid brown bituminous matter. It then no longer 
 gave the odor of bitumen when heated, but a smell like that of burning 
 lignite. The matter, which had thus been treated with benzole, still gave 
 by ignition, 11-8 per cent, of volatile and inflammable matters. It was not 
 attacked by a boiling solution of caustic soda. Portions of this shale, 
 when distilled in close vessels, give from four to five per cent, of oily and 
 tarry matter, besides combustible gases and water. 
 
 A series of careful analyses of various specimens of these pyroschists 
 from the IJtica formation in Canada, were made by Messrs. Chandler and 
 Kimball, for Prof. J. D. Whitney, and are published by him in the Report 
 on the Geology of "Wisconsin, vol. i, p. 184. I is a blackish-brown, very 
 fine-grained rock, from Cape Smith, Lake Huron. It has a somewhat 
 conchoidal fracture, is not schistose in its structure, and contains no traces 
 of fossils. II is from an island to the north of Maple Cape, and is blackish- 
 brown, fine grained, and earthy in texture, with a laminated structure, 
 and contains no fossils. Ill is from Ste. Anne, Montmorenci, and is dark 
 brown, shaly, and contains graptolites. IV is from Gloucester, and is 
 a black shale filled with fragments of trilobites and crinoids. In these 
 analyses the carbonates of lime and magnesia, with the alumina and oxyd 
 of iron, were removed by solution in acids, and the elements of the organic 
 matter determined in the insoluble portion. 
 
 I. II. III. IV. V. 
 
 Clay and sand, 38-45 34-60 37-26 48-27 73-57 
 
 Carbon, 6-83 6-63 -61 6-99 15-03 
 
 Hydrogen, -74 -77 -83 1-13 1-65 
 
 Oxygen, 3-20 2-96 1-71 3-39 5-39 
 
 Carbonate of lime, 45-02 49-31 52-60 20-30 1-29 
 
 " magnesia,... 2-09 2-53 3-42 11-48 '76 
 
 Alumina and oxyd of iron,. 2-16 2-09 3-29 7-99 2-79 
 
 98-49 98-89 99-72 99-55 100-48 
 
 The analysis V in the above table is that of a pyroschist from this forma- 
 tion, in the lead region of Wisconsin. It was dark chocolate-colored, 
 weathering greyish-white, and showed no trace of fossils. It is chiefly 
 silicious, containing only small amounts of carbonates, but is very rich 
 in carbonaceous substances, and gave by ignition in a close vessel, 14*12 
 
CHAP. XIX.] WESTERN PALEOZOIC ROCKS. 623 
 
 per cent, of volatile and combustible matters, leaving 6-84 per cent, of organic 
 carbon, which was removed by calcination in the air. The amount of car- matters * 
 bon in these shales is in no way proportionate to the darkness of their 
 hue, and the organic matter in them is very light colored. This is evident 
 in a yellowish-brown silicious shale examined by Whitney, which contained 
 eleven per cent, of combustible substances ; and in another similar rock, 
 yielding over sixteen per cent, which was light yellowish-brown, becoming 
 of a bluish-ash color on exposure to the air. Both of these rocks con- 
 tained minute fossils, chiefly Lingulae ; and they blackened when exposed 
 to heat, burning with a bright flame. The experiments of Dr. C. F. 
 Chandler, show, on the contrary, that the black, glazed, and apparently 
 highly carbonaceous shales from the valley of the Hudson River, which 
 probably belong to the lower rocks of the eastern district, contain from 
 one half to one per cent, of fixed carbon, but yield no volatile combustible 
 matters. (Geology of Iowa, vol. i, 359.) The source of the hydro- 
 carbonaceous substance which exists in these pyroschists, in a form 
 entirely distinct from bitumen, and in a rock of a marine formation, is not 
 easily determined. It may arise from the decomposition and complete 
 disintegration of either animal or vegetable remains, and seems to be not 
 unlike in its nature to vegetable mould. 
 
 The Silurian rocks of the West examined by Hall and Whitney, present 
 some interesting points of comparison with those of Canada. The Pots- 
 dam and Calciferous formations are there,- as here, represented by great 
 alternations of quartzose sandstones and dolomites, occasionally holding 
 green-sand (page 488), and terminated by a buff-colored magnesian lime- 
 stone, which is regarded as the representative of the Chazy, Birdseye, and 
 Black River formations. A specimen of dolomite from this part of the Galena 
 series on the Escanaba River contains an excess of magnesian carbo- io 
 nate. Its analysis gave to Whitney, carbonate of lime 25*28, carbonate 
 of magnesia 32-77, the remainder being chiefly silicious sand (Geology of 
 Lake Superior, ii, 193). The blue limestone, which there represents the 
 Trenton formation is, however, like the same rock in Canada, a pure lime- 
 stone, but is overlaid by the Galena formation, which is the great lead- 
 bearing rock of Iowa and Wisconsin. This is a pure dolomite,, which in 
 some localities seems to pass into the Trenton limestone, and which has no 
 representative in Canada. It is there overlaid by the Utica and Hudson 
 River formations, with their pyroschists just noticed, which are much less 
 calcareous than the same strata in Canada. 
 
 The strata of the Hudson River formation in Anticosti are made up almost Anticosti 
 entirely of limestones ; and they are there followed by a series of pure lime- rou P- 
 stones, interstratified with small quantities of shaly and argillaceous rocks, 
 which make up the Anticosti group. The lower portions of this are 
 represented in Western Canada and New York by sandstones and red 
 
624 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 and green shales, which constitute the Medina and Clinton formations. 
 These red shales include in one part a band of fossiliferous red hematite ; 
 and at the base of the latter formation on Lake Huron is a considerable 
 mass of dolomite, holding silicified fossils. 
 
 Niagara The beds at the base of the Niagara formation, which at Thorold yield 
 
 >nuation. ft jjyjjjgoJjg cement, contain but little magnesia; but the great part of 
 the formation is dolomitic. It holds nodules and masses of chert in abun- 
 dance, and. as already described, contains small quantities of the sulphurets 
 of lead and zinc, together with geodes holding bitter-spar, calcite, fluor- 
 spar, and sulphates of baryta and strontia, with anhydrite and gypsum. 
 
 Dolomites. Small portions of the latter mineral are occasionally met with in the 
 Medina formation, and even among the shales of the Hudson River 
 formation on Lake Huron. They seem to be the precursors of the great 
 development of gypsum which occurs in the Onondaga formation. A 
 portion of the pearl-spar from Niagara Falls was found on analysis to 
 contain carbonate of lime 55*3, carbonate of magnesia 40-9, carbonate of 
 iron 3-4 = 99-6. 
 
 Gueipu for- Succeeding to the Niagara formation is that of Guelph, which seems 
 tlon> to be in all cases a pure dolomite, and is frequently made up of brilliant 
 crystalline grains, which under a lens are seen to have a characteristic 
 pearly lustre. The rock is generally porous, cellular, and exhibits small 
 cavities lined with crystals. The organic remains, which were common in 
 this formation, have in most cases been removed by solution. In many 
 cases, as described on page 338, the shell has been simply enveloped in 
 the rock, and has left only a cavity corresponding to its exterior. At 
 other times, the interior of the shell was also filled with the dolomite ; so 
 that the cavity corresponds only to the thickness of the shell, of which 
 the markings of both the interior and exterior surfaces are preserved. 
 
 More rarely, the cavities thus formed have been filled up with calcareous 
 matter, apparently replacing the substance of the shell ; and in one place, 
 great numbers of encrinal fragments have become replaced by a white 
 sparry dolomite, whose color contrasts with the yellowish hue of the base. 
 This last rock, which came from Strange's quarry, Rockwood, was how- 
 ever, like the others, cellular, and a pure dolomite. It was submitted to 
 analysis, with another specimen without fossils, from the same locality, a 
 third from Howitt's quarry, Puslinch, and a fourth from McDonald's 
 quarry, Guelph. The first and second gave respectively -90 and '65 
 per cent, of insoluble sand, while the others dissolved without remainder. 
 All of these were pure dolomites, yielding from fifty-three to fifty-four per 
 cent, of carbonate of lime, with traces of oxyd of iron. 
 
 To the Guelph dolomite succeeds the Onondaga formation, which has 
 been minutely described in the thirteenth chapter, both with regard to its 
 distribution, and to its mineralogical and lithological characters. The 
 
CHAP. XIX.] 
 
 WESTERN PALEOZOIC ROCKS. 
 
 625 
 
 absence of organic remains, the interstratified beds of gypsum, the beds 
 of dolomite marked by prismatic and hopper-shaped forms ; with others filled formatlon 
 with thin, lenticular crystals of calcite, whose loss gives to the weath- 
 ered surface a curiously fissured appearance, have all been noticed ; as 
 have also the vesicular cavities in certain beds of dolomite, forming the 
 vermicular lime-rock of Vanuxem. These cavities, in the recently frac- 
 tured rock are found to contain pulverulent carbonate of lime, whose 
 removal gives to the weathered surface its carious appearance. The hopper- 
 shaped impressions, which are supposed to have been formed by crystals 
 of common salt, have since been found between two beds of this series, near 
 York. In a specimen from this place, from which the accompanying figure 
 is drawn, are other similar depressions, not more than half an inch in diameter. 
 
 433. HOPPER-SHAPED MOULD IN DOLOMITE. 
 
 From the lower bed. Natural size. 
 
 After referring to the descriptions already given, it will be sufficient to give 
 the analyses of some argillaceous dolomites of this series, which are some- 
 times employed for the fabrication of hydraulic cement. The first two are 
 by Delesse : I is a dark grey earthy rock, from Martindale's gypsum 
 quarry at Oneida ; II is a specimen of the vesicular dolomite, brownish- 
 yellow in color, from the gypsum quarries at Paris, on the Grand Kiver ; 
 and III is a greenish crumbling shaly rock from the same locality. 
 
 I. II. III. 
 
 Carbonate of lime, 39-91 51-33 25-20 
 
 magnesia, 34-15 40-91 19-70 
 
 Argillaceous residue, 22-10 5-50 52-20 
 
 Water, 3.. 34 2-26 2-90 
 
 100-00 100.00 100-00 
 
 The argillaceous matter in the first of these dolomites was attacked by 
 hydrochloric acid; which dissolved 6-25 per cent, of alumina, with a little 
 peroxyd of iron. 
 
 PP 
 
626 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XIX. 
 
 Soda in 
 limestones. 
 
 Dolomitic 
 conglomerate. 
 
 The great mass of strata, from the Clinton to the Onondaga formation 
 inclusive, in Western Canada, is thus magnesian, and, for the most part, 
 approaches to a pure dolomite : the same fact has been observed by Mr. 
 Whitney throughout these formations, as far to the westward as the Missis- 
 sippi River. In his numerous analyses of the various limestones and dolo- 
 mites from this region, he generally obtained a small proportion of 
 soda ; which apparently exists in the rocks in a form insoluble hi water, 
 but readily soluble in acids. Thus in a very pure limestone of the Tren- 
 ton group from Wisconsin, containing only *75 of silica and alumina; he 
 obtained *27 of carbonate of soda ; and in a crystalline dolomite from the 
 Galena formation, holding 4*43 of silica, with but small traces of alumina 
 and oxyd of iron, there were found -38 of carbonates of soda and potash; 
 besides traces of chlorid of sodium, and of sulphate of lime. The alkalies 
 were in part set free by calcination ; after which, water removed -090 per 
 cent, of carbonate of potash, and -054 of carbonate of soda. Still another 
 of these dolomites, which contained 2-46 per cent, of insoluble matter, but 
 gave to acids not a trace of alumina, yielded '26 of carbonate of soda, 
 besides traces of chlorids. A limestone from the Niagara formation, 
 which contained 4*16 of insoluble matter, and 1-01 of soluble alumina 
 and oxyd of iron, gave '25 of carbonate of soda, and traces of chlorine and 
 sulphuric acid, without any potash ; while another pure dolomite of the 
 same series gave *35 of carbonate of soda, with a trace of potash. Many 
 other similar observations by Mr. Whitney show the presence of portions of 
 combined alkali in these limestones and dolomites, and may serve to throw 
 light on some facts in the history of mineral waters. 
 
 Kesting upon the Lower Silurian and Laurentian rocks, in the vicinity 
 of Montreal, there occur several small areas of dolomitic conglomerate ; 
 which appear to overlie, and to include, masses of pure limestone belong- 
 ing to the Lower Helderberg group. These conglomerates have been 
 noticed on page 355, and it only remains to describe some of their 
 chemical and mineralogical peculiarities. That of St. Helen's Island 
 contains pebbles of shale, chert, and sandstone, besides the included 
 masses of limestone ; the whole mingled with silicious sand, and ce- 
 mented by a ferriferous dolomite into a very tough greyish, yellow- 
 weathering rock. By the action of acids, there were taken up from 
 a portion of the matrix, forty-six per cent, of soluble matter, leaving a resi- 
 due of sand. The soluble part consisted of carbonate of lime 57-8, car- 
 bonate of magnesia 16'4, carbonate of iron 25' 8. A conglomerate with 
 a similar cement occurs at Ste. Anne, and another at Mont Calvaire, 
 which holds, besides pebbles of chert and sandstone, fragments of ortho- 
 clase, and of a violet-colored triclinic feldspar from the Laurentian rocks, 
 besides portions of black cleavable augite and brownish-black mica. In 
 rolled masses of a similar conglomerate, along the shores of Montreal 
 
CA?. XIX.] WESTERN PALEOZOIC ROCKS. 627 
 
 Island, large fragments of augite and mica are also seen imbedded, and, 
 more rarely, portions of olivine half an inch in diameter. At the White 
 Horse Rapids, is a similar conglomerate, but with a somewhat greenish 
 base ; holding, besides fragments of quartz, argillite, and mica, others of 
 a mineral like obsidian. The cement in all these is ferruginous and mag- 
 nesian ; but some beds of the conglomerate at Mont Calvaire, weather 
 white, and their cement is found to be a pure carbonate of lime. 
 
 Succeeding to the magnesian strata of the summit of the Onondaga Comiferoue 
 formation, is found in Western Canada, the Oriskany sandstone ; which, as 
 described on page 360, consists in many parts of chert or hornstone, and 
 forms the base of the Corniferous formation of the Devonian series. This 
 formation is a pure or non-magnesian limestone, which abounds in fossils, 
 and is remarkable for the abundant beds and masses of hornstone, to which 
 it owes its name, and for the liquid and the solid forms of bitumen which 
 it contains. These have been described in detail in the seventeenth 
 chapter, commencing at page 522. 
 
 To these limestones succeed, in Western Canada and New York, the Hamaton 
 shales, marls, and impure limestones of the Hamilton formation, terminated formatiou - 
 by the black pyroschists or shales of Bosanquet, described on page 387 ; 
 which are supposed to be the highest palaeozoic strata in Western Canada. 
 A specimen of the schist, by ignition in a covered crucile, lost 12-4 per 
 cent, of volatile and inflammable matter, and left a black residue, which 
 was not calcareous. Another portion, in fine powder, was digested for 
 several hours with heated benzole, which dissolved -8 per cent, of bitumi- 
 nous matter. The residue, carefully dried at 200 F., then gave off by 
 ignition in a close vessel, 11-3 of volatile matter, and by calcination lost 
 11-6 more ; equal to a total of 23-7 per cent, of combustible and volatile 
 substances. The calcined residue was grey in color. By distillation in 
 an iron retort, there were obtained from the shale, in two experiments, 3-7 
 and 4-2 per cent, of volatile liquid hydrocarbons ; besides a large quantity 
 of inflammable gas, and a portion of ammoniacal water. 
 
 These pyroschists, which closely resemble those of the Utica and Hud- 
 son River formations, are supposed to correspond to the Genesee slate of 
 New York. At the base of the Hamilton formation in that state, is still 
 another band of pyroschists, resting upon the limestones of the Corniferous 
 formation. It is worthy of notice, that the Upper Silurian and Devonian 
 rocks of this region present a lithological succession which resembles that 
 of the Lower and Middle Silurian. In the two series, the Potsdam for- 
 rnation may be compared with the sandstones at the base of the Medina, 
 while the dolomites of the Calciferous, and the lower part of the Chazy, blances * 
 with their accompanying minerals, are paralleled by those of the Clinton, 
 Niagara, Guelph, and Onondaga formations. The pure limestones of the 
 Trenton group, holding chert, silicified fossils, and petroleum, are repeated 
 
628 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 in the Cornlferous formation ; while the shales and pyroschists which follow 
 the latter, resemble lithologically those of the Utica and Hudson River 
 formations. The sandstones and conglomerates which succeed to the latter, 
 represent, on a smaller scale, those of the Upper Devonian. 
 
 Hernstone. The chert or hornstone which is found in the various formations of the 
 palaeozoic series, has been repeatedly referred to. It occurs in rounded or 
 lenticular masses, or in interstratified beds, generally in the limestones, 
 and seems to correspond to the flints of the chalk, or to the beds of buhr- 
 stone in other formations ; being evidently chemically deposited silica 
 (page 574). Chert abounds in the limestones of the Birdseye and Black 
 River division of the Trenton group, both near to Ottawa and in the vicinity 
 of Montreal, where it is sometimes found in interrupted beds, and in masses 
 of two or three inches in thickness. It is often nearly black in color, very 
 brittle, conchoidal in fracture, and with a somewhat resinous lustre. 
 
 Deposits of the nature of chert are not however confined to the lime- 
 stones. A jasper-like rock, two beds of which, respectively of six and eight 
 feet, occur interstratified with the arenaceous shales of the Hudson River 
 
 Jasper. formation, near Cape Rouge, is probably nothing more than a chert, enclos- 
 ing portions of argillaceous and ferruginous matter. This rock has the 
 hardness of quartz, and a density of 2- 64 -2- 66. It is perfectly homo- 
 geneous in texture, sharply conchoidal in fracture, translucent on the 
 edges, and varies in color from dark grass-green to blackish-green. It is 
 traversed by veins of calcareous spar. Analyses of specimens from the 
 
 l different beds at Cape Rouge gave as follows : 
 
 I. II. 
 
 Silica, 77-50 73-30 
 
 Alumina, 8 ' 50 J 16-30 
 
 Protoxyd of iron, 2 70 > 
 
 Lime, -73 traces. 
 
 Magnesia, 2-35 3-90 
 
 Potash, 1-66 undet. 
 
 Soda, 1-38 " 
 
 Volatile, 4-40 3-80 
 
 99-22 
 
 This rock is but slightly attacked by acids ; but on boiling a finely pul- 
 verized portion of I, for an hour, with a dilute solution of caustic soda, 
 there were dissolved 20-8 per cent, of silica, and only 1*2 per cent, of 
 alumina ; indicating thereby the existence of a large proportion of silica in 
 its soluble modification. 
 
 Chert abounds in nodules and layers in the dolomites of the Niagara 
 formation ; but it characterizes in an especial manner, the limestones of the 
 Corniferous formation. In these, the chert occurs both in nodular masses, 
 and in interstratified layers of from one to four inches, which in some sec- 
 
CHAP. XIX.] WESTERN PALEOZOIC ROCKS. 629 
 
 tions make up a large proportion of the rock. This chert is generally nearly 
 white, or greyish and yellowish in color ; opaque, dull, and somewhat earthy 
 in its aspect. The layers sometimes exhibit bands of different shades of 
 color, and the stratification of the limestone is seen to conform to the 
 nodules of chert. Specimens of this substance from the Corniferous for- 
 mation of central and western New York, have lately been examined by 
 Dr. M. C. White of New Haven, and found to be, like the flints of the 
 chalk formation, rich in microscopic organisms. These are principally 
 Desmidiese, embracing numerous forms of Xanthidia, besides a few Diato- 
 macege, and the spiculse of sponges. Similar forms have also since been de- 
 tected in the chert from the Birdseye and Black River limestones. (Amer. 
 Jour, of Science [2], xxxiii, 385.) Closely connected with the subject of 
 these deposits of silica is that of the silicification of organic remains, so f08sUs - 
 often referred to in preceding pages. Silicified fossils are met with in 
 some of the limestones of the Quebec group at Point LeVis ; but they are still 
 more abundant in certain limestone beds of the Trenton group at Lake 
 St. John, Montreal, Pakenham, Paquette's Rapids, and elsewhere. Fos- 
 sils similarly replaced occur also in the dolomites of the Medina and Nia- 
 gara formations in Western Canada ; but they are most abundant in the lime- 
 stones of the Corniferous formation ; some beds of which, as already describe^ 
 in page 366, are little more than a coherent mass of silicified fossils, with 
 a little intermingled carbonate of lime. This silicification is confined to 
 certain layers of the rock ; the fossils being often found unchanged in the 
 same bed, half an inch above or below a layer of silicified specimens ; and 
 even in these, the replacement is often partial, being confined to a portion of 
 the shell. This is still more remarkable in some of the fossil corals from 
 the Trenton group ; where certain portions of species of Receptaculites and 
 of Columnaria are replaced by silica, while other portions of the same 
 specimens are still calcareous. 
 
 The silica replacing the fossils is most frequently in the form of chalcedony, 
 chalcedony, which often presents a mammillary surface, arranged in 
 the form of several concentric circles around a bead-like and raised 
 portion, which may be a tenth of an inch or even more in diameter. 
 In other cases, the surface is nearly smooth, but still exhibits the peculiar 
 structure of chalcedony. The interior of such shells is sometimes partially 
 filled with crystalline quartz, as may be seen by dissolving the limestone by 
 an acid. In two instances where whorled shells had been fractured, the 
 fissure has been filled up by a tissue of chalcedonic quartz. In the case 
 of a silicified specimen of Stromatopora, it is found, on cutting it in two, and 
 subjecting it to the action of an acid, that the silica is confined to an exter- 
 nal crust, and to occasional grains or portions scattered through the cal- 
 careous body of the fossil. This observation, together with the fact above 
 mentioned, that the silicification is confined to certain planes, above and 
 
630 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 below which the fossils are unaltered, points to the conclusion that the 
 replacement preceded their envelopment in the rock, and was connected 
 with the presence of dissolved silica in the waters of the time. Mr. A. H. 
 Church has lately shown that when a solution of silica in about one hun- 
 dred parts of water, containing at the same time carbonic acid, is filtered 
 through fragments of coral, the whole of the silica is taken up by the 
 coral, while a large portion of carbonate of lime is dissolved. Similar 
 results were obtained with shells, but to a less extent, and in this way 
 Mr. Church endeavors to explain the silicification of calcareous fossils, 
 by the solution of the carbonate of lime, and its replacement by silica.* 
 
 Quartz. In some of the fossil shells of the Trenton group, the substance of the 
 
 shell alone is replaced ; in other specimens, the internal cavity, instead 
 of being filled with the sedimentary limestone, is wholly, or hi part, occu- 
 pied by crystallized quartz. The silicified fossils are often found in the 
 immediate vicinity of masses of chert ; and, in some instances, partially 
 imbedded in it. In those of the Corniferous limestone, of which the 
 corals are remarkable for their beauty and perfection, the chalcedony 
 often constitutes only the exterior of the fossil ; the inner part of which is 
 filled with crystalline quartz. 
 
 TWO classes The limestones of the fossiliferous formations of Canada may be divided 
 
 turnesT * nto two & reat classes, those which are made up of calcareous fossils, and 
 those which are apparently chemical precipitates, and have been formed 
 
 Organic, without the intervention of life. In describing the Chazy formation, and 
 the Trenton group, attention has been called to the fact that great portions 
 of these limestones are made up of comminuted organic remains ; and that 
 certain beds owe their peculiar granular texture to the crystalline structure 
 of the fragments of crinoids and cystideans (pages 125 and 138). Dr. 
 Dawson, in the Canadian Naturalist for 1859, vol. iv, p. 161, has described 
 and figured the results of a microscopical examination of a series of sections 
 of these fossiliferous limestones, from the island of Montreal. According 
 to him, these, when examined with a magnifying power of from ten to 
 twenty diameters, are seen to consist of minute fragments of corals, 
 crinoids, and cystideans, with very small shells, cemented by a transparent 
 crystalline calcareous spar. This, in other cases, is mingled with grains 
 of sand, or portions of clay, and colored by a carbonaceous matter. One 
 variety of the grey limestone from the Trenton group, is chiefly made up 
 of fragments of brachiopodous shells ; and, in another bed, according to 
 Dr. Dawson, the fragments of the shells and crinoids are rounded, as if by 
 attrition. He also examined two compact limestones from this series, 
 in which fragments of fossils are imbedded in a fine grained homogeneous 
 and earthy calcareous base. 
 
 * Proc. Chemical Society of London, Feb. 6, 1862 ; Chem. News, vol. v, p. 95 j also, 
 L. E. and D. Phil. Mag. (4), xxiii, 95. 
 
CHAP. XIX.] WESTERN PALEOZOIC ROCKS. 631 
 
 The microscopic examination of a more extended series of specimens of inorganic 
 the palaeozoic limestones of Canada,* while confirming these results, has Iime8tone9 - 
 shown that there are many beds, which, even under powers of from forty 
 to eighty diameters, appear to be made up of a fine grained, confusedly 
 crystalline paste of carbonate of lime, often without any traces of organic 
 structure. Examples of this are seen from the Quebec group, in the 
 limestones of Acton, of Trois Pistoles, and of Point lie* vis ; the latter 
 being the travertine already described on page 612, and containing, in one 
 part, a few minute organisms. These rocks closely resemble, under the 
 microscope, a fine grained and pure dolomite, without fossils, from the 
 Calciferous formation. The compact brown limestone which holds the 
 silicified fossils at Paquette's Rapids, has a similar structure to these, but 
 is rendered opaque, in parts, by an admixture of clayey matter ; while 
 the lithographic stone of Marmora, which, like the last, is from the 
 Trenton group, is still more finely crystalline, and homogeneous. The 
 limestones from the Corniferous formation in Western Canada, exhibit 
 differences similar to those of the Trenton group. A specimen from 
 Walpole is, like some of the Montreal limestones, an aggregation of minute 
 organic remains ; others, from Port Colborne and the Saugeen, contain 
 numerous fossils in a fine grained base ; while others still, from Dumfries 
 and St. Mary's, are finely crystalline, and can hardly be distinguished 
 from that of Point LeVis. That from St. Mary's contained a few minute 
 spiculse, apparently organic. Specimens from the Upper Helderberg on 
 the Me*tis River, and from the Lower Helderberg of St. Helen's Island, 
 were, like those of Montreal, eminently fossiliferous. The limestone from 
 near the Chatte River (page 264), which has an oolitic structure Ooute. 
 apparent to the naked eye, is seen, under the microscope, to consist of 
 small globes, concentric in structure, imbedded in a base of broadly crys- 
 talline spar. A similar matrix, in other cases, encloses grains of sand. It is 
 probable that the pure crystalline marbles of Vermont, and of many other 
 regions, are, like those just described, chemical precipitates from solution; 
 which, in some cases, have been, like modern travertines and tufas, 
 deposits from calcareous springs, but have, in most cases, been formed 
 from sea-water by the reaction pointed out on page 575. 
 
 The columnar markings which occur in the limestone of the Trenton columnar 
 group at Marmora have been noticed on page 182, and those in the Niagara markin 8 8 - 
 formation on page 323. They are also found in the dolomites of the 
 Onondaga and Guelph formations ; and in the pure limestones and cherts 
 of the Corniferous, as described on page 346. These peculiar forms 
 were, by Mr. Vanuxem, called epsomites, being ascribed by him to the 
 crystallization of sulphate of magnesia, or Epsom salt, in the soft sediments 
 
 * These specimens were prepared by Edward Murphy, Esq;, of Montreal, who has 
 kindly presented a series of them to the Museum of the Geological Survey. 
 
632 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 crystallites, at the time the rocks were deposited ; the salt having been subsequently 
 removed by solution, leaving its mould in the sediment to be filled by the 
 succeeding layer. The crystals may however have been of the sulphate 
 of soda, rather than of the magnesian salt. 
 
 434, 436.- CBYSTALLITB8. 
 
 434. Column from the limestone of Kingston. 
 
 435. Column from the dolomite of the Guelph formation. Both of natural size. 
 
 Kingston. These curious forms appear to have been first described and figured by 
 Capt. R. H. Bonnycastle, R. E., in an essay on the rocks of the vicinity 
 of Kingston, published in 1831, in the American Journal of Science [1] , xx, 
 p. 74. They there occur in the limestone of the Trenton group, pene- 
 trating sometimes five or six inches, but, more commonly, only from half 
 an inch to an inch in depth ; and are described as consisting of a series 
 of delicate columns or flutings, the minute striae of which are always parallel 
 to one other, although the columns are sometimes curved, or inclined at 
 various angles to the bed of limestone. The columns are sometimes 
 deeply channelled, and at other times have the form of irregular prisms. 
 Their lower extremities are always rounded, as if by a folding of the ends 
 into a cup, and the layer of shale which covers their surface is there thick- 
 ened y while elsewhere it is but a thin brown shining film, which adheres 
 either to the column or to its matrix. Around the upper part of the 
 columns shorter ones are often grouped in a way which may readily be 
 seen in the accompanying figure, 434, copied from one given in the paper 
 above cited ; the artist having, at the same time, before him other speci- 
 mens from the same locality. Capt. Bonnycastle, who also figured at the 
 same time a similar specimen from Niagara Falls, does not attempt to 
 decide as to the nature of these columns ; but he showed them to consist 
 of limestone, with a thin coating of shale, which he supposed to be the 
 result of infiltration. The explanation of Mr. Vanuxem, that they are the 
 
CHAP. XIX.] 
 
 WESTERN PALAEOZOIC ROCKS. 
 
 633 
 
 moulds of crystals, seems, in the present state of our knowledge, the most 
 probable one, and supposes a great degree of concentration in the sea- 
 water during the deposition of these limestone and dolomite beds. 
 
 436. CRYSTALLITES. 
 
 436. Specimen from limestone of the Corniferous formation near Port Doyer. 
 
 A specimen from the dolomite of the Guelph formation at Rockwood is 
 represented in figure 435. It shows the short columns around the top, 
 and also the slight curvature. The specimens from the Corniferous 
 
 437. CRYSTALLITES. 
 
 437. Specimen from the same locality, in which the crystallites penetrate 
 a mass of chert imbedded in the limestone. 
 
 formation near Port Dover are smaller. The limestone here encloses 
 small beds and lenticular masses of horns tone, in which latter the columns 
 are sometimes impressed. Figure 436 represents a mass of limestone 
 
 .CRYSTALLITES. 
 
 438. Vertical section of a similar specimen from the above locality, the 
 dotted portion showing the upper and broken layer of the chert. 
 
 from this locality, enclosing prisms of various lengths, two of them 
 descending obliquely. Figure 437 represents the columns in a mass of chert 
 imbedded in limestone, the layers of which are seen to conform to the 
 
634 GEOLOGY OP CANADA. [CHAP. XIX. 
 
 chert. Figure 438 is from a vertical section of another specimen, show- 
 ing the displacement of a thin layer of chert, which is indicated by a 
 dotted surface, and, lying above the principal mass of this substance, 
 appears as if it had been broken by a downward pressure. 
 
 Local meta- The local alteration in the limestone in proximity to the igneous rocks 
 morphism. Q f M OUI ^ R yal has already been described on page 582. On Montar- 
 Montarvffle. ville, which consists of a mass of intrusive dolerite breaking up through the 
 shales of the Hudson River group, are seen some interesting results of local 
 metamorphism. Not far from the manor-house is a quarry, where a con- 
 siderable exposure of altered strata is met with. The rock is here, for 
 the most part, fine grained, compact, and sonorous, somewhat schistose, 
 and holds a few fossil shells. A bed of impure earthy limestone, con- 
 taining grains of pyrites, is also interstratified. Not far from this, similar 
 strata are again exposed. Some portions are very fine grained, reddish- 
 brown, and having an earthy sub-conchoidal fracture, with occasional cleav- 
 age joints. The hardness of this rock is not great, and it is apparently a 
 kind of argillite. Between two beds of this, is one of a coarse grained 
 rock, greenish-grey in color, and mottled with a lighter hue. It appears 
 to be feldspathic in composition, and is penetrated in various directions by 
 numerous slender prisms of black cleavable pyroxene, sometimes half an 
 inch in length. The layers of sedimentation are distinctly marked in this 
 bed, as well as in the finer grained strata which enclosed it ; and the whok 
 affords an interesting example of the different effects of the same agency 
 upon beds of unlike composition. Still larger prisms of pyroxene were 
 seen in a loose fragment of a similar rock found near by. Large detached 
 blocks of a highly crystalline rock are also met with on this mountain ; com- 
 posed of blackish-green cleavable hornblende, mingled with small rounded 
 masses of a compact bluish-grey mineral, weathering reddish-brown. This 
 was found by analysis to consist of carbonates of magnesia, lime, and iron ; 
 the first, apparently predominating. It gave besides, abundant traces of 
 nickel ; and the qualitative examination of the hornblende showed the pres- 
 ence of oxyd of chrome. Two varieties of a rock very similar to this in 
 composition and aspect, are said to occur on Rougemont, which is an 
 intrusive mountain of dolerite, like Montarville, and rises through the same 
 formation. One of these is either concretionary or conglomerate in its 
 structure. The paste is a dark greenish crystalline hornblende, which 
 retains its color on the weathered surfaces, while the nodules of buff-colored 
 dolomite become reddish-yellow. Another variety is made up of thin 
 layers of a white crystalline reddish-weathering dolomite, with others of a 
 compact greenish-grey mineral ; and others still of blackish-green crystal- 
 line hornblende, which, like the other bands, vary from one tenth to one 
 fourth of an inch in thickness, and are sometimes interrupted. Occa- 
 sionally, the cleavages of the hornblende, which are nearly perpendicular 
 
CHAP. XIX.] WESTERN PALAEOZOIC ROCKS. 635 
 
 to the beds, are seen cutting through thin layers of the dolomite. A 
 portion of the rock, free from hornblende, was reduced to powder, and 
 effervesced with warm dilute nitric acid ; which removed carbonates of lime, 
 magnesia, and iron. The analysis of the soluble portion yielded carbonate 
 of lime 38-9, carbonate of magnesia 31-2, carbonate of iron 29-9 = 100*0. 
 The insoluble residue gave silica 65*40, alumina 10*10, lime *56, mag- 
 nesia 2-05, protoxyd of iron 4-80, titanic acid 7*30, volatile 2-20, loss, 
 probably alkalies, 7-59 = 100-00. Minute grains of pyrites in the rock 
 gave traces both of copper and nickel. 
 
 In the admixture of ferruginous dolomite, and in the presence of nickel, 
 chrome, and titanium, the stratified crystalline hornblendic rocks of Mon- 
 tarville and Rougemont resemble the sedimentary deposits of the eastern 
 district ; but as the rocks just described are not yet known to occur in 
 place on these mountains, farther examination will be required to arrive 
 at a satisfactory conclusion as to their origin. 
 
 The shales of the Utica formation in the vicinity of a trap dyke at Point St. 
 Charles (page 208) , and near to a mass of intrusive trachyte on a little island 
 above St. Helens, occasionally exhibit small crystals of pyroxene, similar 
 to those of Montarville. In other specimens, crystals having the char- 
 acters of hornblende have been seen penetrating the altered shales. 
 
 In this connection, may be mentioned a remarkable example of local Syracuse, 
 metamorphism, which occurs in the Onondaga formation, at Syracuse in 
 New York, and is described by Vanuxem (Geology of New York, vol. 
 iii, p. 109). The strata between two layers of the vesicular dolomite here 
 consist for the greater part of serpentine, which is dark or blackish-green 
 in color, sometimes blood-red, weathering yellowish, and often in a friable 
 and apparently decomposed state. Some portions of the rock are de- 
 scribed as containing well-characterized black and white mica, and horn- 
 blende ; in small accretions of granite and syenite, having all the ordinary 
 characters of these rocks. The adjacent slaty portions of the formation 
 are also hardened and crystalline. A portion of the ophiolite from this serpentine, 
 locality was found to be an aggregate of grains and rounded masses of 
 serpentine, with others of a fine grained pure limestone, imbedded in a 
 greenish-grey calcareous base. The colors of the serpentine vary from 
 blackish-green to greenish-white. It is often translucent, and takes a high 
 polish. Small portions of bronze-colored diallage are occasionally dis- 
 seminated in the mass. Acetic acid readily attacks this ophiolite, when in 
 powder ; and a proximate analysis thus made, gave carbonate of lime 34*43, 
 carbonate of magnesia 2*73, oxyd of iron and alumina *34, insoluble 62*50. 
 The analysis of the residue of serpentine gave silica 40*67, magnesia 32*61, 
 protoxyd of iron 8*12, alumina 5-13, water 12*77 = 99*30. No traces 
 of nickel or of chrome were detected. The metamorphism is here in an 
 undisturbed region, removed from any known intrusive rocks, and entirely 
 
636 GEOLOGY OF CANADA. [CHAP. XIX. 
 
 local. ' This association of serpentine, diallage, and hornblende, with 
 gypsum and dolomite, in a saliferous formation, recalls the localities 
 in the Pyrenees where hornblendic rocks are accompanied by gypsum, 
 rock-salt, dolomite^ and hot springs, in the Tertiary formation. At Syra- 
 cuse, as remarked by Vanuxem, there is no evidence of igneous action, 
 and hot springs might readily produce the local metamorphism here 
 observed, in a manner similar to that described by Daubree (page 584). 
 Metaiiifer- The veins of segregation, or of infiltration, known to exist among the rocks 
 us veins. O f ^ wes t em palaeozoic district, are few in number. Among them must 
 be included those which hold galena, sometimes with blende and copper 
 pyrites, in a gangue of calcite, or heavy-spar, and are generally found tra- 
 versing the Laurentian limestones. A vein of this kind in the township 
 of Ramsay, however, intersects the Calciferous formation ; and, with the 
 others which resemble it, it may therefore belong to a more recent period. 
 Small veins of calcite, holding fluor-spar and galena, and traversing the 
 limestones of the Trenton group at Bay St. Paul, have been described in 
 page 161. The numerous veins of trappean rocks which intersect the 
 strata of this region will be noticed in the succeeding chapter. 
 
 SOILS AND CLAYS. 
 
 A series of analyses of the soils of Canada was made a few years since, 
 
 in accordance with the notion then generally received, that there was such 
 
 a direct relation between the chemical composition of a soil and its fertility, 
 
 that its agricultural capabilities could be determined from the results of 
 
 a minute chemical analysis. The more recent and profound investigations 
 
 of the first chemists and agriculturists of our time, have however shown 
 
 that this idea is, to a great extent, fallacious. The extreme difficulty of 
 
 obtaining a specimen of soil which shall represent the mean composition of 
 
 a field, has been demonstrated by varied and careful trials, in Germany 
 
 and elsewhere ; and it has besides been repeatedly observed that many 
 
 sterile and apparently exhausted soils contain in greater abundance the 
 
 elements supposed to be necessary to vegetation, than other soils possessing 
 
 soiianaiy- a high degree of fertility. The complete chemical and mechanical 
 
 8es - analysis of a soil can, at best, indicate but a few of the many conditions 
 
 necessary to the healthy growth of plants ; so that its use in guiding the 
 
 farmer is very subordinate ; and when its uncertainty and its inadequateness 
 
 to the estimation of the minute quantities which affect vegetable growth, 
 
 are considered, its value, as has been well said by an eminent authority, is 
 
 Boussin- insignificant.* Boussingault, in his late work on agricultural chemistry, gives 
 
 gauit'sopin- the following, as the summing up of his protracted experience and study. 
 
 ion. . . 
 
 * Prof. S. W. Johnson on Soil Analyses. Amer. Jour, of Science (2), xxxii, page 249. 
 
CHAP. XIX.] SOILS AND CLAYS. 637 
 
 " At an epoch not now remote, it was believed that a strict connection 
 existed between the composition and the quality of arable soil. Numerous 
 analyses, however, soon modified this opinion, as too positive ; and the saga- 
 cious Schiibler even sought to prove, in an investigation which has become 
 classic, that the fertility of a soil depends more upon its physical proper- 
 ties, its state of aggregation, its power of absorption, etc., than upon its 
 chemical constitution. 
 
 " The physical properties, in my opinion, do not enable us, any more than 
 the chemical composition, to pronounce upon the degree of fertility of the 
 soil. To decide this point with some measure of certainty, it is indispen- 
 sable to have recourse to direct observation. It is necessary to cultivate 
 a plant in the soil, and ascertain with what vigor it is there developed. 
 The analysis of the plant afterwards intervenes usefully, to indicate the 
 kind and the quantity of the elements that have been assimilated."* 
 
 Inasmuch, however, as some of the results of the investigations into the 
 composition of the soils of Canada are not without a certain interest in a 
 chemical and geological point of view, whatever may be their value to the 
 agriculturist, they are here subjoined in a table, on page 640. 
 
 The mechanical analysis of the soils was effected by washing a portion, Modes of 
 to separate the clay from the sand. From the latter, the coarser material, analy818 ' 
 when present, was removed by sifting. The soils being previously dried at 
 the ordinary temperature, the amount of water was determined by 
 exposing them to a temperature above 300 F., till they no longer lost 
 weight. In the case of clays, which tenaciously retain moisture, the heat 
 was raised as high as was possible without carbonizing the organic substances 
 which might be present. The amount of organic and other volatile 
 matters was then determined by heating to redness in an open vessel, and 
 burning off the carbon, if necessary. The substances removed by a pro- 
 longed digestion with distilled water, at the ordinary temperature, were in 
 some instances determined ; but in most cases the analysis was confined to 
 the soluble matters removed from the soil by digesting twenty grams of 
 it, for an hour, at a boiling heat, with hydrochloric acid diluted with three 
 or four parts of water. The solution thus obtained, was divided into three 
 parts, in which the soluble silica, the .phosphoric and sulphuric acids, and 
 the" bases, were determined by the usual methods. The phosphoric acid 
 was separated by precipitating it from the solution, in combination with the 
 alumina and peroxyd of iron, and fusing the dried precipitate with a mix- 
 ture of carbonate of soda and silica ; the phosphate from the solution of 
 the fused mass being subsequently determined in the form of an ammonio- 
 magnesian salt. 
 
 * Boussingault, Agronomic, Chimie Agricole et Physiologic, vol. i, p. 283. 
 
638 GEOLOGY OF CANADA. [OflAP. XIX, 
 
 I and II are soils from the domain of Mr. Kierzkowski, in the seigniory 
 of St. Charles. I is a black mould taken at a depth of eight inches from 
 the surface, and consisting of sand 49' 2, clay 23'4, organic matter 20*8, 
 water 6*6 = 100-00. One hundred parts of this soil gave to distilled 
 water *786 parts of soluble matters, chiefly organic ; which by ignition left 
 104 of an alkaline residue, containing lime, magnesia, and alkalies. The 
 watery solution gave *008 of chlorine, with a small portion of nitrates, and 
 a trace of sulphates. II contained but a trace of vegetable matter, and 
 consisted of sand 56*0, pebbles of gneiss and quartz 8-0, clay 27-8, water 
 8-2 == 100-0. One hundred parts of this soil yielded to water -0506 
 parts of solid matter, which by ignition were reduced to "0347, and which 
 contained, chlorine -0134, sulphuric acid -00046, lime -0085, besides mag- 
 nesia and alkalies, but no nitrates. 
 
 st. miaire. Ill and IV are soils from the farm of Major Campbell at St. Hilaire. 
 Ill is from a tilled field, taken at the depth of six inches, and contained 
 but very little organic matter. It gave sand 3'0, clay, 89-7, water, etc., 
 7-3 = 100-0. IV was a portion of the underlying clay from a depth of 
 thirty inches. It contained only traces of sand and organic matter, and 
 lost by ignition 15*5 per cent. 
 
 st.Domi- V and VI are from St. Dominique. V is the blue clay from beneath a 
 mque * large peat bog, and consisted of silicious sand, with a little feldspar and 
 mica, 38.0, clay, with traces of organic matter, 59*0, water 3-0 = 100-00. 
 VI is from near the surface of a long-tilled field near the bog, and was 
 regarded as an exhausted soil. It consisted of sand 46-00, clay 42-2, 
 organic matter 9-5, water 2-3 = 100-0. 
 
 st. Hya- VII and VIII are from about two miles south of St. Hyacinth. VII 
 cinth. wag sa ^ to be from a field which had been tilled sixty or seventy years 
 without manure, and consisted of sand 34-0, clay 62-2, organic matter 
 1-5, water 2-3 = 100-0. VIII was said to be the sub-soil of the same 
 field, from a depth of about two feet, and differs widely in its mechanical 
 constitution from the surface soil. It contained neither sand nor organic 
 matter, and lost only four per cent, by gentle ignition. It held portions 
 of lime and magnesia as carbonates. 
 
 chambiy. IX, X, and XI are from Chambly. IX is a reddish clay, taken at a 
 depth of sixteen inches, from a well-tilled field near the village. It con- 
 tained but a small amount of sand, and traces of organic matter, and gave 
 by ignition 5*5 per cent, of volatile matter. X is an apparently similar 
 soil, from an adjoining field ; which had been cultivated with wheat for many 
 years, and was supposed to be exhausted. It consisted of silicious sand, 
 with a little feldspar, 9-0, clay 79-2, vegetable matter 6-8, water 5-00 = 
 100*0. XII is from an untilled field, on a ridge of light, gravelly soil 
 near to the church. An average portion of it contained twenty per cent. 
 of pebbles, and twelve of coarse gravel, derived from Laurentian rocks. 
 
CHAP. XIX.J SOILS AND CLAYS. 639 
 
 The portion which passed through a sieve consisted of gravel 75-0, clay 
 13'7, organic matter 6-1, water 5-2 = 100-0. 
 
 XII is from Montreal, and is the soil from a long-tilled field on the farm Montreal, 
 of James Logan, Esq. It is a clay, containing 13*5 j>er cent, of silicious 
 
 sand, mixed with a little magnetic oxyd of iron. Its ultimate analysis 
 gave silica, by difference, 65-53, alumina 13-15, peroxyd of iron 8-50, 
 lime 1-73, magnesia 1-14, potash 1-76, soda 2-35, phosphoric acid -54, 
 water and organic matter 5-30 = 100-00. 
 
 XIII is from Ste. Anne de la Pocatire, and is a clay almost entirely ste.Anne. 
 free from sand, taken from a meadow at the foot of the hill below the 
 college. The preceding soils, with the exception of XI, from Chambly, 
 belong to the quaternary clays of the St. Lawrence valley. 
 
 XIV and XV are soils derived from the disintegration of the red shales St. Jean, 
 of the Sillery formation. The first is from St. Jean, Port Joli, and was 
 collected at a depth of four inches, in a field covered with short turf, where 
 
 the upturned edges of unbroken slates were within a few inches of the surface. 
 The soil was scarcely coherent, and was separated by sifting from the 
 fragments of shale. It was of a deep red-brown color, and contained 
 scarcely any organic matter, except a few fibrous roots. XV is from St. at. Thomas. 
 Thomas, and was taken at a depth of six inches, in a pasture where the 
 shales were about a foot from the surface. The disintegration was here 
 more complete than in the last, and the soil was dark red, and strongly 
 coherent. Both of these contained a little oxyd of manganese. 
 
 XVI is from the twenty-eighth lot of the third range of Bastard, and Bastard, 
 is from an untilled field, where about a foot of very fertile soil rests upon 
 
 the horizontal strata of the Calciferous formation. It was taken from a 
 depth of six inches, and was a sandy loam, with very little organic matter. 
 
 XVII and XVIII are soils from Strathmore, near Brantford. The first Brantford. 
 is from the plains known as the oak openings ; and was taken from a depth 
 
 of eight inches, beneath the sod of an untilled and recently cleared field. 
 A large portion of this soil is finely divided, but cannot be called a clay. 
 It consisted of sand 47*4, finer material 49-2, organic matter 2-4, water 
 1-0 = 100-0. XVIII is the rich black loam from the alluvial flats of 
 the Grand River, and was taken under similar circumstances to the last. 
 It contained considerable portions of lime and magnesia as carbonates, and 
 consisted of sand 72*0, finer material 20-0, organic matter 6-5, water 
 1-5 = 100-0. 
 
 XIX and XX are from the township of Raleigh. The first is from the 
 rich alluvial flats of the Thames, which are covered with from six to ten 
 inches of black loam, resting upon a yellowish clay. This, near to the 
 village of Chatham, was observed to have a thickness of about four feet, 
 and to be underlaid by a regularly stratified sandy loam ; while beneath, 
 at a depth of ten feet from the surface, was a tenacious blue clay. The 
 
640 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XIX. 
 
 
 
 
 T-H 
 
 ^Ot-OO O COi-HO 
 rrj CO "tf 00 OO <M CO 00 
 O CO 00 CO i-HOO 
 
 O 
 
 oooiooomo 
 ^osoocomTticqooo 
 
 COOlOOOO<MCOi-HCO 
 
 ^2 
 
 
 
 ^ 
 
 
 THr-^rH^^ 
 
 1 
 
 
 05 
 
 OOrHOCOOOOOO 
 COCO.C^COOCO^5orH 
 
 OS 
 I-H 
 
 OOOO O OOOO 
 
 cq co o co cq o o 05 
 cocomo oo -^r-icq 
 
 0$ 
 
 i 
 
 
 
 co oo cq 
 
 
 Cq O rH i-H 
 
 CD 
 
 A 
 
 
 oo' 
 
 ooo.t-coocqcoo 
 cqoococot-cocqocq 
 
 oo' 
 
 sssiilliS 
 
 5 
 
 
 
 O CO cq cq 
 
 
 cq 10 co 
 
 02 
 
 
 ^ 
 
 llSISlsss 
 
 JtJ 
 
 ooocomooooo 
 
 OOCO-^rHOCOOO 
 
 l 
 
 
 
 OqiO r- 
 
 
 cq cq 
 
 1 
 
 
 CO* 
 
 SiliSlIIS 
 
 CO 
 l-H 
 
 U3 
 
 Is 
 
 cq^ 
 
 
 
 CO ^ r-l 
 
 
 CO ** 
 
 - 1 rrj 
 
 
 1C* 
 
 lleSslssI 
 
 1 1 
 
 1 IllSlsi 
 
 *a 1 
 
 
 
 Tf CO rH 3 
 
 
 1C ^ 
 
 J3 W 
 
 CQ 
 
 _q 
 
 t i 
 
 ^ 
 
 1I1IS13IS 
 
 r- 1 
 
 s sssslss 
 
 ^ rH 
 
 rH ~ 
 
 o~ ^ 
 
 OQ 
 
 
 M0 - 
 
 
 ^ 
 
 ^ ^ 
 
 fe 
 O 
 
 CO* 
 
 lllllalls 
 
 CO* 
 
 o coocooooooco 
 <<* coio-*cocq-HCO 
 
 i" 1 
 
 s w 
 
 CQ 
 
 
 cq t- i i 
 
 i-H 
 
 
 o 
 
 'S r 
 
 03 rH' 
 
 K 
 OQ 
 !* 
 !_q 
 
 C5 
 
 OOOCOCOOIO^O 
 
 CNI 
 
 o ocoooJ?-oo^<rq 
 r-i oo. co I-H 03 cq o oq 
 
 Si" 
 
 <1 
 
 
 pH CO rH 
 
 
 00 
 
 orT g 
 
 
 
 1 
 
 J 
 
 ||||lg3| 
 
 i-H 
 
 ilsllSlsi 
 
 -02 
 09 
 
 & IO 
 
 
 
 ^ CO rH 
 
 
 cq 10 
 
 .H 1 
 
 P 
 
 
 1 
 
 .2 
 
 
 
 
 
 l 
 
 . ** 
 * j^ 
 oo o 
 
 ^ p* 
 
 : :f 
 
 
 3 
 5 
 
 1 
 
 I 
 
 Q *3 " "* 
 
 | 
 
 
 0} 
 
 1 
 
 t 
 
 o 
 o 
 
 rH 
 
 ** *+ 
 
 ^ .f_:|| 
 
 ^ PM S S Pv M ^ 02 02 
 
 l 
 
 W rf 
 
 02 
 CO** 
 
 i" 
 
 1 
 
 O 
 
 02 
 cq** 
 
CHAP. XIX.] SOILS AND CLAYS. (541 
 
 soil is one of great richness, and supports a growth of oak, maple, black 
 walnut, and whitewood. The specimen was taken from the seventh lot of 
 the first range, at a depth of six inches, from a recently cleared field, and 
 contained but a trace of white silicious sand. It consisted of clay 83-4, 
 organic matter 12-0, water 4*6 = 100*0. XX is from the seventeenth 
 lot of the first range of the same township, and is the mould from a 
 recently drained portion of the prairie land, which extends from near 
 Chatham to Lake St. Clair. The mould is here a foot deep, and the 
 specimen was taken at a depth of six inches. It contains no sand, but 
 a small amount of carbonates ; and consists of clay 80*9, organic matter 
 13-6, water 5-5 = 100*0. 
 
 Some of the quaternary clays of the St. Lawrence valley are calcareous, ciays. 
 and effervesce freely with acids. A reddish-fawn colored impalpable clay, 
 from the banks of the Riviere a la Graisse, in Rigaud, was attacked with 
 dilute hydrochloric acid ; which dissolved alumina and peroxyd of iron 
 12*95, lime 3-97, and magnesia 1-92. The ultimate analysis of this clay 
 gave silica, by difference, 52*95, alumina and peroxyd of iron 27*30, lime 
 5*32, magnesia 2*62, potash 1*26, soda 2*06, phosphoric acid *74, carbonic 
 acid 3*25, water 4*50 = 100*00. The carbonic acid, which is the mean 
 of two closely agreeing determinations, is very little more than is required 
 to form a carbonate with the lime which is soluble in dilute acids ; so 
 that the remaining portions of lime, and the magnesia, probably exist as 
 silicates. A fine blue clay, which is interstratified with the above, gave to 
 hydrochloric acid, lime 2*74, magnesia 2*86 per cent. ; while the ultimate 
 analysis gave lime 8*12 per cent., of which a large portion therefore exists 
 as a silicate. A portion of clay was taken, from a depth of eight inches, in Niagara, 
 an untilled field in the township of Niagara ; resting upon the escarpment 
 here formed by the dolomites of the Niagara formation. It contained 
 three or four per cent, of silicious sand, besides some calcareous pebbles. 
 After the separation of these, an analysis by hydrochloric acid gave as 
 follows : insoluble 58*00, carbonate of lime 15*30, carbonate of mag- 
 nesia 7*68, alumina and peroxyd of iron, with traces of manganese, 13*50, 
 alkaies *51, phosphoric acid *09, water 4*70 = 99*78 ; besides traces of 
 sulphate of lime. 
 
 A fine marly clay, which occurs at a depth of from five to ten feet from London, 
 the surface, in and about London, and is seen in the banks of the Thames, 
 near the town, was found to be mixed with limestone pebbles, and to give 
 out a bituminous odor when treated with hydrochloric acid ; by which pro- 
 cess it yielded, insoluble 57*00, carbonate of lime 29*40, carbonate of 
 magnesia 6.91, phosphate of lime -39, alumina and oxyd of iron 4*40, 
 water and loss 1*90 = 100*00. It contained no trace of sulphate of lime. 
 Similar calcareous clays have been examined from Delaware, Mosa, and 
 Port Stanley. The above analyses, although imperfect, are not without 
 
 QQ 
 
642 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XIX. 
 
 Peate. 
 
 interest, as indicating the composition of some of the more recent sedi- 
 mentary deposits of this region. These are probably derived in part 
 from the ruins of calcareous palaeozoic rocks. 
 
 The great deposits of peat which abound in the province, will be considered 
 in another chapter, with reference to their economical applications. The 
 composition of some specimens, and the analysis of the ash of one of them, 
 Sherrington. may, however, be given in this connection. Of two specimens from a 
 peat bog in Sherrington, one was fine grained, compact, and so heavy as 
 to sink in water. It gave by incineration only 3-53 per cent, of a light 
 greyish ash, of which the greater part was soluble in hydrochloric acid, 
 and consisted of carbonate of lime, with traces of magnesia and iron, a 
 considerable portion of sulphates, and a little phosphate. A specimen of 
 the lighter peat, from the upper part of the bog, gave 4-66 per cent, of ash. 
 
 The peat from the bog of St. Dominique was examined by igniting it in 
 close vessels, and determining the loss of vegetable matter. A solid 
 coke was in this way obtained, which left by ignition a light reddish ash. 
 Of two well-dried specimens, a compact .one gave fixed carbon 29-30, 
 volatile 63-43, ash 7-27 = 100-00 ; and a more porous one, fixed carbon 
 29-57, volatile 63-68, ash 6-75 = 100-00. The ash from this peat yielded 
 to water a large amount of sulphate of lime, besides portions of alkalies 
 as chlorids and sulphates. The lime and magnesia in the ash were in 
 great part as carbonates, but partly, also, in a free state. One hundred 
 parts gave by analysis, lime 47-040, magnesia 3-150, potash -330, soda 
 254, alumina 2-440, peroxyd of iron 4-680, oxyd of manganese -040, 
 sulphuric acid 9-175, carbonic acid 23-060, phosphoric acid -932, chlorine 
 247, combined silica 4-920, sand 4-040. These elements being combined 
 in the usual manner, give for 100 parts of the ash, carbonate of lime 
 52-410, sulphate of lime 15-085, phosphate of lime 2-019, chlorid of 
 sodium -412, sulphate of soda -'076, sulphate of potash -605, besides 
 10-431 of uncombined lime, and 3-750 of magnesia, from the decomposition 
 of the carbonates ; these, with the silica, alumina, and metallic oxyds, 
 making up 100-308. The various shell marls which are often associated 
 with the peat deposits in Canada, have, in all cases where they have been 
 examined, proved to be nearly pure carbonate of lime. The chemical 
 history of the ochres and bog iron ores of the superficial deposits of the 
 country, has already been given in the seventeenth chapter. 
 
 St. Domi- 
 nique. 
 
 Peat ashes. 
 
CHAP. XX.l GEOLOGY OF CANADA. 643 
 
 CHAPTER XX. 
 
 ERtJPTIYE HOCKS. 
 
 CONSIDERATIONS; ORIGIN; STRUCTURE; COMPOSITION; CLASSIFICATION; DEFINITIONS! 
 GRANITE, ORTHOPHYRE, TRACHYTE, DtORlTE, DIABASE, DOLERITE. INTRUSIVE ROCKS 
 OV THE IiAURENTIAN SERIES; DOLERITE; SYENITE ; t ORTHOPHYRE. OS 1 THE PALAEOZOIC 
 SERIES. TRACHYTE; BROME; SHEFFORD; CHAMBLY; MONTREAL; LACHINE; YAMASKA. 
 PHONOLITE. DIORITE; YAMASKA; MOUNT JOHNSON-; BELCEIL; RIGAUD> DOLERITE AND 
 PYROXENITE; MONTARVILLE; ROUGEMONT; MOUNT ROYAL. GRANITES. 
 
 Before commencing an account of such of the intrusive rocks of Canada 
 as have been examined, it is proposed to give a few definitions, and to explain 
 the nomenclature which will be followed in their description. This is the more 
 necessary, as much of the obscurity to be found among writers on lithology 
 arises from the great number of names, often nearly synonymous, and from 
 the vague manner in which these are applied. Many of those rocks which Theoretical 
 have been hitherto* described as eruptive, are sediments, which, although Yiew8< 
 altered, and retaining but little evidence of their former condition, are still 
 in the beds in which they were originally deposited. At the time of their 
 chemical metamorphism, they were impregnated with water, and, by the 
 joint action of this and of an elevated temperature, were evidently re- 
 duced to a more or less plastic mass. This in some cases is found to have 
 been displaced, and, having forced its way among disrupted strata, to have 
 assumed the form of an intrusive rock ; which becoming consolidated under 
 a sufficient pressure, retains the same mineral characters as in its parent 
 bed. This view may probably be extended to explain the origin of every 
 eruptive rock ; whose equivalent is thus to be looked for among crystalline 
 strata. It is only those rocks which, like lavas, have become solid near 
 to the surface and under a feeble pressure, that will present characters 
 different from those of the undisplaced crystalline sediments. With these 
 exceptions, then, the only distinction that can be drawn between stratified 
 and unstratified masses must, in most cases, be founded upon their atti- 
 tude, and their relations to the adjacent rocks. 
 
 In the description of the Laurentian rocks, on page 28, facts are 
 detailed which show that the stratified crystalline limestone of that series 
 was at one time plastic, and, when in that condition, was forced into the 
 fissures of broken silicious strata in the vicinity ; thus taking the form of an 
 
644 GEOLOGY OF CANADA. [CHAP. XX. 
 
 Limestones, eruptive rock. In another instance, two beds of crystalline limestone were 
 connected by a dyke of the same rock traversing an intervening bed of 
 gneiss. Other evidences of the softened state of these limestones, and 
 of their accompanying rocks, have also been given above, in the thin 
 interstratified bands both of gneiss and quartzite ; which have been broken, 
 contorted, and even twisted spirally. 
 
 The observations of Dr. Edward Hitchcock among the altered strata of 
 the Green Mountains, seem to show, in like manner, that the pebbles of 
 quartz and of gneiss, in certain conglomerate beds, have been at one time 
 so softened, as to have become flattened, laminated, and bent around each 
 other. (Amer. Journal of Science [2], xxxi, 372.) 
 
 Similar facts to those mentioned above have induced some geologists to 
 regard even crystalline limestone as eruptive. Serpentine has, in like 
 manner, generally been described by European geologists as an intrusive 
 serpentines, rock ; but it has been shown in the preceding chapters, that the serpen- 
 tines, both of the Laurentian and palaeozoic series, in Canada, are 
 stratified rocks of sedimentary origin : although it is not improbable 
 that serpentine may in certain cases, like limestone, assume the form 
 of an eruptive rock. The sedimentary origin of many granites, syenites, 
 diorites, and dolerites, cannot be denied ; and hypersthenite, which has 
 hitherto been described as eruptive, occurs in the Laurentian series as a 
 stratified sedimentary rock. 
 
 Mineral spe- It will, therefore, be proper first to indicate briefly the nature and com- 
 cies. position of the various crystalline silicated rocks, and then to describe such 
 
 of them as occur in Canada in an intrusive form. The mineral species 
 which are essential to the composition of these rocks, are few in number ; 
 and consist of quartz, orthoclase, a triclinic feldspar, which may be albite, 
 oligoclase, andesine,labradorite, or anorthite ; leucite, nepheline, natrolite, 
 or some allied zeolite ; garnet, epidote, hornblende, pyroxene, olivine, ser- 
 pentine, diallage, potash mica, magnesian mica, chlorite and talc. To 
 these may be added the carbonates of lime, magnesia, and protoxyd of 
 iron, together with magnetite. Tourmaline, beryl, zircon, spodumene, and 
 various other minerals are found, with quartz, feldspar, and mica, in cer- 
 tain granitic veins. These, however, for reasons given on page 477, are 
 to be regarded, like metalliferous veins, as the results of segregation, or 
 of infiltration ; and are thus excluded from the present category of rocks, 
 structure. The mechanical structure of crystalline rocks is very varied ; and 
 differences based upon this fact have led to a great multiplication of 
 names. First may be noted the granitoid structure, in which the mineral 
 elements are crystalline and distinct, as in ordinary granite. As these 
 become smaller, the rock is granular, and, from this, passes into a compact 
 form, in which the constituent elements cannot be distinguished by the 
 eye : such rocks are sometimes denominated cryptocrystalline. In certain 
 
CHAP. XX.] ERUPTIVE ROOKS. 645 
 
 f 
 
 cases, a foliated mineral, like mica or talc, may be so arranged as to give 
 a gneissoid form to a rock ; and this arrangement, although generally 
 regarded as an evidence of stratification, has sometimes been observed in 
 eruptive masses. Occasionally the crystallization of a rock takes place 
 around certain centres, giving rise to small rounded masses, which have a 
 radiated or a concentric structure, and form the so-called globular or 
 orbicular rocks. Distinct crystals of feldspar or of augite are often found 
 imbedded in a compact base. To such rocks the name of porphyry is 
 given; and, by analogy, a rock with a granular base, enclosing larger 
 crystals, is designated as porphyritic, or porphyroid. The name of por- 
 phyry, at first applied to designate a peculiar type of feldspathic rocks, 
 has now become so much extended, that it must be regarded only as 
 designating an accident of structure. The title of amygdaloid is given 
 to various rocks having rounded cavities, which are wholly or partially 
 filled with various crystalline minerals. Many of these amygdaloids are 
 undoubtedly altered strata, like those described on page 607 ; while others 
 are as evidently intrusive rocks, the cavities of which have been filled after 
 their eruption. 
 
 The masses into which some feldspathic mineral enters as a prominent ciassmca- 
 element, constitute by far the greater part of the rocks now under tion * 
 consideration, and are naturally divided into two classes. The first of 
 these is characterized by an excess of silica, with alumina, much potash, and 
 small portions only of lime, magnesia, and oxyd of iron ; and the second, by 
 a smaller amount of silica, and larger proportions of alumina, lime, magnesia, 
 and oxyd of iron, with soda, and but little potash. These chemical differ- 
 ences are apparent, in the crystalline rocks, in the nature of the constituent 
 minerals, and in the compact varieties, by differences in color, specific 
 gravity, and hardness. Thus, in the first class, the predominant mineral is 
 orthoclase feldspar, generally associated with quartz ; and the compact 
 rocks of this class seldom have a specific gravity much above that of these 
 species, or from 2-6 to 2-7. In the second class, the characteristic minerals 
 are a triclinic feldspar, and pyroxene, or hornblende, the feldspar sometimes 
 being predominant ; while in other cases, the pyroxene, or hornblende, makes 
 up the principal part of the rock. The presence of these latter minerals 
 generally gives to the fine grained rocks of this class, a dark color, a hard- 
 ness somewhat inferior to that of the more silicious rocks, and a 
 specific gravity which may vary from 2-7 to above 3-0. It will however 
 be found that the line between the two classes cannot always be distinctly 
 drawn, inasmuch as rocks containing orthoclase and quartz often include 
 triclinic feldspars, such as albite and oligoclase ; and by an admixture of 
 hornblende, offer a transition to the rocks of the second class. On the other 
 hand, quartz is sometimes found with triclinic feldspars and hornblende, in 
 the rocks of this class. 
 
646 GEOLOGY OF CANADA. [CHAP. XX. 
 
 The rocks in which epidote and garnet replace the feldspars, are related 
 by their chemical composition to the second feldspathic class ; and these 
 two classes, by a diminution of the amount of the aluminous element, 
 afford a natural transition to those rocks which consist essentially of silicates 
 of protoxyd bases. 
 
 Three The silico-aluminous rocks may thus be conveniently grouped in three 
 
 families : first, those in which the aluminous mineral is a potash orthoclase ; 
 secondly, those in which it is a triclinic feldspar, to which may also be added 
 those rocks containing nepheline, leucite, and natrolite; and thirdly, 
 those which contain epidote or garnet, in place of a feldspar. It is worthy 
 of note that some feldspars, having the crystallization and the general char- 
 acters of orthoclase, nevertheless contain a large proportion of soda. This 
 is shown in the analyses of several feldspars from the Laurentian rocks, 
 
 various and from the trachytes of Canada. Feldspars from the trachytes of Ger- 
 
 feidspare. many, similar in composition to these, have been described by the name of 
 potash-albite ; but the low specific gravity of the feldspars from the Canadian 
 trachytes, as *well as their apparent crystalline form, shows them to belong 
 to orthoclase rather than to albite. The relations in composition between 
 the various triclinic feldspars, including albite, oligoclase, andesine, 
 labradorite, and anorthite, have been defined on page 480. It is to be 
 recollected that in the less dense of the triclinic feldspars, silica and soda 
 predominate ; while those -"of higher specific gravity are richer in alumina 
 and lime, and are more readily attacked by acids, than the former. Thus 
 anorthite, and even labradorite are, when in powder, decomposed by heated 
 hydrochloric acid, with the separation of silica in a pulverulent form. 
 
 Pyroxene. Pyroxene or augite, and hornblende, which are essentially silicates of 
 lime, magnesia, and protoxyd of iron, occasionally contain portions of alkali, 
 chiefly soda. Certain varieties of both of these species, especially the black 
 ferruginous pyroxene, to which the name of augite is more particularly 
 given, include large portions of alumina, apparently replacing silica. The 
 composition of these two species is such that they may be represented 
 by the same general formula ; and their crystalline forms, as is well known, 
 
 Hornblende, belong to the same system, and are very simply related to one another. 
 The specific gravity of the different varieties of augite is however appar- 
 ently greater than that of the corresponding ones of hornblende ; from which 
 it is probable that the two species are isomeric, and that the equivalent of 
 pyroxene is more elevated than that of hornblende. These two minerals 
 are not unfrequently found associated in the same rock (page 467). The 
 varieties of pyroxene known as diallage and hypersthene, are sometimes 
 surrounded or penetrated by hornblende ; the crystals of the species having, 
 in such cases, their axes parallel. This association of the two minerals in 
 nature has frequently been observed, and should be kept in mind ; inasmuch 
 as the substitution of hornblende for pyroxene in feldspathic rocks is 
 
CSAP. XX.] ERUPTIVE ROCKS. 647 
 
 made the basis of a sub-division in their classification. (American Journal 
 of Science [2], xxvii. 339, xxviii. 185.) 
 
 The principal varieties of crystalline rocks may now be mentioned ; and for 
 the reasons already given, the eruptive and the stratified masses will 
 be noticed together. Inasmuch, however, as a stratified structure, arising indigenous 
 from the arrangement of the constituent minerals may occur hi eruptive 
 masses, the sedimentary origin of crystalline stratified rocks in general, is 
 denied by some geologists. On the other hand, certain undisturbed sedi- 
 mentary masses, from the conditions of their deposition, or from the 
 changes undergone during metamorphism, retain but few traces of their 
 origin. In order to assert that any given mineral masses are sediments 
 crystallized in place, it is proposed to designate them as indigenous rocks ; 
 in contradistinction to which, intrusive masses may be called exotic rocks. 
 
 The* admixture of crystalline orthoclase and quartz, generally with the Granitic 
 addition of mica, gives rise to granite. Oligoclase or albite is often asso- rocks * 
 ciated with the orthoclase, and maybe distinguished by its striated crystals, 
 or by its greyish or greenish color. The mica of granitic rocks is some- 
 times muscovite, and at other times a magnesian mica. These two species 
 are sometimes associated in the same rock, or even in the same crystal, 
 the one surrounding the other, with a common cleavage. Chlorite and 
 talc frequently occur in granite ; and the latter, by entirely replacing the 
 mica, gives rise to protogine. Black hornblende often occurs with the 
 mica, giving rise to syenitic granite ; or, by a complete replacement of the 
 mica, to syenite. Elseolite, epidote, and magnetite are sometimes met with in 
 granitic and syenitic rocks ; and the name of miascite is given to a granitoid 
 mixture of orthoclase and black mica, with elaeolite, sometimes with horn- 
 blende, albite, and quartz. To this may perhaps belong the elseolite rock 
 from Pic Island on Lake Superior, noticed on page 480. On the main 
 shore of the lake, nearly due north of the western extremity of this island, 
 is a mass of syenitic rock, composed of red feldspar and hornblende, with 
 zircons ; which resembles the zircon-syenite of Norway. 
 
 The coarsely lamellar varieties of granite are sometimes distinguished 
 by the name of pegmatite, or graphic granite ; while fine grained mixtures 
 of orthoclase and quartz have received the names of granulite, leptinite, 
 and eurite ; or where apparently homogeneous, are called petrosilex. This 
 form often becomes porphyritic from the presence of crystals of orthoclase, 
 giving rise to orthoclase-porphyry or orthophyre. In some of these porphy- 
 ries, as in those of Grenville, about to be described, the quartz is also pres- 
 ent in distinct grains ; while in some of the red antique porphyries, the base 
 contains no excess of silica, and occasionally holds crystals of oligoclase, or 
 of hornblende. Many of the granites, syenites, and orthophyres, are in- 
 trusive ; while others, scarcely distinguishable from these, are indigenous, 
 and, becoming schistose, pass into gneiss and mica-schist. 
 
648 GEOLOGY OF CANADA. [CHAP. XX. 
 
 Trachytee. The trachytes, -which consist chiefly of orthoclase feldspar, are closely 
 connected with the granites. The typical trachytes are white or of 
 pale colors, granular or finely crystalline, and frequently porous or cel- 
 lular. They appear to consist of aggregated grains, crystals, or lamellse of 
 orthoclase, without a cementing medium ; and to this appears to be due 
 that roughness to which they owe their name. Occasionally the feldspar 
 becomes coarsely crystalline, forming a granitoid trachyte, and including 
 crystals of hornblende or of magnesian mica. Grains of quartz are also 
 sometimes met with, presenting a transition to granite. 
 
 The analyses of some trachytes show the presence of an excess of 
 silica ; while in others the proportion of this element is less than in pure 
 orthoclase. It is also to be remarked, that the feldspathic substance of the 
 trachytes generally contains, besides potash, a considerable portion of 
 soda, which has led some to conclude that the feldspar of the trachytes 
 is closely related to albite ; while certain varieties are said to contain 
 crystals of oligoclase. The granitoid trachytes of Canada consist, however, 
 of an orthoclase containing a considerable proportion of soda. In many 
 of the so-called trachytic rocks of Hungary and of Guadaloupe, the pre- 
 dominant mineral is a basic feldspar like labradorite; containing large 
 amounts of lime and soda, with but little potash. 
 
 Among the trachytes found in Canada, besides the granitoid, compact, 
 and earthy varieties, are trachytic porphyries ; of which the base is some- 
 times compact, and at others crystalline. These trachytes often contain, 
 intimately mingled, a considerable amount of carbonates, chiefly carbonate 
 of lime, and occasionally portions of a zeolite, apparently natroute, are also 
 diffused throughout the mass. Through this admixture the trachytes pass 
 into phonolite. Trachytes appear to be, in all cases, exotic rocks, and the 
 lavas of many volcanoes of the historic period are trachytic. Obsidian 
 and pumice-stone, which are often associated with trachytes, are related to 
 them in composition ; and pitchstone and perlite are similar rocks, differing, 
 
 Pttchetone. however, in containing a portion of Combined water. Varieties of rocks, 
 having the characters of pitchstone, and sometimes enclosing distinct 
 crystals of feldspar, constituting a pitchstone porphyry, are found on the 
 south side of Michipicoten Island, but have not yet been studied. 
 
 From the orthoclase rocks, there is a transition, through admixture of 
 albite and oligoclase, and through trachytes containing labradorite, to 
 those rocks which are characterized by the presence of triclinic or anor- 
 thic feldspars, to the exclusion of orthoclase ; and which will be described 
 under the names of diorite, diabase, and dolerite. Some of the older lavas 
 of Etna contain, besides oligoclase, augite, and mica, crystals of ortho- 
 clase ; and the compound rock, as it forms a link between two groups, 
 has been designated trachy dolerite. Those rocks which are macle 
 up almost entirely of triclinic feldspars, have been described in the 
 
CHAP. XX.] ERUPTIVE ROCKS. 649 
 
 preceding chapter, by the name of anorthosites. Most frequently, how- 
 ever, these feldspars are accompanied by amphibole or pyroxene ; and 
 through the predominance of these, a passage is afforded to amphibolite and 
 pyroxenite, which are rocks entirely made up of these minerals. 
 
 The name of diorite is, by good authorities, restricted to rocks whose Diorite. 
 dominant elements are a triclinic feldspar, with amphibole or hornblende ; 
 while the names of diabase and dolerite distinguish those rocks in which 
 pyroxene takes the place of hornblende. As already remarked, however, 
 on page 646, the association of these two minerals in the same rock affords 
 a connecting link between diorite and diabase. 
 
 The feldspar of the diorites varies in composition from albite to anorthite, 
 and is occasionally associated with quartz. This, although most frequent 
 with the more silicious feldspars, is sometimes met with in diorites which con- 
 tain species approaching to anorthite in constitution. The varieties in diorites 
 depend not only upon differences in composition, but in structure. Some- 
 tunes the two elements are distinct, and well crystallized, constituting a 
 granitoid rock ; fine examples of which are seen in the intrusive masses of 
 Yamaska and Mount Johnson. At other times, the rock becomes finely Greenstone, 
 granular or compact ; when its color is generally of a green, more or less 
 dark, from the disseminated hornblende, and it takes the name of green- 
 stone. The greenstones of the Huronian series are, in part at least, dio- 
 rites ; but a great number of the so-called greenstone traps are pyr- 
 oxenic, and belong to the class of diabase or of dolerite. Diorite not unfre- 
 quently contains mica, which is generally brown or black in color. Chlorite, 
 magnetite, ilmenite, and sphene often occur as disseminated minerals, 
 as also carbonate of lime. The finer grained diorites are very frequently 
 porphyritic from the presence of crystals of feldspar or of hornblende. 
 Occasionally the rock is concretionary in its structure, as in the orbicular 
 diorite, or napoleonite, of Corsica ; which contains a feldspar allied to anor- 
 thite, with hornblende, and some quartz. The norite from Sweden is a 
 granular mixture of a similar kind, containing also mica ; and the ophite 
 of some authors, is a diorite in which hornblende greatly predominates, 
 passing into amphibolite. The altered rocks of the Eastern Townships 
 afford abundance of diorites, occasionally albitic ; which pass into anortho- 
 sites on the one hand, and into amphibolites on the other. These rocks 
 are there associated with pyroxenites and ophiolites, and are, in great part 
 at least, indigenous. 
 
 The rocks which are essentially composed of anorthic feldspar and pyr- Diabase, 
 oxene, present still greater diversities than the diorites, and have received 
 various names, based upon differences in texture, and in the form of the 
 pyroxenic element. It is here proposed to restrict the name of dolerite to 
 such of these rocks as contain the black augitic variety of pyroxene, and 
 to include the mixtures of triclinic feldspars with all other varieties of this 
 
650 GEOLOGY OF CANADA. [CsAP. XX. 
 
 species, under the head of diabase. These two subdivisions agree in the 
 general absence of quartz ; and in containing, as occasional disseminated 
 minerals, olivine, epidote, garnet, chlorite, talc, magnesian mica, magne- 
 tite, ilmenite, sphene, and carbonates of lime, magnesia, and iron. 
 
 The finer grained and impalpable varieties of diabase have received the 
 name of aphanite, which is often indistinguishable from the corresponding 
 forms of diorite ; and like these, it may become porphyritic, giving rise to 
 the augite-porphyry of some authors. Different varieties of this have 
 received the names of labradophyre, oligophyre, and albitophyre, according 
 to the nature of the imbedded feldspar crystals. These are sometimes 
 accompanied by crystals of pyroxene, or altogether replaced by them ; in 
 which case the pyroxene often takes the form of augite. 
 
 Hyperite. The name of hyperite or hypersthenite has been applied to those 
 varieties of diabase which contain hypersthene, or a pyroxene with the 
 form of diallage. These rocks occur abundantly in the Laurentian series, 
 and have already been described in the preceding chapter. The hyper- 
 sthene in these sometimes takes the form of a green diallage, or of a gran- 
 ular pyroxene, and is associated with mica, red garnet, and ilmenite. In 
 addition to these, epidote* is said to occur in the hypersthenites of the 
 same series, in northern New York ; and olivine, in those of Sweden and 
 the isle of Skye. Hornblende is also, in some localities, associated with 
 the hypersthene. The hyperites, although indigenous rocks in Canada, 
 are described as forming, in other regions, eruptive masses. 
 
 Those varieties of diabase or hyperite which contain diallage, have, by 
 the Italian lithologists, been called granitone ; but by Rose and others, 
 they have been described by the name of gabbro. This rock sometimes 
 contains hornblende, mica, and a mixture of epidote ; which is generally 
 finely granular or compact, and white, or greenish-white, in color. This 
 compact epidote, or zoisite, which has the hardness of quartz, and a specific 
 gravity of 3*3 3*4, is the true saussurite. With smaragdite, which is an 
 emerald-green pyroxene, often mingled with hornblende, and sometimes 
 
 Euphotide. passing into diallage, saussurite forms the euphotide of Haiiy, from Mont 
 Rosa. The compact varieties of labradorite, and of similar triclinic feld- 
 spars, have, by most modern lithologists, been confounded with saussurite ; 
 and hence the name of euphotide is frequently given to the so-called 
 granitone or gabbro, which is really only a diallagic variety of diabase. 
 The true euphotide often contains a portion of talc, and sometimes encloses 
 crystals of a triclinic feldspar, apparently labradorite ; thus offering a 
 transition to diabase. (Amer. Jour, of Science [2], xxvii, 336.) 
 
 Doierite. Under the title of dolerite, it is proposed to class those rocks which 
 consist chiefly of feldspar, and of black ferruginous pyroxene, or augite. 
 These rocks, which are sometimes coarsely granular or granitoid in their 
 structure, pass into fine grained or compact varieties, which are distin- 
 
CHAP. XX.] ERUPTIVE ROCKS. 651 
 
 guished by the names of anamesite and basalt. To the latter varieties Basalt, 
 belong a great part of the greenstone traps ; although, hi rocks of this 
 texture, it is often impossible to determine whether it is hornblende or 
 pyroxene which is mingled with the feldspar. Otivine, in grains and in 
 crystals, occurs both in the fine grained basaltic dolerites, and in the 
 granitoid varieties ; giving rise, by its predominance, to what is called 
 peridotite. Some fine grained dolerites are porphyritic, from the presence 
 of crystals of black cleavable augite, and often pass into augite-rock. 
 The carbonates of lime and iron are occasionally present in these rocks 
 to the extent of twenty per cent., or more. In like manner, mag- 
 netite and ilmenite, which are often associated in the coarser dolerites, 
 may constitute several hundredths of the mass. Many fine grained 
 dolerites contain, like phonolite, large portions of some zeolitic mineral ; 
 and they often abound in chlorite, which seems, in certain cases, 
 almost entirely to replace the pyroxene. Something analogous to this is 
 seen in the greenstones ..noticed on page 605, whose analysis shows the 
 presence of a basic hydrous silicate, allied to chlorite hi composition. The 
 name of melaphyre is often given to certain varieties of dolerite, but 
 there seems no sufficient reason for retaining the term. The fine grained 
 dolerites are often cellular, giving rise to amygdaloid or spilite ; 
 the cavities of which are generally filled with calcite, quartz, or some 
 zeolitic minerals. The earthy varieties of basalt, which are perhaps a 
 result of partial decomposition, constitute the wacke of some authors. 
 Both nepheline and leucite occasionally replace the feldspar hi dolerite ; 
 the latter admixture giving rise to what has been named leucitophyre. 
 Analcimite is a doleritic rock, containing analcime and olivine. 
 
 While very many of these rocks occur as intrusive masses, the undoubted 
 indigenous character of at least a great portion of the diabase, makes it 
 probable that a large part of the dolerites have had a similar origin. 
 Those which occur in beds, and were regarded as having been poured out 
 from the earth in a molten state, have come to be regarded, hi many cases, 
 as sediments altered in situ. Many of the so-called melaphyres, the porphy- 
 ries, and the spilites of the Alps, once regarded as eruptive, are considered 
 by recent investigators to be indigenous rocks. 
 
 The dense aluminous silicates epidote and garnet, and perhaps idocrase, Garnet and 
 give rise to a variety of compound rocks, in which they may be regarded e P idot - 
 as replacing the feldspars. In the epidosites and the red garnet-rock, 
 already noticed, these minerals occur with quartz ; while in euphotide, as 
 above described, a white epidote, or zoisite, is associated with smaragdite. 
 Related to these, is the white garnet-rock described on page 496 ; in which 
 garnet is mingled with serpentine, or with hornblende and feldspar. In 
 this connection may also be mentioned omphazite or eklogite ; which consists 
 of smaragdite and red garnet, sometimes mixed with mica, quartz, and 
 
652 GEOLOGY OF CANADA. [CHAP. XX. 
 
 kyanite, and passing, through an increase of the latter, into disthenite or 
 kyanite-rock. The latter occurs in the state of Georgia, as the gangue of 
 crystallized rutile ; and mixtures of hornblende and red garnet occur in 
 the Green Mountains in Vermont. Red garnet, with lievrite and some 
 mica, forms a rock in the Laurentian series, as described on page 460. 
 This is evidently related to eulysite, a rock forming strata in gneiss in 
 Sweden, and made up of garnet, augite, and a mineral having the compo- 
 sition of an olivine, in which a great part of the magnesia is replaced by 
 the protoxyds of iron and manganese. Related to this is an apparently 
 undescribed rock from the Tyrol, consisting of red garnet, green pyroxene, 
 and yellowish-green olivine, the latter greatly predominating ; and also a 
 coarsely crystalline rock from central France, recently describe^ by the 
 name of cameleonite, and consisting of olivine, with pyroxene, and enstatite, 
 a magnesian augite ; these minerals being accompanied by spinel, sphene, 
 and ilmenite. These rocks form a connecting link between some of those 
 just noticed, and the granitoid dolerites containing olivine, which are about 
 to be described. Through the disappearance of the aluminous element, 
 they are related to the amphibolites and pyroxenites; which pass into 
 diorite and diabase on the one hand, and, through diallage-rock, into 
 ophiolite on the other. 
 
 INTRUSIVE BOOKS OP THE LAURENTIAN SERIES. 
 
 The intrusive rocks of Canada present great varieties in composition, 
 structure, and geological antiquity. Some of them were erupted through 
 the Laurentian series before the deposition of the Lower Silurian rocks, 
 and are among the oldest intrusive masses known. In the county of 
 Rocks of Grenville there is a considerable area which abounds in eruptive dolerites, 
 Grenvme. gyenite, and orthophyre. These have been described with some detail on 
 page 37, and the succeeding pages. The oldest is a fine grained dolerite, 
 numerous dykes of which intersect the crystalline limestone and the gneiss 
 of the Laurentian series. The eruption of this rock was succeeded by that . 
 of a great mass of red syenite, passing, through an admixture of mica, into 
 granite. Dykes branching from this rock cut both the gneiss and the 
 dolerite, and are in their turn intersected by others of orthophyre, or 
 quartziferous porphyry, which traverse both the syenite and the gneiss. 
 Nothing corresponding to the syenite, or to the porphyry, is met with 
 among the adjacent Lower Silurian strata ; which are seen to repose upon 
 the worn surfaces of these intrusive rocks. A fourth series of dykes of a 
 porphyritic dolerite is however found to cut all of the preceding rocks, 
 and is perhaps identical with some of the dolerites which intersect the 
 Silurian rocks of the island of Montreal. In the other parts of the 
 Laurentian series, so far as yet examined, intrusive rocks have been 
 
CHAP. XX.] ERUPTIVE ROCKS, 653 
 
 but seldom met with. Much of what has been called syenite and granite 
 in various parts of this series, seems, like the hypersthenite and other 
 anorthic feldspar rocks, to be indigenous. 
 
 The most ancient dykes of dolerite or greenstone, from Grenville, are older do- 
 fine grained, dark greenish-grey in color, and weather greyish-white. lente ' 
 Under a lens, the rock is seen to consist of a greenish-white feldspar, with 
 a scaly fracture, mingled with grains of pyroxene, occasional plates of 
 mica, and grains of pyrites. It contains no carbonates. Two analyses 
 of portions of the dolerite, from dykes differing a little in texture, gave 
 as follows : 
 
 I. II. 
 
 Silica, 60-35 60-25 
 
 Alumina, 17 ' 35 * 32-10 
 
 Peroxyd of iron, 12-50 > 
 
 Lime, 10-19 0-63 
 
 Magnesia, 4-93 6-04 
 
 Potash, -69 -68 
 
 Soda, 2'28 2-12 
 
 Volatile, -75 1-00 
 
 99-04 100-72 
 
 The iron, although given above as peroxyd, exists in the form of pro 
 toxyd ; and in the second specimen, in part as a sulphuret, These rocks, 
 which appear to have the composition of mixtures of a basic feldspar with 
 pyroxene, do not differ from ordinary dolerite, 
 
 The newer dolerite which cuts the three other classes of eruptive rocks Newer do- 
 in the Laurentian series, has a greyish-black, very fine grained base, lerite ' 
 earthy and sub-conchoidal in fracture, and resembling somewhat the pre- 
 ceding. It contains small brilliant black grains of ilmenite, with others of 
 sphene, and small scales of mica. Occasional masses of black cleavable 
 augite, sometimes half an inch in diameter, give to the rock a porphy- 
 ritic character. It contains, besides, small cleavable masses of white 
 carbonate of lime, with which the whole rock seems penetrated. When in 
 powder, it effervesces freely in the cold with dilute nitric acid, and the 
 solution evolves red fumes on heating. In this way there were dissolved, 
 lime, equal to 8-70 per cent, of carbonate, 0-50 of magnesia, and 6-50 of 
 alumina and oxyd of iron = 15-70 per cent. The residue, dried at 212 F., 
 equalled 83*80 per cent. A portion of aluminous silicate had evidently 
 been attacked by the acid. The dried residue gave on analysis, silica 
 52*20, alumina 18*50, peroxyd of iron, with some titanic acid, 10*00, 
 lime 7*34, magnesia 4*17, potash 2*14, soda 2*41, volatile 2-50 = 99*26. 
 Except in the somewhat greater proportion of potash, it will be seen that 
 the insoluble portion of this rock differs but little from the older dolerite 
 described above. 
 
654 GEOLOGY OP CANADA. [CHAP. XX. 
 
 syenite. The intrusive syenite of this region is generally made up of flesh-red 
 
 orthoclase, and greyish vitreous quartz, with a portion of blackish-green 
 hornblende ; which is sometimes almost or altogether wanting. The feld- 
 spar is sometimes distinctly crystalline, and cleavable ; at other times, it is 
 nearly compact. In some portions, the syenite has undergone a peculiar 
 decomposition, which has reduced it to a soft unctuous greenish matter, 
 having somewhat the aspect of serpentine, or rather of steatite. This 
 change is observed in the vicinity of the remarkable veins of chert, which 
 are here found Cutting the syenite, and is more or less complete for a dis- 
 tance of two hundred yards on either side of them. In specimens of this 
 altered rock, the quartz remains unchanged ; while the feldspar, still pre- 
 serving its cleavages, has a hardness no greater than carbonate of lime. 
 It is somewhat unctuous to the touch, with a feeble waxy lustre ; and its 
 color is occasionally reddish, but more often of a pale green. Such a 
 specimen was selected for analysis, and gave of silica 80-65, alumina 
 12-60, lime -60, soda and a little potash 2-65, volatile 2-10, magnesia and 
 oxyd of iron, traces 98' 60. From this result, it appears that the feld- 
 spar of the syenite has lost nearly two thirds of its alkali ; the iron and 
 other bases having also for the most part disappeared. This change is 
 therefore in fact a partial conversion of the feldspar into kaolin ; and as 
 such a process involves a separation of silica in the form of a soluble alka- 
 line silicate, it is not impossible that this decomposition may have been the 
 source of the chert of this* locality ; which is nearly pure quartz, approach- 
 ing to chalcedony in its characters. 
 
 orthophyre. The orthophyre, or quartziferous porphyry, of Grenville, has a fine 
 grained base, which appears to be an intimate mixture of orthoclase and 
 quartz, colored by oxyd of iron, and varying in color from dark green to 
 various shades of red, purple and black, according to the state of oxydation 
 of this metal. Throughout this paste are disseminated well-defined crystals 
 of a rose-red or flesh-red feldspar, apparently orthoclase ; and, although less, 
 frequently, small grains of nearly colorless translucent quartz. Some masses 
 of this porphyry include fragments of gneiss and syenite, forming a veritable 
 breccia. For analysis, a characteristic variety was selected, the paste of 
 which was greenish-black, jasper-like, conchoidal in fracture, and feebly 
 translucent on the edges, with a somewhat waxy lustre. The hardness 
 of the rock was nearly equal to that of quartz, and the specific gravity' 
 2'62. It contained a few distinct crystals of red feldspar, and some grains 
 of quartz. The base, freed as much as possible from both of these, gave 
 silica 72-20, alumina 12-50, protoxyd of iron 3-70, lime -90, potash 3-88, 
 soda 5-30, volatile -60 = 99-08. The oxygen ratio of the alkalies and 
 the alumina is 2-02 : 5-84 ; or very nearly as 1 : 3. The alumina re- 
 quires 43-80 parts of silica to form with the alkalies, 65-48 parts of a 
 feldspar having the oxygen ratios 1 : 3 : 12 ; which are those of ortho- 
 
CSAP. XX.] ERUPTIVE ROCKS. 655 
 
 clase and albite. There will then remain 28-40 parts of silica. This, 
 with the exception of a small amount which is probably united with the 
 oxyd of iron and lime, may be regarded as uncombined. 
 
 INTRUSIVE ROCKS OP THE PALEOZOIC SERIES. 
 
 The palaeozoic strata of the district of Montreal afford a great variety vicinity of 
 of intrusive rocks, which may be classed under the heads of trachyte, Montreal - 
 phonolite, diorite, and dolerite. These various rocks appear along a 
 line of disturbance, which is nearly transverse to the undulations of the 
 Notre Dame Mountains. Commencing at the hills of Brome and Shef- 
 ford, which are nearly on the line dividing the eastern and western dis- 
 tricts of palaeozoic rocks, this disturbance may be traced for a distance of 
 180 miles, nearly w.estward, to the Lac des Chats, upon the Ottawa 
 (page 9). In this vicinity, the undulation, which is more gentle to the 
 eastward, gives place to a break in the strata. 
 
 The most important of the intrusive masses appear along this line, in the 
 form of hills, breaking through the Lower Silurian strata ; and are as 
 follows, commencing with the contiguous mountains of Brome and Shefford, 
 and going westward : Yamaska, Rougemont, Beloeil, Montarville, Mount 
 Eoyal and Rigaud ; the last being about ninety miles distant from the 
 first. A few miles to the south of Beloeil, is Mount Johnson, or Monnoir, 
 another intrusive mass ; which, although out of the range of those just 
 mentioned, apparently belongs to the same series. The mineral compo- 
 sition of these rocks varies greatly, not only for the different hills, but for 
 different parts of the same one. Thus, Shefford and Brome mountains 
 consist of a granitoid trachyte; while the succeeding one of Yamaska, and 
 Rigaud, at the other extremity of the line, are partly of trachyte and 
 partly of diorite. Monnoir and Beloeil are made up of diorite ; while 
 Rougemont, Boucherville, and Mount Royal consist in great part of 
 dolerite ; presenting, however, many varieties in composition, and some- 
 times passing into pyroxenite. The dolerites of Rougemont and Mount 
 Royal are cut by dykes of trachyte : similar dykes also traverse the diorite 
 of Yamaska, and may perhaps be connected with the trachytic portion of 
 the mountain. It is probable, judging from some specimens from Rouge- 
 mont, that the dolerite is there intersected by veins of diorite ; some of 
 which resemble that of Beloeil, and others that of Mount Johnson. Dykes 
 both of trachyte and of dolerite are also found traversing the sedimentary 
 strata, in many localities, in the vicinity of these great eruptive masses. 
 The principal varieties of intrusive rocks in this region will now be 
 described ; commencing with the trachytes, and thence passing to the 
 diorites and the dolerites. 
 
656 GEOLOGY OF CANADA. [CHAP. XX. 
 
 TBACHYTES AND PHONOLITE. 
 
 The trachytes of Brome and Shefford occupy two mountainous areas 
 near to each other. The larger one covers about twenty square miles in 
 the township of Brome, and the western part of the township of Shefford ; 
 and consists of several rounded hills, of which Brome and Gale Mountains 
 are the principal, and rise boldly to an elevation of about 1000 feet above 
 the surrounding plain. The rock shows divisional planes, giving it an 
 aspect of stratification, and is divided by other joints into rectangular 
 blocks. Another similar mass, covering an area of about nine miles, is 
 met with in the township of Shefford, a little to the north-west of the last, 
 and distant at the nearest point only about two miles from it. These 
 trachytes break through the strata of the Quebec group, and are near the 
 limit of the eastern palaeozoic district. 
 
 The rocks of these two mountainous areas present but very slight dif- 
 ferences ; being everywhere made up in great part of a crystalline feldspar, 
 with small portions of brownish-black mica, or of black hornblende, which 
 are sometimes associated. The proportion of these two minerals is 
 never above a few hundredths, and is often less than one hundredth. The 
 other mineral species are small brilliant crystals of yellowish sphene, and 
 others of magnetic iron, amounting together probably to one thousandth 
 of the mass. In some finer grained varieties, a few rare crystals 
 of sodalite and of nepheline are met with. But for the absence of 
 quartz, these rocks might be taken for varieties of granite and syenite. 
 They are very friable, and subject to disintegration ; so that the soil, for 
 some distance around the mountains, is almost entirely made up of the 
 separated crystals of feldspar ; which, however, show but little tendency 
 to decomposition, and retain their lustre. The rock is sometimes rather 
 finely granular ; but is often composed of cleavable masses, which are from 
 one fifth to one half of an inch in breadth, and sometimes nearly an inch in 
 length. The cleavages of the feldspar are those of orthoclase. The lustre 
 is vitreous, and, in the more opaque varieties, pearly ; but the crystals 
 never exhibit the eminently glassy lustre, nor the fissured appearance, 
 that characterizes the feldspars of many foreign trachytes, which are 
 identical with these in composition. The color of the feldspars of these 
 rocks is white, passing to reddish on the one hand, and to pearl-grey or 
 lavender-grey on the other. 
 
 Brome. Specimens of the rock of Brome Mountain were taken from the side 
 near to the village of West Shefford. It was coarsely crystalline, lavender- 
 grey in color, and contained a little brown mica, sphene, a^id magnetic 
 iron, but no hornblende. The density of fragments of the rock was found 
 to be 2 *632- 2*638. Selected grains of the feldspar had a specific 
 
CHAP. XX.] ERUPTIVE ROCKS. 657 
 
 gravity of 2-575 : its analysis has already been given, oh page 476, V. 
 A second specimen, from another portion of the rock, gave silica 65' 30, 
 alumina 20-70, lime '84 ; showing an identity in composition. 
 
 A specimen from the south side of Shefford Mountain was next examined, shefford. 
 A little above the place where it was collected, the rock was a coarse greyish- 
 white feldspar, with a little black mica, and closely resembled that just 
 described ; but the portion selected contained a little black hornblende in 
 brilliant crystalline grains about the size of those of rice, with very small 
 portions of magnetite and of yellow sphene. These were disseminated in a 
 base, which, although completely crystalline, was more coherent, and finer 
 grained than that of Brome ; rarely exhibiting cleavage planes more than 
 one fourth of an inch in length. Its color was yellowish-white, and it 
 was sub-translucent, with a somewhat pearly lustre. Fragments of the 
 rock had a specific gravity of 2-607-2-657. By crushing and washing 
 the mass, the white feldspar grains were separated from the heavier 
 minerals, and had a specific gravity of 2-561. The composition of this 
 feldspar, which scarcely differs from the last, is given on page 476, VI. 
 
 The greater part of the mountain of Yamaska may be described as a Yamaeka. 
 micaceous trachytic rock ; which differs from that of Brome and Shefford in 
 being somewhat more micaceous, and more fissile. The dark brown mica is in 
 elongated flakes, and there is no hornblende in the specimens collected ; 
 which however hold small portions of magnetite, and minute crystals of 
 amber-yellow sphene. These seem to be disseminated in veins of segrega- 
 tion, which are of a lighter color than the mass. The feldspar grains 
 which make up this rock are brilliant, of a vitreous lustre, and often yel- 
 lowish or reddish-grey in color. A portion of this feldspar, separated by 
 washing from the crushed mass of the rock, had a density of 2-563. The 
 analysis of this, and of another portion of selected grains, is given on page 
 479, XIII and XIV. These feldspars will be seen to differ widely in 
 composition from those of the previous trachytes, and to approach oligo- 
 olase and andesine in composition. The sphene from this rock is described 
 on page 502. 
 
 At Chambly, a mass of porphyritic trachyte is intruded in the form 
 a bed, among the strata of the Hudson River formation ; and about mid-way 
 on the Chambly canal, a similar trachyte is met with, which contains, in 
 drusy cavities, crystals of quartz, calcite, analcime, and chabazite. The 
 base of this rock is of a pale fawn color, and appears at first sight to be mica- 
 oeous ; but on closer examination it'is seen to be almost entirely feldspathic. 
 Minute portions of pyrites, and grams of magnetic iron, are rarely met 
 with, and small scales of a dark green micaceous mineral are very sparsely 
 disseminated. The crystals of feldspar, which are very abundant, are 
 sometimes an inch in length, and one fourth of an inch in thickness ; they are 
 more or less modified, and terminated at both ends. They are easily 
 
 BB 
 
658 GEOLOGY OF CANADA. [CHAP. XX. 
 
 detached from the rock, and are yellowish and opaque on the exterior ; 
 but the inner portions of the larger crystals are transparent and vitreous. 
 Their composition, which is given at page 476, IV, will be seen to be almost 
 identical with that of the feldspars of Brome and Shefford. The base of 
 this porphyry, carefully freed from crystals, lost by ignition 2*1 per cent. 
 When pulverized, and digested with dilute nitric acid, it effervesced 
 slightly, giving off carbonic acid, together with red fumes from the oxyda- 
 tion of the pyrites ; and yielded carbonate of lime 1*70 per cent., carbonate 
 of magnesia 0-98, and peroxyd of iron, with a trace of alumina, 2-12 
 per cent. The residue, dried at 300 F., gave by analysis, silica 67*60, 
 alumina 18*30, peroxyd of iron 1*40, lime *45, potash 5*10, soda 5*85, 
 volatile *25 = 98*95. The fine grained portion of this rock therefore 
 differs but little from the crystals in composition. It contains only a very 
 slight excess of silica, and seems to be made up of lamellae of orthoclase, 
 mingled with small portions of carbonates of lime and magnesia. A 
 part of the iron also is probably present as carbonate, which, by its decom- 
 position, gives rise to the rusty red color of the weathered surface of 
 the trachyte. 
 
 Rigtud. A large part of Rigaud Mountain is composed of a reddish orthoclase 
 
 rock, coarsely crystalline like that of Shefford, and sometimes holding quartz. 
 Other portions are a feldspathic porphyry, with a fine grained greyish 
 base, like the trachyte of Chambly. These trachytes are cut by thin veins 
 or dykes of a hard reddish-brown jaspery feldspathic rock. 
 
 The island of Montreal offers a great variety of trachytic rocks, which 
 traverse both the Lower Silurian strata, and the dolerite of Mount Royal. 
 Some of these dykes are finely granular, occasionally crumbling to sand ; 
 and they are frequently earthy in texture. In some cases, they assume a 
 concretionary structure, and they are often porphyritic from the presence of 
 feldspar or of hornblende. One variety exhibits large feldspar crystals in 
 a compact purplish or lavender-grey base, with a waxy lustre. This effer- 
 vesces with acids, from an admixture of earthy carbonates ; and closely 
 resembles in its aspect certain trachytes from the Siebengebirge, on the 
 calcareous Rhine. Other varieties can scarcely be distinguished from the so-called 
 trachytes. <j om ite, the trachyte of the Puy de D6me, and exhibit small drusy cavities. 
 The presence of carbonates in trachytic rocks has generally been over- 
 looked ; Deville, however, found seven per cent, of carbonate of lime 
 in a trachytic rock from Hungary, and it occurs disseminated in some 
 of the trachytes of the Siebengebirge. Some of the trachytes about 
 to be described, contain, moreover, carbonates of magnesia and protoxyd of 
 iron, and weather to some depth of a reddish-brown color, from the peroxy- 
 dation of the latter ; like the trachyte from Chambly just noticed. Acids 
 remove from many of these rocks, in addition to the carbonates, portions 
 of alumina and alkalies. These are derived from a soluble silicate, which 
 
CHAP. XX.] ERUPTIVE ROOKS. 659 
 
 is not met with in the trachytes already described, if the occasional pres- 
 ence of nepheline be excepted. In some of the compact and earthy 
 varieties about Montreal, however, this soluble silicate exists to a large 
 extent, and has the composition of natrolite. By this admixture of a 
 zeolite the trachytes pass into phonolite. 
 
 The first of these trachytes which will be noticed forms a dyke near Montreal. 
 McGill College. The rock is divided by joints, into irregular fragments, 
 whose surfaces are often coated with thin bladed crystals of an aluminous 
 mineral, apparently zeolitic. Small brilliant crystals of cubic iron pyrites, 
 often highly modified, are disseminated through the mass. The rock has 
 the hardness of feldspar, and a specific gravity of from 2-617 to 2 % 632. 
 It has a feebly shining lustre, and is slightly translucent on the edges, 
 with a compact or finely granular texture, and an uneven sub-conchoidal 
 fracture. Before the blow-pipe it fuses, with intumescence, into a white 
 enamel. The rock in powder, is attacked even by acetic acid, which 
 removes 0-8 per cent, of carbonate of lime, besides 1/5 per cent, of alumina 
 and oxyd of iron ; the latter apparently derived from a carbonate. Nitric 
 acid dissolves a little more lime, oxydizes the pyrites, and takes up, besides 
 alumina and alkalies, a considerable portion of manganese. This appa- 
 rently exists in the form of sulphuret, since, while it is soluble in dilute 
 nitric acid, the white portions of the rock afford no trace of manganese 
 before the blow-pipe ; although minute dark colored grains, associated with 
 the pyrites, were found to give an intense manganese reaction. From the 
 residue, after the action of the nitric acid, a solution of carbonate of soda 
 removed a portion of silica ; and the remainder, dried at 300 F., was free 
 from iron and from manganese. Its analysis is given on the next page, 
 under I. That of the matters dissolved by nitric acid from 100 parts of 
 the rock, will be found under I, A. 
 
 A dyke near to the last, and very similar to it in appearance, was sub- 
 mitted to the action of nitric acid, but the insoluble residue was not treated 
 by carbonate of soda. Its analysis is given under II, while that of the 
 soluble matters is to be found under II, A. A white trachyte from a dyke LacWne. 
 at Lachine, resembled the preceding, but was somewhat earthy in its aspect, 
 and effervesced with nitric acid ; which removed a portion of lime equal to 
 7*40 per cent, of carbonate. On boiling the pulverized rock with nitrate 
 of ammonia, an amount of lime equal to 5' 33 per cent, of carbonate was 
 dissolved. An accident prevented the complete determination of the 
 alkalies in the feldspathic residue of this trachyte ; and the soluble 
 silica was not removed previous to the analysis, whose result is given 
 under in. The proportion of the potash to the soda was, however, found 
 to be, by weight, nearly as two to three. The matter dissolved by nitric 
 acid will be found under III, A. 
 
GEOLOGY OF CANADA. [CHAP. XX. 
 
 Another dyke of trachyte from Lachine was concretionary, and stained 
 by infiltration : the interior of the concretions was white and earthy. The 
 substances removed from 100 parts of the rock by nitric acid, and by car- 
 bonate of soda, are given in IV, A. A partial analysis of the insoluble 
 residue showed it to be a feldspar allied to those of the preceding tra- 
 chytes : the quantities of potash and soda were, however, nearly in the 
 ratio of four to three., 
 
 A large dyke of trachyte in the limestone quarries at the Mile End, 
 near Montreal, is remarkable for the amount of carbonates which it con- 
 tains. It is greyish-white, with dark grey spots, granular, sub-vitreous 
 in lustre, and holds a few crystals of hornblende. By ignition, it loses 
 11-0 per cent, of its weight. In powder, it effervesces freely with nitric 
 acid, disengaging carbonic acid, and, when heat is applied, red fumes from 
 the peroxydation of the iron. 100 parts of the rock yielded in this way 
 4-84 per cent, of alumina ; besides lime, magnesia, and peroxyd of iron. 
 These, represented as carbonates, equalled carbonate of lime 11-60, car- 
 bonate of magnesia 3-58, carbonate of iron 3-82 = 19-00. The alkalies 
 in the solution were not determined. The composition of the residue 
 from nitric acid, from which the soluble silica was not removed, is 
 given in IV. V and VI are the analyses of the feldspathic residues 
 from two specimens of the phonolite of Lachine, which is described below. 
 
 I. II. III. IV. V. VI. 
 
 Silica, 63-25 62-90 58-50 61-62 59-70 60-90 
 
 Alumina, 22-12 23-10 24-90 21-00 23-25 24-45 
 
 Lime,...; -56 -45 -45 2-69 -99 -45 
 
 Potash, 5-92 2-43 undet. 4-66 9-16 undet. 
 
 Soda 6-29 8-69 " 5-35 .2-97 " 
 
 Volatile, -93 1-40 2-10 2-37 2-23 2-10 
 
 99-07 98-97 97-69 98-30 
 
 A second determination of the alkalies in a portion of the trachyte, I, 
 which had not previously been treated by acid, gave potash 5-40, and 
 so.da 6-49. A second analysis of II gave potash 2-28, and soda 7-95. 
 
 I, A. n, A. m, A. IV, A. 
 
 Silica, 1-43 undet. undet. 5-00 
 
 Alumina, 2-437 2 . 84 <0-27 1-32 
 
 Peroxyd of iron, 2-40$ il-47 2-51 
 
 Lime, -60 1-86 4-14 3-50 
 
 Magnesia, 1-34 1-35 
 
 Potash, -40 -25 undet. undet. 
 
 Soda, -98 -21 " 
 
 Red oxyd of manganese, 1-31 -87 .... .... 
 
 Associated with the trachytic dykes at Lachine is one of the phono- 
 lite, already referred to. It is brittle, and somewhat' schistose, breaking 
 
CHAP. XX.] ERUPTIVE ROCKS. 661 
 
 into angular fragments ; and appears to consist of a reddish-fawn colored phoneme 
 base, in which are disseminated greenish-white rounded masses, often LacWni - 
 grouped, and apparently concretionary in their nature. These greenish 
 portions are sometimes half an inch or more in diameter, and cover from 
 one third to one half of the surface. They are not very distinctly seen 
 unless the rock is moistened. The hardness of the different portions does 
 not greatly vary, and is nearly that of apatite. The specific gravity is very 
 low, being only 2-414. The mass contains small cavities filled with carbo- 
 nate of lime, which is rarely- stained purple : it is also found in small films 
 in the joints. The rock is granular in its fracture, without lustre, and is 
 feebly translucent at the edges. When pulverized, and treated with nitric 
 acid, of specific gravity 1'25, a slight effervescence ensues, with abun- 
 dant red fumes. The mass grows warm, and gelatinizes ; and on washing 
 out the acid solution, and treating the insoluble portion with a solution of 
 caustic soda, a white granular residue remains. These reactions are 
 obtained both with the fawn-colored and the greenish portions, but the 
 amount of insoluble matter is greater from the last. The rock is but 
 slightly hygroscopic : a portion of it in powder lost only 0-2 per cent, by 
 a prolonged exposure to 300 F. ; but 7-10 per cent, at a red heat. 
 
 For the quantitative analysis, the method already indicated was followed. 
 It was found, that, while a dilute solution of caustic soda removed 
 all the gelatinous silica, it took up only a trace of alumina ; leaving 
 a feldspathic residue, which was no longer attacked by nitric acid. The 
 silica was separated from the alkaline liquid. The acid solution was 
 found to contain, besides alumina and soda, a little potash, some lime, mag- 
 nesia, and iron, and traces of manganese. The greater part of the lime 
 is evidently present as carbonate ; for when a portion of the pulverized 
 phonolite, which gave to nitric acid, lime equal to 4-36 per cent, of carbo- 
 nate, was boiled with a solution of nitrate of ammonia, there were dissolved 
 3-87 per cent, of carbonate of lime ; besides which, there was a separation 
 of a considerable amount of oxyd from the decomposed carbonate of iron. 
 From this reaction, and from the entire absence of sulphur, which was 
 carefully sought for, it is probable that the whole of the iron, except the 
 small portion of peroxyd which colors the rock, exists in the state of car- 
 bonate. In the following analyses, therefore, the lime and the iron, as 
 well as a little magnesia, are calculated as carbonates. I, on the next 
 page, is the result obtained with four grams of the reddish portion of the 
 phonolite, as free as possible from the green ; and II was obtained with two 
 and a half grams of a mixture of the two colors. 
 
 In order to fix the composition of the soluble silicate, the amounts of 
 the insoluble portion, the silica, the alumina, and the alkalies, having 
 been carefully determined, and the lime, magnesia, and oxyd of iron calcu- 
 
662 GEOLOGY OF CANADA. [CHAP. XX. 
 
 lated as carbonates, the water was estimated by the loss. In this way 
 there were obtained from I and n the results given under LA and II. A. 
 
 I. 
 
 Insoluble silicate, 45 T5 
 
 Soluble " (by difference), 46 5 7 
 
 Carbonate of lime, 3.63 
 
 " iron, 3-52 
 
 " magnesia, -53 
 
 100-00 100-00 
 
 The composition of the soluble zeolitic mineral, and the readiness with 
 which it gelatinizes with acids, lead to the conclusion that it is natro- 
 lite. This, in the phonotite, is mingled with carbonates of lime, magnesia, 
 
 I, A. n, A. 
 
 Silica, 51-96 51-66 
 
 Alumina, 24-42 24-88 
 
 Soda, 12-93 13-05 
 
 Potash, 1-15 1-28 
 
 Water, 9-54 9-13 
 
 100-00 100-00 
 
 and iron, and with a potash feldspar, whose composition has already been 
 given above, under V and VI on page 660. The excess of silica in the 
 soluble portion, over that required to form natrolite, is probably due to 
 a partial decomposition of the feldspar. 
 
 Nature of The feldspars of the above trachytes and phonolites offer some con- 
 siderable variations in their composition, especially in the proportions of 
 the alkalies. In I, on page 660, the proportions of potash and soda are 
 nearly the same as in the trachytes of Brome, Shefford, and Chambly ; and 
 the same is true of IV. These are doubtless to be regarded as varieties of 
 orthoclase, with a large amount of soda ; while in the feldspar from the 
 phonolite the proportion of soda is very small. In II, on the contrary, 
 the large predominance of soda indicates a composition approaching that of 
 albite. It is further apparent, from a comparison of the feldspars of the 
 other trachytes, whose complete analyses are not given, that the pro- 
 portions of the alkalies are liable to considerable variation, even in adja- 
 cent and apparently similar dykes. All of the above feldspars are pro- 
 bably to be referred to orthoclase or to albite ; but these, in the earthy 
 trachytes, have undergone a commencement of decomposition, which con- 
 sists in the loss of a portion of silica and of alkali, and the fixing of water ; 
 resulting in the formation of kaolin. An admixture of this substance will 
 explain the increased amount of alumina, the deficiency of silica, and the 
 presence of water in the feldspars of the more earthy of these trachytes. 
 
 These trachytic dykes are not confined to the vicinity of Montreal. To 
 the southward, on the shore of Lake Champlain, there is found in and 
 about Burlington, Vermont, a great number of dykes of intrusive rock ; 
 
CHAP, XX.] ERUPTIVE ROCKS. 663 
 
 some of which appear to intersect the strata of the Quebec group, and Trachytes of 
 others those of the Trenton group. Some of these dykes are described Vemont 
 as being of greenstone ; and others, as a white or yellowish-white feldspathic 
 rock, often porphyritic from the presence of feldspar crystals. The base 
 of a yellowish-grey porphyritic dyke from Shelburne, having a rough frac- 
 ture, and a specific gravity of 2*60, gave to Prof. G. F. Barker, silica 
 67*30, alumina and peroxyd of iron 19-10, lime *79, magnesia, traces, 
 potash 4*74, soda 6-04, volatile 1*70 = 99-67. It contained a little 
 intermingled quartz ; and the mass resulting from the fusion of the rock 
 with an alkaline carbonate, contained traces of a sulphuret. (Geology of 
 Vermont, pages 579-707.) 
 
 Somewhat to the south of Burlington, on the west side of Lake Cham- New York, 
 plain, and near to Essex, there is a great mass of intrusive rock, found in 
 the slates of the Hudson River formation. As described by Emmons, it 
 is interstratified in an irregular manner among the layers of the unaltered 
 sedimentary rocks, and has a fissile and schistose structure, which gives, at 
 first sight, the aspect of stratification to what is undoubtedly an intrusive 
 rock. When exposed to the action of the waves on the lake-shore, its struc- 
 ture appears to be columnar, and sometimes concretionary. This rock is 
 described as composed of a reddish or pale leek-green compact feldspar, 
 holding crystals of the same mineral. (Geology of New York, vol. ii, 
 page 84.) These intrusive feldspathic rocks on Lake Champlain resem- 
 ble closely the trachytes of Montreal and Chambly, with the latter of 
 which, the rock of Shelburne, the only one of them which has been 
 chemically examined, closely agrees in composition. 
 
 Those diorites of the Eastern Townships, which are found in the meta- Diorites. 
 morphic region, and are regarded as indigenous rocks, have already been 
 noticed on page 604. It now remains to describe those which break up 
 through the unaltered strata, and are clearly intrusive rocks. The first Yamaska. 
 to be noticed is that of Yamaska. The greater part of this mountain 
 consists, as already described, of a micaceous granitoid trachyte ; but the 
 south-eastern portion is entirely different, being a diorite made up of a pearly 
 white crystalline translucent feldspar, with black brilliant hornblende, 
 ilmenite, and magnetic iron. This rock is in some parts rather fine grained, 
 though the elements are always very distinct to the naked eye. In other 
 parts are seen large cleavage surfaces of feldspar half an inch in breadth, 
 which exhibit in a very beautiful manner the striae characteristic of the 
 poly synthetic macles of the triclinic feldspars. The associated crystals 
 of hornblende are always much smaller, and less distinct ; forming with 
 grains of feldspar, a base, to which the larger feldspar crystals give a 
 porphyritic aspect. Finer grained bands, hi which magnetite and ilmenite 
 predominate, traverse the coarser portions, often reticulating; and the 
 
664 GEOLOGY OP CANADA. [CHAP. XX. 
 
 whole mass is also occasionally cut by dykes of a whitish or brownish grey 
 trachytic rock ; which are often porphyritic, and may perhaps be branches 
 from the trachytic part of the mountain. 
 
 A portion of the coarse grained diorite selected for examination, con- 
 tained, besides the minerals already enumerated, small portions of black 
 mica, with grains of pyrites, and a little disseminated carbonate of lime., 
 which caused the mass to effervesce slightly with nitric acid. The macled 
 feldspar crystals, sometimes half an inch in length, were so much pene- 
 trated by hornblende that they were not fit for analysis ; but by crushing 
 and washing the rock, a portion of the feldspar was obtained, which did 
 not effervesce with nitric acid, and contained no visible impurity, except 
 a few scales of mica. It was decomposed by hydrochloric acid, with 
 separation of pulverulent silica ; and its analysis, which is given on page 
 479, shows it to be near to anorthite, and identical in composition with the 
 feldspar of diorite from Bogoslowsk, in the Ural Mountains. This is 
 associated with a greenish-black hornblende, containing some soda and 
 titanic acid, with a little mica, and some quartz. (Scott ; L. E. and D. 
 Philos. Magazine [4] , xv, 518.) 
 
 Mount Mount Johnson, or Monnoir, is composed of a diorite, which, in its 
 
 general aspect, greatly resembles that of Yamaska, just described, except 
 that it is rather more feldspathic. The finer grained varieties are greyish 
 in color, and exhibit a mixture of grains and small crystals of feldspar, 
 with hornblende, brown mica, and magnetite. Frequently, however, 
 the rock is much coarser grained, consisting of feldspar grains, with slen- 
 der prisms of black hornblende, often half an inch long and one tenth 
 of an inch broad, and numerous small crystals of amber-colored sphene. 
 In this aggregate, there are imbedded cleavable masses of the feldspar, 
 often an inch long by half an inch in breadth. At the southern foot of the 
 mountain, large blocks of the coarse grained diorite are found in a state of 
 disintegration ; affording detached crystals of feldspar, with rounded angles, 
 and weathered externally to an opaque white, from a partial decomposition. 
 Near to the base of the mountain, a coarse grained variety of the diorite 
 encloses small but distinct crystals of brown mica ; and a fine grained 
 micaceous variety, containing sphene, occurs near the summit. 
 
 The feldspar, in all the specimens examined from this mountain, appears 
 to be uniform in character. Its color is white, rarely greenish or greyish ; 
 it has a vitreous lustre, inclining to pearly ; and it is somewhat translucent. 
 The cleavages of this feldspar resemble those of oligoclase, with which 
 species it also agrees in specific gravity and chemical composition. The 
 macled forms, so common in the crystals of triclinic feldspars, have not, 
 however, been detected in this variety, whose description and analysis 
 will be found on page 477. 
 
 Specimens of the rock of Beloeil Mountain consist of a kind of micaceous 
 diorite. The feldspar, which so far predominates as to give a light grey 
 
CHAP. XX.] ERUPTIVE ROCKS. 665 
 
 color to the mass, is in white translucent vitreous cleavable grains ; Beiceii. 
 associated with small distinct prisms of black hornblende, scales of 
 copper-colored mica, and grains of magnetite. The analysis of the feld- 
 spar, extracted by washing a portion of the crushed rock, and still 
 containing a little mica, is given on page 479, XV. It resembles hi 
 composition the feldspars XIII and XIV, on the same page, from the 
 micaceous portion of Yamaska; which has been described above as a 
 trachyte, and which, with the rock of Belceil, seems to constitute a passage 
 between trachyte and diorite. 
 
 A portion of Rigaud Mountain consists of a rather coarse grained diorite, Rigaad. 
 which is made up of a crystalline feldspar, white or greenish in color, 
 with small prisms of brilliant black hornblende, and crystals of black mica. 
 In some specimens the feldspar, and in others the hornblende, predominates. 
 This rock resembles the diorites of Beloeil and Mount Johnson. 
 
 DOLEKITES AND PYROXENITE. 
 
 In describing the intrusive rocks of the county of Grenville, it has been Doierite. 
 Shown that the dolerites there met with are of two ages, one anterior to the 
 syenite and the orthophyre, and the other, more recent than all of these, 
 and containing carbonate of lime and crystals of augite. This last rock 
 may be contemporaneous with some of the dolerites about to be noticed, 
 which, besides forming numerous dykes, constitute great portions of the 
 mountains of Rougemont, Montarville, and Mount Royal. In all of these, 
 however, great diversities of composition are met with, which will be 
 successively noticed. 
 
 The greater part of Montarville is composed of a coarse grained granitoid Montar- 
 dolerite,in which black cleavable augite predominates, sometimes almost to ville * 
 the exclusion of any other mineral. Small portions of white feldspar, and 
 scales of brown mica, are sparsely scattered through the rock, with grams 
 of carbonate of lime. The solution of these from the weathered surface 
 often gives to it a pitted character. In other portions, the feldspathic 
 element predominates, and the rock becomes porphyritic from the presence 
 of large crystals of augite. The worn surfaces of the dolerite sometimes 
 show alternations of this variety, with another, which is finer grained 
 and whiter. The two are arranged in bands, whose varying thickness and 
 curving lines suggest the notion that they have been produced by the flow 
 and the partial commingling of two semi-fluid masses. 
 
 Another and a remarkable variety of dolerite, found at Montarville, 
 appears to be confined to a hill on the shore of the little lake, about half 
 a mile northward from the manor-house. The whole of this hill, with the 
 exception of some adherent portions of indurated shale, seems to be com- 
 posed of a granitoid dolerite, containing large proportions of olivine. 
 
666 GEOLOGY OF CANADA. [CHAP. XX. 
 
 Peridotite. This mineral occurs in yellowish-brown rounded crystalline masses, from 
 one tenth to one half an inch in diameter ; associated with a white or 
 greenish-white crystalline feldspar, black augite, a little brown mica, and 
 magnetite. The augite appears in the form of small grains, and also in 
 well defined and terminated crystals ; which are often an inch in length by 
 half an inch in diameter, and are sometimes partially coated by a film of 
 brown mica. A further description, with an analysis of this augite, will 
 be found on page 468. The olivine varies in amount ; but, in some portions 
 of the rock, it is the predominant mineral. An account of its chemical 
 characters, and the results of its analysis, are given on page 464. 
 
 An average specimen of this olivinitic dolerite, or peridotite, was 
 reduced to powder: it did not effervesce with nitric .acid, and when 
 ignited lost only -5 per cent. When gently warmed with sulphuric acid, 
 the olivine was readily decomposed, with the separation of flocculent silica ; 
 and by the subsequent use of a dilute solution of soda, followed by hydro- 
 chloric acid, and a second treatment with the alkaline ley, 55*0 per cent, 
 of the whole were dissolved. This portion consisted of silica 37' 30, mag- 
 nesia 33-50, protoxyd of iron 26-20, alumina 3-00 = 100-00; being 
 equal to 18-4 of magnesia for the entire mass. In another experi- 
 ment, 18-0 per cent, were obtained. Taking the mean of the two analyses 
 of olivine abbve referred to, which gives 39-5 per cent, of magnesia ; 
 18.0 parts of this base correspond to 45-5 parts of olivine. The 
 remaining 9-5 parts represent alumina and silica from the feldspar, 
 and oxyd of iron from the magnetite ; both of which were somewhat 
 attacked by the acids. The undissolved portion of the rock equalled 
 ' 44- T per cent. ; and appeared to consist of a feldspar, with pyroxene, 
 some mica, and a little magnetite. Its analysis afforded silica 49-35, 
 alumina 18-92, protoxyd of iron 4'51, lime 18-36, magnesia 6-36, loss 
 (alkalies?) 2-50 = 100-00. 
 
 In some portions of the dolerite of Montarville, the feldspar is more 
 abundant, and appears in slender crystals, with augite, and with a smaller 
 proportion of olivine than the last. A specimen of this variety, being 
 crushed and washed, gave 3-9 per cent, of magnetite, and 10-0 per cent, 
 of a mixture of ilmenite with olivine. The feldspar was obtained almost 
 pure, in the form of yellowish vitreous grains, having nearly the compo- 
 sition of labradorite. Its analysis is given on page 479, XVI; where, by 
 an error, the amount of potash is said to be 9-71, instead of 0.71 per cent. 
 
 The dolerite of Montarville is traversed by veins belonging to several 
 different periods. In one instance, the black highly augitic rock is cut by 
 a dyke of a fine grained greyish-white dolerite. This is intersected by a 
 dyke of a fine greenish rock, which, in its turn, is cut off by another small 
 vein like the first. The altered shales from Montarville have been described 
 on page 634. 
 
CHAP. XX.] ERUPTIVE ROCKS. 667 
 
 The rocks of Rougemont offer a general resemblance to those of Mont- 
 arville. Some portions are a coarse grained dolerite, in which augite mont ' 
 greatly predominates; with grains of feldspar, and a little disseminated 
 carbonate of lime. In some parts, the augite crystals are an inch or 
 more in diameter, with brilliant cleavages ; and grains of pyrites are 
 abundant, with calcite, in the interstices. This rock resembles the highly 
 augitic dolerite of Montarville. Olivine is very abundant in two varieties 
 of dolerite from Rougemont. One of these has a greyish-white finely 
 granular feldspathic base, in which are disseminated black augite and 
 amber-colored olivine ; the latter sometimes in distinct crystals. The 
 proportions of these elements sometimes vary in the same specimen ; the 
 feldspar forming more than half the mass in one part, while in another 
 the augite and olivine predominate. By the action of the weather, the 
 feldspar acquires an opaque white surface ; upon which the black shining 
 augite, and the rusty-red decomposing olivine, appear in strong contrast. 
 
 Fine grained granitoid dykes are said to traverse the dolerite of 
 Rougemont ; and among the specimens brought from it, is a light grey 
 rock ; which is made up of a white crystalline feldspar, with small prisms 
 of black hornblende, and scales of brown mica ; resembling somewhat the 
 finer grained diorite of Mount Johnson. Other specimens, which are more 
 micaceous, approach in aspect to that of Beloeil. A dyke of compact 
 dolerite, holding crystals of feldspar, and grams of olivine, cuts the 
 strata of the Hudson River formation at St. Hyacinth, and has been 
 noticed on page 210. 
 
 Mount Royal consists for the most part of a mass of highly augitic Mount 
 dolerite. In some parts, large crystals of augite, like those of Montarville, Eoya1 ' 
 are disseminated through a fine grained base ; which is dark ash-grey in 
 color, and often effervesces freely with acids, from the presence of a portion 
 of disseminated carbonate of lime. At other times this is wanting, and the 
 rock is a mass of black crystalline augite, constituting a veritable pyrox- 
 enite, from which feldspar is absent. Mixtures of augite with feldspar are pyroxenite. 
 also met with, constituting a granitoid dolerite ; in parts of which, the feld- 
 spar predominates, giving rise to a light greyish rock. Portions of this 
 are sometimes found, limited on either side by bands of nearly pure black 
 pyroxenite, giving at first sight an aspect of stratification. The bands of 
 these two varieties are found curiously contorted and interrupted, and, 
 as at Montarville, seem to have resulted from movements in a heteroge- 
 neous pasty mass ; which has effected a partial blending of an augitic 
 magma with another more feldspathic in its nature. 
 
 The more augitic parts of Mount Royal contain, like the similar varie- 
 ties from Rougemont and Montarville, considerable portions of magnetite, 
 and some ilmenite. At the north end of the mountain, a variety of dolerite 
 containing olivine, occurs. It consists of a base of greyish-white granular 
 
668 GEOLOGY OP CANADA. [CHAP. XX. 
 
 Mount feldspar ; which, in the specimen examined, constitutes about one half of the 
 Boyal - mass, and incloses crystals of brilliant black augite, and semi-transparent 
 amber-yellow olivine. This rock closely resembles the feldspathic perido- 
 tite of Rougemont, described above ; but the imbedded crystals are some- 
 what larger, although less than those in the dolerite of Montarville. A 
 portion of the feldspar, freed as much as possible from augite, gave by 
 analysis the following result ; which shows that it approaches labradorite in 
 composition: silica 53*60, alumina 25*40, peroxyd of iron 4*60, lime 
 8*62, magnesia -86, alkalies, by difference, 6*12, volatile -80 = 100*00. 
 The silica contained 1*60 per cent, of a substance, which was insoluble in 
 a solution of carbonate of soda, and was apparently titanic acid. 
 Newer do- These granitoid dolerites, containing coarsely crystalline augite and oli- 
 lentes. vine, break through the Lower Silurian strata ; and portions of these two 
 minerals, probably derived from these intrusive rocks, are found in the 
 dolomitic conglomerates near Montreal ; which in some cases include masses 
 of Upper Silurian limestone, as on St. Helen's Island. Here the conglom- 
 erate is cut by dykes of a fine-grained dolerite. These, which perhaps 
 correspond to the newer dykes of the same rock at Grenville, show that 
 there were at least three distinct eruptions of dolerite, one during the 
 Silurian period, one before it, and another after it. The trachytes of 
 Montreal and Chambly appear to be still more recent, and to traverse the 
 newest dolerites. 
 
 The trachytes of Brome and Shefford seem to constitute a group apart ; 
 but the diorites of Yamaska and Mount Johnson ; although similar in 
 aspect, differ widely in chemical composition. Facts are still wanting to 
 establish the geological age of these intrusive masses. Rocks which, like 
 the different dolerites, are related in mineral composition, have been seen 
 to belong to different geological periods ; and it would not be safe to affirm 
 that the different diorites or the different trachytes of this vicinity are 
 contemporaneous. Nor, on the other hand, should even great discor- 
 dances in chemical or mineralogical constitution be necessarily regarded as 
 establishing a difference in the age of eruptive rocks. Evidence to the 
 contrary of this is seen in the contiguous and intermingled masses of black 
 pyroxenite and grey feldspathic dolerite, of Mount Royal and Montar- 
 ville ; and it is not improbable that the olivinitic dolerite which is asso- 
 ciated with these, may be contemporaneous. If, as has been already 
 suggested in this chapter, the various intrusive rocks are only displaced 
 sediments of deeply-buried and unconformable strata, it will readily be 
 conceived that plastic masses of very unlike characters may be ejected 
 simultaneously along a line of disruption. The appearance, along a similar 
 line, of mineral springs, unlike in constitution, and coming from different 
 stratigraphical horizons, as already explained on page 562, is a somewhat 
 analogous phenomenon. 
 
CHAP. XX.] ERUPTIVE ROCKS. 669 
 
 The various intrusive masses of the palaeozoic series which have been 
 described in this chapter, appear, from their compact and crystalline struc- 
 ture, to have been ejected and consolidated under the pressure of a con- 
 siderable mass of superincumbent strata. The fact, that even their 
 summits, which are in some cases more than 1000 feet above the present 
 level of the plain, appear equally solid and crystalline with their bases, 
 implies the removal, by denudation, since the eruption of these masses, of a 
 thickness of sedimentary strata, much exceeding their present height. This 
 denudation must however have taken place before the eruption of the later 
 trachytes and dolerites ; since the dolomitic conglomerates, which enclose 
 the fragments both of the olivinitic dolerite and of the Lower Helderberg 
 limestone, repose unconformably upon the Laurentian and the various 
 Lower Silurian strata ; in such a manner as to show that these offered nearly 
 their present distribution at the epoch of the deposition of the conglomerates 
 (page 358). If, then, as is probable, the exposure, by denudation, of the 
 whole of the eight hills which have been described, took place at one epoch, 
 these are all shown to have a greater antiquity than the trachytes and 
 the dolerites which traverse the conglomerate. The fine grained and 
 earthy trachytes of Montreal are consequently far more recent than the 
 crystalline ones of Brome and Shefford ; with which, however, some of 
 them agree in chemical composition. 
 
 The general absence of granite from among these intrusive masses is a 
 fact worthy of notice. Quartz has not yet been detected in the feldspathic 
 rocks of Brome and Shefford ; although, as above mentioned, the base of 
 the feldspathic porphyries of Chambly, and of Shelburne, contains a slight 
 excess of silica. The granitic rocks of Shipton, and of St. Joseph on the 
 Chaudiere, appear to be indigenous masses, belonging to the strata of the 
 Quebec group ; but the higher fossiliferous formations to the east of the 
 Notre Dame Mountains, are traversed in various places by veins and great 
 masses of intrusive granite, whose characters and distribution have been 
 described on pages 430 and 434. It is worthy of note, that the intrusive 
 masses on the two sides of the mountain range are, so far as yet observed, 
 entirely distinct in character ; and that eruptive rocks are generally want- 
 ing among the Notre Dame Mountains, which consist chiefly of stratified 
 rocks. It is also to be remarked, that the intrusive granites at their 
 eastern base, are not unlike, in mineralogical characters, to the indigenous 
 granites of the mountains ; thus suggesting the view that these are 
 possibly the source of the intrusive granites which break through the 
 Devonian strata. A similar relation has been pointed out by Durocher, 
 in Scandinavia, where the palaeozoic strata are broken by intrusive 
 masses of granite, orthophyre, zircon-syenite, and diorite. These rocks, 
 according to him, are specifically analogous to those of the underlying 
 primitive gniess, but petrographically distinct. (Bull. Soc. Gre61. de France, 
 
670 GEOLOGY OF CANADA. [CHAP. XX. 
 
 [2,] vi, 33.) These facts are in accordance with the theory of erup- 
 tive rocks developed at the commencement of this chapter ; and it 
 would be easy to extend the comparison to the intrusive diorites and 
 dolerites about Montreal, and to show their resemblance to the strati- 
 fied feldspathic rocks of the Laurentian series. (Amer. Jour, of Science 
 [2], xxix, 283, and xxxi, 414.) 
 
 The intrusive rocks of Lake Superior, which are very curious and varied 
 in their characters, for the most part remain to be studied. The little 
 which is known of their composition, including the researches of Prof. 
 Whitney, has already been given in this chapter. The intrusive rocks 
 of the peninsula of Gaspe*, have also yet to be investigated. The 
 greenstone dykes, which intersect the limestones and sandstones in the 
 vicinity of Gaspe* Basin, have been noticed on page 402. Some of 
 them are of columnar greenstone ; and others, which are amygdaloidal, 
 contain calcite, crystalline quartz, and chalcedony, and often present 
 cavities filled with petroleum. The trappean rocks interstratified with 
 the conglomerates of the Bonaventure formation, are noticed on page 441 ; 
 and the numerous trap dykes found near New Carlisle are mentioned on 
 page 446. The nature of the adjacent crystalline rocks, and their rela- 
 tions to the intrusive masses, have yet to be determined. They are per- 
 haps metamorphic strata, like those of Cape Maquereau described on page 
 2T2. Great portions of trap are also associated with the sandstone of 
 this formation at Black Cape ; and the singular brecciated beds of the 
 intrusive rock, which are found in the section at this place, have been 
 described on page 447. 
 
CHAP. XXI.] ECONOMIC GEOLOGY. 671 
 
 CHAPTER XXI. 
 
 ECONOMIC GEOLOGY, 
 
 CLASSIFICATION: 1, METALS AND THEIR ORES; H, MINERALS USED lit CERTAIN CHEMICAL MAflff- 
 FACTURES; III, MINERALS USE!) IN AGRICULTURE ; IV, MINERALS USED AS PIGMENTS; V, 
 COMBUSTIBLE AND CARBONACEOUS MATERIALS ; VI, REFRACTORY MATERIALS, AND OTHERS 
 
 tfSED IN SMELTING METALS; VII, MATERIALS FOR BRICKS, POTTERY, AND GLASS; VIII, MATE- 
 RIALS FOR CEMENTS AND MORTARS ; IX, GRINDING AND tfOLISHlNG MATERIALS ; X, BUILD- 
 ING MATERIALS; XI, MATERIALS FOR ORNAMENTAL PURPOSES; XII, LITHOGRAPHIC STONE, 
 
 Under this head it is proposed to notice those mineral substances found 
 in the province, which are susceptible of economic application. In the pre- 
 vious portions of the Volume many of these have been mentioned in describ- 
 ing the distribution of the various geological formations, or in the subse- 
 quent chapters on the minerals, rocks, and mineral waters. The economic 
 value of the latter as remedial agents is very considerable, but its discus- 
 sion would lead to considerations foreign to the plan of the present work. 
 The possible uses in the arts, to which some of these waters may be applied, 
 have already been noticed on page 564. A convenient classification of classification, 
 the other economic minerals of the province presents no small difficulties* 
 The following scheme is essentially that followed in the arrangement of 
 the collections of mineral products sent from Canada to the Exhibitions 
 of 1851 and 1855, and to the International Exhibition of 1862. Like all 
 technical arrangements, it has a disadvantage arising from the fact that 
 many substances, from their various applications, have claims to be consid- 
 ered in more classes than one. 
 
 I. Metals and their ores : iron, lead, copper, nickel, silver, gold. 
 II. Minerals used in certain chemical manufactures: iron pyrites, 
 chrome, cobalt, manganese, titanium, molybdenum, carbonate of 
 magnesia, etc. 
 HI. Minerals used in agriculture : phosphate of lime, gypsum, marl. 
 
672 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 IV. Minerals used as pigments : ochres, sulphate of barytes, etc. 
 V. Combustible and carbonaceous minerals: peat, bituminous shale, 
 
 petroleum. 
 
 VI. Refractory materials used in constructing furnaces, or in smelting 
 , metals : plumbago, soapstone, pots.tone, mica, sandstone, fire- 
 clay, moulding sand. 
 
 VII. Materials for bricks, pottery, and glass. 
 VIII. Materials for cements and mortars. 
 
 IX. Grinding and polishing materials: millstones, grindstones, hone- 
 stones, garnet. 
 
 X. Building materials : granites, sandstones, limestones, marbles, ser- 
 pentines, roofing slates, flagstones. 
 XI. Materials for ornamental purposes : porphyries, feldspars, agates, 
 
 jaspers. 
 XII. Lithographic stones. 
 
 I. METALS AND THEIR ORES. 
 
 i 
 
 Metals. Under this head will be considered those substances which are used in 
 
 the arts in their reduced or metallic state, including iron, lead, copper, nickel, 
 silver, and gold. Of the other metals enumerated on page 501 as being 
 found in Canada, cobalt, manganese, chromium, titanium, molybdenum, and 
 arsenic are chiefly used in the arts in their oxydized compounds, and will 
 be considered in the second class. The remaining elements of this class/' 
 cerium, tungsten, uranium, mercury, platinum, and indium, are as yet 
 known to exist only in minute quantities hi Canada, and the facts in their 
 history will be found in the seventeenth chapter ;. to which the reader is 
 also referred for many mineralogical details with regard to the matters 
 about to be described. 
 
 IKON. 
 
 im. The ores of iron, of economic importance in Canada, are the magnetic 
 
 oxyd, the anhydrous peroxyd, and the hydrous peroxyd. The carbonate 
 of iron has not been observed in any considerable quantity ; and the sul- 
 phuret, which is not used as an ore of iron, but is valuable for other pur- 
 poses, will be noticed in the second class. 
 
 The most abundant ore of iron in the province is probably the magnetic 
 oxyd, or magnetite ; which receives its name from the fact that it is attracted 
 by the magnet. It is sometimes endowed with polarity, and then consti- 
 tutes the native magnet or lodestone. This ore has a specific gravity of a 
 little over five times that of water, is iron-black in color, and gives a black 
 powder. It is hard, brittle, and with a shining, more or less metallic lustre. 
 When pure, it consists of 72-4 parts of iron, and 27*6 parts of oxygen ; 
 but it often contains foreign matters, either mechanically mingled or chem- 
 
CHAP. XXI.] IRON ORES. 673 
 
 ically combined, which reduce more or less the percentage of the ore. 
 The magnetic oxyd sometimes occurs in masses made up of coarse grains ; 
 at other times, the ore is fine grained and almost compact ; more rarely, it 
 occurs in regular octahedral crystals. This ore is found only hi crystalline 
 or metamorphic rocks ; and the deposits of it in Canada occur in the Lau- 
 rentian series, or in the crystalline rocks of the eastern palaeozoic basin. 
 In the former, it is met with in beds of great extent and thickness, which 
 have been noticed on pages 26, 509, and 593. A detailed description of 
 the principal deposits of this ore in the Laurentian series will now be 
 given, commencing with those on the Ottawa, and thence proceeding along 
 the Rideau, to those of Bedford and the region about Marmora. 
 
 On the south half of the third lot of the fifth range of Grenville, Grenvffle. 
 a bed of magnetic iron ore, six or eight yards wide, occurs in a mica- 
 ceous gneiss, which is interstratified with numerous bands of quartzite. 
 It was traced for about 150 yards westward, and then north-westward. 
 The accompanying strata are cut off, and limited on either side, by a mass 
 of intrusive syenite ; leaving only about 350 yards on the strike, which 
 would thus be the extent of the iron bed. The ore is somewhat mingled 
 with the earthy minerals of the gneiss, but an average sample gave 52-23 
 per cent, of metallic iron. 
 
 On the north half of the third lot of the fourth range of the same town- 
 ship, is a similar bed of magnetic ore in gneiss, from a few inches to a foot 
 in breadth. It was traced for about 100 yards, and was apparently parallel 
 with the last-mentioned band. Small portions of the sa'me ore have also been 
 met with in the fourth lot of the seventh, and in the fifth lot of the eighth range, 
 forming only small seams hi the gneiss. They are probably of no economic 
 importance, except in so far as they show the distribution of the ore, and 
 not improbably belong to the same band as the wider one mentioned above. 
 The ore in Grenville occurs in the vicinity of the limestones of the series. 
 
 On the south side of Gate Lake, in the twenty-sixth lot of the sixth wentworth. 
 range of Wentworth, two sets of beds of this ore, about 100 yards apart, 
 have been traced for half a mile on the strike ; which is N. 10 E. 
 The ore occurs in bands of gneiss interstratified in the limestone, and 
 forms several small irregular layers, not more than an inch or two in 
 thickness. It is possible that in other portions of this limestone band the 
 ores may become of economic importance. Specimens of magnetic iron 
 ore have been received from a bed about twenty feet in thickness, which 
 occurs in gneiss, in the township of Grandison. 
 
 A large deposit of magnetic iron ore is met with in the southern half Hull, 
 of the eleventh lot of the seventh range of Hull ; and it is said to have been 
 met with , again a mile beyond, in the rear of the twelfth lot of the 
 same range. The ore occurs in syenitic gneiss, which is interstratified 
 with white crystalline limestone holding mica and graphite, and forms 
 
 ss 
 
674 GEOLOGY OF CANADA, [CHAP. XXL 
 
 a bed about ninety feet in thickness. This seems to be brought to the 
 surface on the crown of an anticlinal, through which an underlying bed 
 of crystalline limestone appears. The ore is coarsely granular and very 
 pure, but is in some parts mingled with scales of graphite. An analysis 
 of what was deemed an average specimen gave for one hundred parts, 
 3-18 of quartz and graphite, and 96-09 of magnetic oxyd of iron ; = 99-27. 
 This equals 69-65 per cent, of metallic iron. 
 
 In 1854, this deposit of ore was opened by Messrs. Forsyth & Co., 
 of Pittsburg, Pennsylvania, for the supply of their furnaces at that 
 place, where it was used in connection with the iron from the ores of that 
 region. It was shipped by the Rideau Canal to Kingston, and thence by 
 the lakes to Cleveland. Up to 1858 about 8000 tons of the ore had 
 been thus exported, when the opening of the Newborough mine in South 
 Crosby, which afforded greater facilities for shipping the ore, caused the 
 Hull mine to be abandoned. 
 
 south An important deposit of magnetic iron occurs on an island in Mud 
 
 Lake, on the Rideau Canal, not far from Newborough, on the twenty- 
 sixth and twenty-seventh lots of the sixth range of South Crosby. It forms 
 a bed 200 feet thick, running northeast and southwest, in gneiss, adjoining 
 the crystalline limestone, and, according to Messrs. G. Chaffey & Brothers, 
 has been traced from the lake, on to the first and second lots on the same 
 range. This ore has, within the last few years, been mined, like that of 
 Hull, for shipment to Pittsburg, and during the years 1858 and 1859 
 about 6000 tons of ft were forwarded thence by the way of Kingston. 
 
 south ^ n *ke fourteenth lot of the first range of South Sherbrooke, a bed 
 
 sherbrooke. of twelve feet of magnetic iron occurs in gneiss. A few hundred tons of it 
 have been raised, and it has been used with advantage in lining the 
 hearths at Mr. Gzowski's iron works at Toronto. A large deposit of this 
 ore is also said to occur on the north shore of Myers's Lake, in front of 
 the seventeenth, eighteenth, and nineteenth lots of the third range of this 
 township. These lots lie nearly to the north of the last, and the bed, 
 which, according to Dr. Wilson of Perth, has a thickness of about sixty 
 feet, may be a continuation of that just mentioned. A specimen of the 
 ore from this locality was found to contain 63-0 per cent, of iron, equal to 
 87-0 of magnetic oxyd, and 12-1 of insoluble quartz and mica; = 99*1. 
 
 Bedford. ^ n * n e twenty-first lot of the ninth range of Bedford, a bed of mag- 
 netic iron ore, three or four feet in thickness, occurs at or near the 
 junction of the gneiss with the crystalline limestone. Deposits of 
 this ore are also said to have been recently discovered on the sixth lot of 
 the third range, and on Black Lake in the eighth lot of the fourth range 
 of the same township ; but no details are yet known with regard to them. 
 Another locality where this ore has been observed is near the northeast 
 end of Bob's Lake, supposed to be in the twenty-fifth lot of the fifth range 
 
CHAP. XXI.] IRON ORES. 675 
 
 of the same township. Fragments of the ore were here found at the foot 
 of a ridge of crystalline limestone, but it was not met with in place. 
 
 On the seventh lot of the second range of Escott, magnetic iron Eecott. 
 ore occurs in a reddish feldspathic gneiss, which encloses micaceous 
 layers. The strata, running northeast, dip at a high angle to the 
 northwest, and are much contorted, and traversed by small veins of 
 white quartz with flesh-red feldspar. The ore is found both in the veins, 
 and interstratified ; the largest mass of it being clasped in one of the 
 folds of the strata, and running in its axis, where it forms reticulating 
 strings. The whole quantity exposed occupies a length of about fifty 
 yards, with a maximum breadth of six or seven inches. The iron ore is 
 mixed with specks of copper pyrites ; and in an attempt made to mine it, 
 a considerable deposit of copper ore was found, from which some eighteen or 
 twenty tons are said to have been taken. The locality is probably unim- 
 portant as a source of iron ore. 
 
 The contiguous townships of Madoc, Marmora, Belmont, and Seymour 
 contain several beds of magnetic iron ore, some of which have been 
 wrought to a small extent. On the eleventh lot of the fifth range of Madoc Madoc. 
 is a bed, from which ore was formerly raised and brought to the village of 
 Madoc, where it was smelted in a blast furnace by Messrs. Seymour & Co., 
 and yielded excellent iron. The bed appears to be enclosed in a soft black 
 micaceous rock, and holds a course, which, as far as could be traced, is 
 about east by south ; while the slope of the bed, which is towards the south, 
 is between seventy-five and eighty degrees. The greatest observed 
 breadth of the bed was found to be about thirty feet, and it would probably 
 average twenty feet. A material similar to the black micaceous rock 
 which encloses the bed, appears to cut it diagonally at short intervals. In 
 one portion, the bed is said to have been thus divided at distances of from 
 three to ten feet, and in another there was an unbroken portion of fifty 
 feet. The ore is black, fine grained, and apparently very pure. It is 
 not only magnetic, but in parts possessed of magnetic polarity : these 
 portions appear to run across the ore-bed, at right angles to it. Nodules of 
 green radiating actinolite are disseminated in the ore, and yellow uranite 
 occurs in small quantities in the fissures. On either side of the above- 
 named lot, the ore is said to have been traced, westward on the twelfth lot 
 of the fourth range, and eastward on the tenth lot of the sixth, and the 
 ninth lot of the seventh range ; the distance between the extreme points 
 being about two miles. 
 
 On the north side of Crow Lake, about 300 yards from the shore, on the 
 twelfth lot of the third range of Marmora, magnetic iron ore is met with Marmora, 
 thickly imbedded in a pale green epidotic rock. An opening, which has 
 been made here, exposes a breadth of from twenty to thirty feet, through 
 which the ore is irregularly disseminated in lumps and masses, running with 
 
676 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 the stratification, which is nearly east and west, and apparently with a 
 southward dip. The bed was traced for about 300 yards to a clearing, 
 where it terminates in a sharp cliff. Portions of this ore, which were used 
 at the Marmora furnace, were said to hate been of excellent -quality, 
 and it is very free from pyrites. The course of this ore-bed, westward, 
 would carry it to an intersection with the northwestward course of the 
 big ore-bed of Beimont, next to be described : and the dip of the one being 
 northeast, and the other south, it seems probable that they may be different 
 parts of the same bed, in opposite sides of a synclinal. 
 
 Beimont. The magnetic ore formerly smelted at 'the Marmora iron furnace 
 was obtained from the eighth lot of the first range of Beimont. This 
 deposit, known as the big ore-bed, has usually been called 100 feet 
 thick. It appears however not to be a single bed, but a succession of beds 
 of ore, interstratified with layers of greenish talcoid slate and of crystalline 
 limestone, occupying a breadth across the strike, and back from Crow 
 Lake, into which it runs obliquely, of about 500 feet. Serpentine, 
 chlorite, diallage, and a greenish epidotic rock are also met with in 
 this association. The general strike of the strata appears to be about 
 S. 35 E., and the slope towards the northeastward from 25 to 50. 
 Crystalline limestone overlies the mass ; and the first hundred feet of the 
 iron-bearing strata show a vast bulk of ore, often very nearly pure, the upper 
 part of which chiefly was mined for smelting. The upper beds of ore con- 
 tain an admixture of iron pyrites, 'from which the lower portion of the 
 mass is free. The ore from a layer of thirteen feet thick at the base, 
 seems superior to the upper portion, but was not mined until a short time 
 before the works were abandoned. Many years ago a blast furnace was 
 erected at the village of Marmora, for the purpose of smelting the ore 
 from this deposit, and iron of a superior quality was manufactured. More 
 recently different companies' have, for short periods, made renewed attempts 
 to smelt the ore, with very satisfactory results so far as the quality of the 
 metal was concerned. The distance of the place from a shipping port was, 
 however, found a serious obstacle to success, and the furnace is for the 
 present abandoned. 
 
 Seymour. At Allan's Mills, on the twenty-fifth lot of the twelfth range of Seymour, 
 a dome of Laurentian rock, of two or three acres in extent, protrudes 
 through the fossiliferous limestone, and contains disseminated magnetic 
 iron ore. The rock is in part a conglomerate, holding only small crystals 
 and strings of the ore ; but apparently overlying it, and with a dip to the 
 southeast, is a rock made up of feldspar, pyroxene and epidote, holding 
 magnetic iron in considerable* abundance, for a breadth of about thirty 
 yards. It is however doubtful whether the quantity is sufficient to be 
 wrought to advantage. There are several other places in these townships 
 where iron ore has been observed and mined to a small extent. One is 
 
CHAP. XXL] IRON ORES. 677 
 
 on the ninth lot of the eighth concession of Marmora, where a fine grained 
 and pure red hematite occurs in patches disseminated through the rock. 
 
 Among the altered rocks of the Eastern Townships, magnetic iron is 
 met with, massive, or disseminated in crystals, and sometimes forming work- 
 able deposits. On the ninth lot of the ninth range of Sutton, there is a sutton. 
 bed of dolomite, whose analysis has been given on page 613. It is twelve 
 feet in breadth, and holds octahedral crystals of magnetite, which amount, 
 in many specimens, to fifty-six per cent of the mass ; corresponding thus 
 to about thirty-eight per cent, of iron. The dolomite contains, more- 
 over, a large amount of carbonate of iron, besides carbonate of man- 
 ganese ; and it is not improbable that this ore may sometimes be used to 
 advantage for smelting with other ores. This iron-bearing belt is inter- 
 stratified with a large thickness of magnesian limestone, in one part of 
 which is an irregular bed of red hematite ore, from one to two feet in thick- 
 ness. Magnetite also occurs on the second lot of the fourteenth range of 
 Bolton, in minute crystals disseminated in a fine chloritic rock. The speci- 
 mens contain a little more than one half their weight of the ore. A simi- 
 lar deposit is said to occur near the twenty-first or twenty-second lot of the 
 fifteenth range of Orford. Large loose blocks of magnetic ore, sometimes 
 half a ton in weight, are found on the second lot of the tenth range of 
 Leeds. They are near a band of serpentine, and probably not far removed Leeds. 
 from the parent rock. The presence of magnetic iron, mixed with titanium, 
 in the serpentines of this series of rocks, has already been mentioned on 
 page 501, and will be again considered under the head of Titanium. The 
 iron ores of the Eastern Townships belong, for the most part, to the species 
 about to be described. 
 
 The anhydrous peroxyd of iron assumes very different forms. When Bed hematite, 
 uncrystalline, it is dark-red and earthy in appearance, constituting the 
 varieties known as red hematite and earthy red iron ore. At other 
 times it forms scaly masses made up of small crystalline scales with a 
 metallic lustre, and is known as micaceous iron ore ; while the varieties 
 offering distinct crystals, or large crystalline faces, are known by the 
 name of specular iron, from their brilliant metallic lustre. When in this 
 form, it is dark steel-grey, or even iron-black in color ; and granular varie- 
 ties of it sometimes resemble magnetite, but are distinguished by their 
 red powder, and by being slightly or not at all attracted by the magnet. 
 
 . This ore frequently replaces the magnetic species among the crystalline 
 rocks of the Laurentian series. An important deposit of it is known on 
 the sixth lot of the ranges C and D in the township of MacNab. It 
 occurs near the Fall of the Dochart, and about a quarter of a mile from the . 
 shore of the Lac des Chats. The bed of ore, which is thirty feet in thick- 
 ness, dips S. 17 W. at an angle of 70, and rests upon crystalline Lau- 
 rentian limestone ; while it is limited at the top by a magnesian limestone, 
 
678 GEOLOGY OF CANADA. [CHAP. XXL 
 
 belonging to the Calciferous formation. To the westward, the bed has been 
 traced about one hundred yards ; but to the eastward, it is concealed by a 
 marsh. Specimens of the ore are however said to have been found in the 
 soil a mile farther to the eastward. The ore is purplish-red and compact, 
 but occasionally exhibits in its fracture a finely crystalline structure. It 
 is very pure, containing only small disseminated portions of quartz and 
 carbonate of lime. The analysis of an average specimen of this ore gave for 
 100 parts: peroxyd of iron 84*10, silica 4-00, carbonate of lime 8-80, 
 water and loss 3-10. This is equal to 58-8 per cent, of iron. 
 Bristol. At Hudson's Wharf, on the Lac des Chats, on the second lot of 
 the first range of Bristol, micaceous specular iron occurs in contact with 
 a bed of white crystalline limestone, which is overlaid by reddish syenitic 
 gneiss. The ore, which is partially mixed up with the limestone, has a 
 maximum thickness of about six inches. A small bed of the same ore 
 occurs in the overlying gneiss, at the south point of the bay, near the 
 wharf ; where it forms an interstratified bed, mingled with quartz. Neither 
 of these deposits however are of economic importance. 
 
 Lake The name of Iron Island has been given to an island in Lake Nipissing, 
 
 Kipissing. f rom <fa e i ar g e amount of red hematite which is there met with. For a 
 breadth of about forty yards along the cliff, on the east side, the rock holds 
 portions of the ore of various sizes ; sometimes running in strings of an inch 
 or more in thickness, and at other times forming masses of more than 
 half a ton weight, imbedded in the crystalline Laurentian limestones. Great 
 quantities of the ore in rounded masses, from the disintegration of the lime- 
 stone, are here scattered along the beach. At various other points on the 
 island the ore is observed, either disseminated in the limestone, or covering 
 the shore in rolled masses. It is finely granular in texture, of an iron-grey 
 color, and apparently very pure. In the red feldspathic gneiss along 
 the north shore of the island, magnetic iron ore is disseminated in con- 
 siderable abundance. 
 
 The great beds of red hematite which occur at Marquette, in northern 
 Michigan, belong to the Huronian series of rocks; but these, in Canada, 
 have as yet presented only a single small bed of the ore, which is at the 
 Wallace copper mine on Lake Huron (page 66). 
 
 specular The red hematite ores which belong to the altered strata of the Quebec 
 schists. group ? have been described on pages 245 and 615, by the names of itabir- 
 ite and specular schist. They are generally composed of small crystalline 
 scales of the micaceous variety of the red oxyd, mingled with grains of 
 quartz, and often with chlorite ; these foreign minerals being present in very 
 variable quantities, so that the schist is sometimes a rich iron ore, and some- 
 times so poor as to be of little value. The most southern locality observed 
 in Canada is on the forty-fifth lot of St. Armand East, adjoining the south- 
 eastern corner of Sutton. Here a bed, of which only five feet were visible, 
 
, XXI,] IRON ORES. 679 
 
 is interstratified with chloritic and epidotic rocks, the dip of the strata being st. Annand. 
 to the eastward, at an angle of 84. The bed was traced thirty feet, and 
 then became covered up. A portion of the ore yielded 50-0 per cent, of 
 peroxyd of iron, and another 54*8 per cent. : the mean of these would give 
 87*0 per cent, of iron. On the fifteenth lot of St. Armand West, and on 
 the west side of the Pinnacle Mountain, very beautiful specimens of coarsely 
 foliated specular iron are met with. Unlike the last, however, the ore here 
 occurs, not in a bed, but in a transverse vein, with quartz, cutting argilla- 
 ceous and chloritic slates. The ore appeared to form a bunch in the vein ; 
 and although fourteen inches thick in one part, it thins out rapidly in 
 either direction, and is not of economic importance. 
 
 Several exposures of these iron slates occur in the township of Sutton. sutton. 
 The first to be mentioned is on the seventh lot of the ninth range, where 
 the same bed is apparently repeated several times by undulations, which 
 present three distinct anticlinal folds, showing exposures of ore, fifteen, 
 eighteen, and fifty-seven feet in width. The thickness of the bed is prob- 
 ably about eight feet, and the proportion of iron varies considerably in 
 different parts. A specimen from the western side of the lot contained 
 only 24-0 per cent, of peroxyd. Another portion gave 39-0, and a third 
 yielded of peroxyd of iron 38*07, insoluble matter 55-70, volatile 0-20, loss, 
 consisting of alumina and magnesia 4-03 ; = 100-00. In the sixth lot of the 
 ninth range of Sutton, is another exposure of the iron slate, at a distance 
 of not much over one hundred yards from the last, of which it is perhaps 
 a repetition. It here presents an anticlinal fold, spanning an arch of thirty 
 feet, and has a thickness of about seven feet. In the southwest corner of 
 the same lot, and near the line of the fifth, a bed of iron slate, six feet in 
 thickness, is met with. A specimen from this gave 59-4 per cent, of per- 
 oxyd, equal to 41-6 per cent of iron. Again, on the fifth lot of the ninth 
 range, and but a few yards from the last locality, a smoothly worn, nearly 
 vertical bluff of the ore is exposed, with a breadth of twenty, by a height of 
 fifteen feet. The slaty laminae of this mass exhibit very curious contor- 
 tions, and the rock often splits into curved plates. A portion of the ore 
 from this mass yielded nearly 70-0 per cent, of peroxyd, which contains 
 seven tenths its weight of iron, equal to 49-0 per cent. 
 
 In the tenth range of Sutton, two beds of the iron slate have been exa- 
 mined. In one of these, on the northeast corner of the seventh lot, a 
 breadth of one foot of ore is exposed, which contained 56-0 per cent, of 
 peroxyd. The other bed is met with on the northeast corner of the eighth 
 lot, and has a thickness of seven feet. A specimen, which was regarded 
 as an average, gave 45*0 per cent, of peroxyd. In the eleventh, and 
 most northern range of Sutton, a bed of the iron slate, seven feet in 
 thickness, occurs in the centre of the ninth lot. Two portions of it gave 
 respectively 31-0 and 57*0 per cent, of peroxyd. This ore is very 
 chloritic in its aspect ; and the examination of a third specimen gave 47-4 
 
680 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 of peroxyd, and 44' 6 of insoluble residue; besides 2*1 percent, of mag- 
 nesia, together with alumina and a little lime. Near the south end of the 
 seventh lot of the above range is an exposure of the ore, the thickness 
 of which has has not been ascertained. It gave 41/0 per cent, of peroxyd. 
 
 The same iron slates are again met with in the adjoining township of 
 Brome. Brome. On the eastern part of the first lot of the third range are three 
 parallel exposures of the ore, the most western of which is about five feet 
 wide, and is bounded on either side by glossy black slates. About two 
 hundred yards to the east of this, is the second exposure, of which only 
 three feet are seen ; but a little to the southwestward, on the strike, a band 
 of ore, supposed to be the same, shows a breadth of eighteen feet. This 
 was formerly mined, and carried a distance of between thirty and forty 
 miles to Troy, in Vermont ; where it was smelted with an admixture of the 
 magnetic ore, which there occurs in serpentine. About thirty yards from 
 the eastern limit of the lot, a third exposure occurs, which has been mined 
 for the same purpose as the last. The thickness of the bed is here about 
 five feet, but it presents an anticlinal fold, which gives it a breadth of ten 
 feet. Cracks occur in the fold, which are filled with white quartz ; and 
 both these and the joints of the ore are sometimes lined with films of green 
 carbonate of copper. 
 
 On the second lot of the third range of Brome, and probably in con- 
 tinuation of one of the exposures just mentioned, is a bed of the iron slate, 
 five feet in thickness. It is traversed by veins, which hold quartz, chlorite, 
 and yellowish sphene, occasionally stained green by carbonate of copper. 
 A specimen of this ore gave 4'10 per cent, of peroxyd. Another yielded 
 peroxyd of iron, 45*4 ; insoluble, chiefly quartz, 52*5 ; volatile, 2*00 ; = 
 99-9. The latter equals 31-8 per cent, of iron. On the fifth lot of the 
 fourth range of Brome, a band of iron slate crosses the Yamaska, just 
 above the fall. It is eight feet thick, but is divided by a thin bed of 
 chloritic slate, and holds strings and masses of quartz. On the sixth lot, on 
 the line between the third and fourth ranges, the following section is seen : 
 
 Ft. in. 
 
 1. Chloritic schist, 10 
 
 2. Specular schist, 1 
 
 3. Dolomite, 18 
 
 4. Chloritic schist, 90 
 
 5. Specular schist, 1 
 
 6. Chloritic schist and glossy argillite, 230 
 
 7. Specular schist, 3 
 
 8. Dolomite, 9 
 
 9. Chloritic schist and glossy argillite, 180 
 
 10. Specular schist, 6 
 
 11. Dolomite, 12 
 
 12. Specular schist, 6 
 
 13. Chloritic schist, 10 
 
 565 
 
CHAP. XXI.] IRON ORES. 681 
 
 The strata of the above section, which includes the whole dolomitic 
 belt, are nearly vertical, and are given in their order from east to west. 
 A thin layer of quartz runs with the bed No. 7, and shows stains of car- 
 bonate of copper, and flakes of talc. The ore of this bed was formerly 
 mined, and sent to Troy in Vermont, to be smelted. The assay of two 
 samples of it gave respectively 56-0 and 78-0 per cent, of peroxyd of iron. 
 Another small excavation, from which ore was formerly mined for the same 
 purpose as the last, occurs on the fourth lot of the fifth range of Brome, 
 near its western limit. The bed of ore, which lies in chloritic slates, is 
 five feet in thickness, laminated in structure, and divided by thin layers of 
 granular quartz and chloritic slate. The ore is dark purple-red in color, 
 and much richer in its aspect than most of those previously noticed. A 
 specimen of it was found to contain 70' 6 per cent, of peroxyd of iron. On 
 the fifth lot of the fifth range, a bed of ore, which is probably a continu- 
 ation of the last, is met with, but its extent has not been determined. 
 
 A bed of iron slate, two feet in thickness, is said to occur in chloritic Inverness, 
 schist on the fourth lot of the second range of Inverness ; and it is probable 
 that these ores, which are so abundant in the townships of Brome and 
 Button, will be found in many intermediate localities. These slaty iron 
 ores, as will be seen from the assays, although less rich than the ores of 
 the Laurentian series, are sufficiently so to be smelted with advantage. 
 The considerable admixture of silicious matter which they contain, will 
 render it necessary to use some calcareous matter as a flux. In North 
 Carolina, where similar ores, probably belonging to the same geological 
 series, are met with, they are smelted, and are said to yield an iron which 
 is convertible into steel of very superior quality. In Plymouth, Vermont, 
 a specular schist, similar to those of Brome and Sutton, is mined ; and 
 it is mixed with the hydrous peroxyd or brown hematite, for the purpose of 
 smelting. The only attempt as yet made to work these ores of Canada, 
 is that just mentioned, in which they were carried to Vermont to be 
 smelted with the magnetic iron of Troy. Small quantities of titanium are 
 frequently found in these ores, as has been mentioned on page 501 ; and 
 as small portions of this element in iron appear, from some late experi- 
 ments of Mr. Mushet, to render it peculiarly fitted for the manufacture of 
 steel, it is not improbable that its presence in these ores may give to them 
 a peculiar value. 
 
 The presence of small amounts of red hematite among unaltered palaeo- 
 zoic rocks in various localities, has been noticed on page 510. On the Bastard 
 twenty-fifth lot of the tenth range of Bastard, there is an exposure of about 
 thirty feet of horizontal strata, belonging to the Potsdam formation, and 
 more or less colored by intermingled peroxyd of iron, which near the top 
 is found in considerable abundance, through a thickness of about three feet; 
 where it takes the form of a finely micaceous red iron ore, sometimes soft 
 
682 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 and staining the fingers, and at other times strongly coherent, and contain- 
 ing thin seams and scales of< crystalline specular iron. In some parts len- 
 ticular masses of this pure hematite, of an inch or two in thickness, occur. 
 Many years since an attempt was made to mine the ore for the supply of 
 a blast furnace erected at Furnace Falls, but the supply was found to be 
 insufficient. Similar indications of iron are also met with in the adjacent 
 township of Lansdowne (page 93), and in Ramsay ; and it is not improb- 
 able that in some parts of the distribution of this formation, the quantity of 
 ore may be such as to be economically available ; especially as deposits of 
 this ore which are wrought in northern New York, are said to belong to 
 the same formation. 
 
 The Clinton formation in the state of New York contains a bed of fos- 
 siliferous red hematite, which, in the extension of the formation into Canada, 
 
 Ancestor, is represented by an impure ferruginous bed, noticed on page 314. Near 
 Ancaster, however, a thin bed of the ore is exposed, which gave by 
 assay 54*0 per cent, of peroxyd of iron. It does not yet appear that the 
 ore in this formation in Canada is of economic importance. 
 
 In the section of the Gasp sandstones, given on page 395, it is men- 
 tioned that nodules of argillaceous carbonate of iron, or clay iron-stone, 
 occur in some of the beds. Further examinations of these strata may show 
 that, in some parts of their distribution, this important ore occurs in work- 
 able quantities. 
 
 Limonite. The ores which consist of hydrated peroxyd of iron are, for the most 
 part, included under the specific name of limonite. This mineral, in its 
 purest form, consists, in 100 parts, of peroxyd of iron 85-6, water 14'4. 
 It is distinguished from the anhydrous oxyds by its inferior hardness, and 
 its yellowish-brown powder. Limonite is never crystallized, but often 
 fibrous in structure, and sometimes forms concretionary masses. To the 
 purer and more solid varieties the name of brown hematite is often given, 
 while the less pure and more earthy varieties are known by the names of 
 
 Bog iron bog iron ore and iron ochre. These latter often contain, besides admixtures 
 
 oro - of clay or sand, a variable proportion of organic matter in chemical com- 
 bination. On page 512 will be found the description of an ochre of this 
 kind, which contains not less than fifteen per cent, of an organic acid, 
 and on the preceding page are given analyses of several bog ores ; from 
 which it will be seen that they sometimes include small amounts of oxyd of 
 manganese, and of phosphoric acid, which last detracts from their value 
 as iron ores. The more solid varieties of limonite, or brown hematite, 
 have not been met with in Canada. The ochres will be farther noticed 
 under the head of Mineral Pigments. Bog iron ore, which is of recent 
 formation, and is found at or near the surface of the soil, is widely dis- 
 tributed throughout Canada ; and as it is an important ore of iron, its 
 principal known localities will now be indicated. 
 
CHAP. XXL] IRON ORES. 683 
 
 On the shore of Lake Erie this ore is found in various localities, espe- Lake Erie. 
 cially in the townships of Charlotte ville, Middleton, and Windham. A 
 smelting-furnace at Normandale in this region was formerly supplied with 
 ore from Charlotte ville, where it was mined on the fourth lot of the third 
 range, and on the sixth, thirteenth, and fourteenth lots of the sixth range. 
 In Middleton, the ore is known on the seventeenth lot of the first range 
 north of the Talbot road ; and in the third range, on Venison Creek. In 
 Windham, it is met with on the twelfth lot of the fourteenth range. At 
 Thamesville, on the Longwood road, between London and Chatham, indi- 
 cations of the ore were observed on the banks of Mill Creek, which falls 
 into the Thames on the thirteenth lot of range B of Campden. The ore 
 occurs at intervals for about a mile above the mouth of the stream, and 
 probably in sufficient abundance to be worth working. 
 
 In the seigniory of Vaudreuil, on the sixteenth and seventeenth west lots vaudreuii. 
 of C6te St. Charles, is a deposit of bog iron, which has been traced over an 
 area of three acres, and probably extends much farther, as it is found in 
 many other lots in the vicinity. The bed of ore has in some parts a thickness 
 of four feet, and in one place a small brook exposes a section of it eight feet 
 thick. The ore is also found in the sixteenth east lot of C6te St. Charles ; 
 and in the centre of the seigniory, on the west side of C5te St. Louis. 
 Bog iron ore is said to occur in the adjoining seigniory of Klgaud, in C6te 
 St. Guillaume, on the third concession; and has been observed in scattered 
 fragments on the south side of the road, on the twelfth, thirteenth, and four- 
 teenth lots. The analysis of these ores will be found on page 511 : they 
 are very pure, and contain about 52-0 per cent, of iron. 
 
 A bed of bog ore, about two feet thick, occurs on the twenty-first lot of Bastard, 
 the seventh range of Bastard, not far from Beverley, but its extent is not 
 known. The same ore was observed on the twenty-first lot of the eighth 
 range of Eardley, at Upper Rocky Point, where it forms a bed of six inches, 
 made up of nodular masses. The extent of the deposit is not known. 
 Analyses of the ore from these two deposits will be found as above. 
 Other localities of this ore on the Ottawa are said to be as follows : 
 Templeton, on the Riviere Blanche, above McArthur's mills ; Hull, on the 
 fourteenth lot, of the seventeenth range ; March, on Lake Constance ; and 
 in Fitzroy, near the Chats. 
 
 In the Eastern Townships, bog iron ore occurs hi considerable abundance Stanbridge. 
 in Stanbridge, on the thirteenth lot of the sixth, and the twenty-seventh 
 lot of the seventh range, and probably in other parts. It is also met with 
 in the adjoining township of Farnham. The ore from Stanbridge was 
 formerly mined, and carried to Alburg in Vermont, where it was smelted 
 to some extent. Another deposit of bog ore, said to be of some importance, 
 occurs on the eighth lot of the twelfth range of Simpson. Other localities, 
 apparently of less note, are the sixteenth lot of the ninth range of Ascot, 
 
684 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 the twenty-fourth lot of the third range of Stanstead, the twelfth lot of the 
 fourth range of Ireland, and the seigniory of Lotbinie"re, at the mouth of 
 the Grande Riviere du Chene. In St. Lambert, in the seigniory of Lauzon, 
 on the east side of the ChaudiSre, is a bed of bog ore about twenty inches 
 in thickness, which has a breadth of thirty yards on the road, and was 
 traced for sixty yards to the south-east, but may probably extend very 
 much farther. 
 
 St. vainer. This ore also occurs in several localities in the seigniory of St. Vallier, 
 and in quantities which may become economically available. Two deposits 
 were examined about a mile above the junction of the two branches of the 
 Rividre du Sud. One was about 300 yards northwest from the mill on 
 the main branch, about a mile and a quarter above the junction. It 
 extended northward thirty yards, with a breadth of twenty-eight yards, 
 and a thickness of about twenty inches. The second area, about forty 
 yards farther west, was measured 1200 yards northward, with an aver- 
 age breadth of twenty-four yards, and a thickness of from twelve to twenty 
 inches. Other beds of the ore are said to occur about two miles to the 
 southeast of the main branch : and also to the northwest of the smaller 
 branch, in St. Michel. 
 
 Green island. Bog iron ore is found in abundance on the second concession of Green 
 Island, on the land of Mr. Felix Avril. It occurs in patches of from three 
 to eight inches in diameter, and from twelve to twenty inches thick, scat- 
 tered at intervals of thirty or forty paces. These were traced, with a 
 breadth of about 100 yards, across ten lots, in a southwest course, and 
 in less abundance for half a mile in a contrary direction. In the seigniory 
 of Villeray, about three miles west from Green Island River, on the land 
 of Mr. ISFarcisse Marquis, there is a bed of ore about 270 feet long, and 
 from twenty to thirty feet wide, with a thickness of from six to twelve 
 inches. It also occurs in smaller quantities on several of the farms in 
 the neighborhood. Again, in the seigniory of Cacouna, in the village of 
 La Plaine, on the land of Mr. Stanislaus Roy, a small bed of the ore was 
 observed, measuring fifty by fifteen feet, and four inches thick. A similar 
 bed was also observed on the adjoining lot to the east. Traces of the ore 
 have been met with in several other places in the seigniories of Green 
 Island, Villeray, Cacouna, and RiviSre du Loup, as well as in the townships 
 of Viger and Wentworth. The ore-bearing tract in this region measures 
 about twenty-five miles east and west, by five or six miles north and 
 south. Whether the ore occurs here in sufficient quantities to warrant 
 the establishment of a smelting-furnace is perhaps doubtftd. 
 
 Small quantities of bog ore have been found on the east side of the 
 Ha-ha River, about a mile from the Bay of that name, on the road lead- 
 ing to Bay St. Paul. It has also been observed in this region, on the 
 land of Mr. Joseph Tremblay, in the second range of Bagot, beyond the 
 
CHAP. XXI.] IRON ORES. 685 
 
 river St. Alphonse. These localities are mentioned, as they may lead to 
 the discovery of more important deposits in the vicinity. 
 
 The St. Maurice Forges, hi the vicinity of Three Rivers, were for st.Mawice. 
 more than a century supplied with bog ore collected in that vicinity. 
 One locality, now nearly exhausted, was hi the Augmentation of Caxton, 
 chiefly on the land of Mr. Pierre Boivin. About four miles to the north- 
 east of this, in the fourth range of the fief St. Etienne, is a marsh cover- 
 ing about 1200 acres, from which during the dry weather of summer a 
 good deal of ore was extracted a few years since : it occured scattered in 
 irregular patches. Two and a half miles southeast from this, in the second 
 range of St. Etienne, on the land of Mr. Louis Bellefeuille, is a bed, 
 extending in patches from six to nine inches thick, over an area of thirty 
 or forty acres, from which ore was extracted hi 1852. The ore has also 
 been obtained in considerable quantity from several localities hi the adja- 
 cent seigniory of Pointe du Lac ; and it is also said to have been brought 
 from near Nicolet, on the south side of the St. Lawrence. Two analyses 
 of selected specimens of the ore formerly used at the furnace, are given 
 on page 511, and show 52-0 and 54*2 per cent, of iron. 
 
 Between the St. .Maurice and Batiscan rivers some important deposits 
 of ore have been met with, especially in a triangular area of about six 
 square miles, lying hi the ranges of St. Felix and Ste. Marguerite, partly 
 in the seigniory of Champlain, and partly in that of Cap de la Madeleine. Champiain. 
 Over this surface, the ore is scattered in irregular patches of from four to 
 ten inches in thickness ; and for several years large quantities were obtained 
 for smelting at St. Maurice. The piles of ore obtained from several 
 patches included in three fourths of an acre, were estimated by measure at 
 390 tons ; while two other piles in the vicinity contained about 750 tons. 
 
 In the seigniory of Champlain, and on the south side of the river of the 
 same name, there is an area extending northeast, from near Richardson's 
 mills, for a distance of nearly three miles, occupying about 1100 acres ; 
 and another parallel band on the northwest, covering about seventy-five 
 acres. Over both of these the ore is distributed in patches or small beds 
 of from three to twelve inches in thickness. The northeast portion of this 
 reaches the RiviSre a la Lime, in the seigniory of Batiscan, and has been Batiscan. 
 wrought to supply the forges on the Batiscan river. To the east of this, 
 river numerous patches of the ore are found in the seigniories of Batiscan 
 and Ste. Anne de la Parade ; as also on the road between Portneuf and 
 St. Basil, on the Jacques Cartier, at Cap Sant, and elsewhere. 
 
 Within four or five miles of the village of Industey, there are several industry, 
 places hi which bog iron ore is met with. One of these is partly in the 
 township of Kildare, and partly in the Augmentation of the seigniories of 
 Lanoraie and Dautraye, comprising a superficies of .about nine square 
 miles ; and it exhibits patches of ore hi so many of the parts which have been 
 
686 GEOLOGY OP CANADA, [CHIP. XXI. 
 
 cleared of forest, as to lead to the hope that it may become profitable. 
 Among other localities in this region, the ore is found on the line between 
 the first and second ranges of Kildare, on the seventh and eighth lots ; and 
 on the seventh lot, on the road between the fourth and fifth ranges. Other 
 localities where the ore was observed were in C6te Ste. Emelie, and C6te 
 Ste. Rose ; but these portions being still in part covered with wood, it is 
 difficult to determine the extent of the ore, although it appears to be con- 
 siderable. Farther to the east, this ore was also met with between the 
 rivers Ste. Marie and Achigan, and in the seigniory of Lachenaye. 
 
 It will be seen*from the preceding description that bog iron ore in con- 
 siderable quantities is spread along the north shore of the St. Lawrence, 
 from the vicinity of Montreal nearly to Quebec. Many of these deposits 
 have been long known, and a furnace for smelting the ore was established 
 in St. Maurice in the year 1737, where the manufacture of iron was con- 
 tinued until the year 1858. In 1831, according to Bouchette, from 250 
 to 300 persons were employed at the establishment, which was famed for 
 the fine quality of its castings, and also for a superior wrought iron ; but, 
 owing to the growing scarcity of ore and charcoal in the immediate vici- 
 nity, the St. Maurice Forges were finally abandoned. 
 
 Radnor The Radnor Forges have within a few years been erected at Batiscan, 
 in the seigniory of Cap de la Madeleine, and are supplied with ore and 
 charcoal from this and the adjoining seigniory of Champlain. The crude 
 ore is brought to the furnace, partly by the workmen of the company, and 
 partly by the farmers on whose land it is found. It is washed to free it 
 from adhering earth, and then yields from forty to fifty per cent, of metal ; 
 about 2,000 tons of cast iron being now produced annually from between 
 4,000 and 5,000 tons of ore. The number of workmen employed at the 
 Radnor Forges varies from 200 to 400 ; a great many hands being required 
 at certain seasons, to dig up and bring in the ore, and to prepare and 
 transport the charcoal. 
 
 The chief manufacture of the company has, of late, been cast-iron 
 wheels for railway cars, for which the metal appears well adapted. A pair 
 of car-wheels, with an axle, of this manufacture, were sent by Messrs. 
 Larue & Co., the proprietors of the Forges, to the International Exhibi- 
 tion of 1862, which were said to have run 150,000 miles. Wrought iron 
 is also made at this establishment ; and a rolling-mill has recently been 
 - erected here, which furnishes iron for the manufacture of scythes, and 
 nail-rod iron. Limestone, which is used as a flux for the ore, is obtained 
 from the Trenton formation in the vicinity ; and a refractory sandstone for 
 the furnace hearths is obtained from the Ore's Rapids, on the St. Maurice. 
 This rock belongs to the Potsdam formation ; and being here of a freer 
 texture than in most other parts of the province, it is better fitted for resist- 
 ing fire. Blocks of from twelve to fourteen inches thick, four feet long, 
 
CHAP. XXI.] LEAD ORES. 687 
 
 and twenty inches wide, are found not to require renewal oftener than 
 once in two years. A sand which is used for moulding is found in the 
 neighborhood. 
 
 It will be seen from the preceding pages, that, with the exception of St. 
 Maurice and Batiscan, but little has been done to turn to advantage the 
 iron ores of Canada. The exportation of iron ores from Brome and Stan- 
 bridge to Vermont in former times, and more recently of those from Hull 
 and Newborough to Pittsburg, has been mentioned ; as also the furnace 
 for smelting the bog ore at Normandale, and those erected at Madoc and 
 Marmora. Canada, however, possesses in the crystalline ores of the 
 Laurentian rocks, and in the iron slates of the Eastern Townships, inex- 
 haustible supplies of rich ores of this precious metal, which may compare 
 with those of the United States, or with Sweden. It is from these magnet- 
 ite and red hematite ores, reduced by charcoal, that the finest iron of 
 the world is manufactured ; and it cannot be doubted that skilled labor 
 and capital will one day make the iron mines of Canada great sources of 
 national wealth. 
 
 LEAD. 
 
 The chief ore of lead is the sulphuret, commonly called galena, which, Galena, 
 when pure, contains in one hundred parts, 86-6 of lead and 13-4 of sulphur. 
 Galena almost always holds small portions of silver ; and in some cases the 
 amount of this metal is sufficient to render the galena valuable as a silver 
 ore. The principal facts with regard to the occurrence of sulphuret of 
 lead in Canada have already been given on page 516 ; and it now remains 
 to notice in greater detail such of the veins as have been examined, and 
 promise to be of economic importance. Well-defined veins holding galena 
 are met with in many localities traversing the rocks of the Laurentian 
 series ; and in some cases they pass upwards through the overlying Pots- 
 dam and Calciferous formations, showing them to be younger than the 
 latter. The veins at Bay St. Paul, mentioned on page 516, traverse the 
 limestones of the Trenton group ; and the great lead-bearing stratum of 
 Wisconsin is newer than the Trenton group (page 623). 
 
 Several veins containing galena, are met with cutting the Laurentian Bedford, 
 limestone in the township of Bedford. One of them, on the twenty-first 
 lot of the eighth range, has a direction about east and west, with an under- 
 lie to the north, < 80. It is four feet wide, and consists chiefly of calc- 
 spar, through which galena is disseminated in crystals or hi seams, some- 
 times an inch or two in thickness. A shaft was formerly sunk here to a 
 depth of twenty-five feet. Two other veins similar in character are met 
 with near the line between the eighteenth and nineteenth lots of the 
 same range, the one running N. 20 W., and the o'ther N. 37 W. A 
 little to the west of these, and on the nineteenth lot of the seventh range, 
 
688 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 Lansdowne. 
 
 Ramsay. 
 
 on the property of Mr. Weston Hunt of Quebec, are five nearly parallel 
 lodes, running northwest, and included in a breadth of a quarter of a 
 mile. They traverse crystalline limestone, and include galena in a mix- 
 ture of calc-spar and heavy spar. A specimen from one of them shows a 
 breadth, across the vein, of five inches of solid galena. About a mile to 
 the eastward of these lodes, there are others on land belonging to the pro- 
 prietor of the last. Shallow trial shafts were, many years ago, sunk upon 
 these, but the amount of lead ore obtained from them is not known. On 
 lot thirteen of the fifth range of Bedford, Messrs. Foley & Co. of Montreal 
 have sunk a trial shaft to a depth of sixteen feet, on a lode of six inches, 
 the gangue of which is heavy-spar. The lode traverses the crystalline 
 limestone, and enters the gneiss, in both of which rocks it holds good 
 masses of galena. 
 
 Similar veins of lead ore are found in Lansdowne. One of these, on 
 the second lot of the eighth range, has been traced for a quarter of a mile, 
 running nearly N. W. and S. E., and has an average breadth of two feet. 
 Through the gangue, which is of calc-spar and heavy spar, galena is irregu- 
 larly distributed in crystals and small masses ; and it is also found dis- 
 seminated in the crystalline limestone which forms the walls of the vein. 
 Trial shafts were at one time sunk here ; but the mine was abandoned. 
 Another lode running N. 65 W., was subsequently found on the third 
 lot of the same range. It traverses crystalline limestone, and has a breadth 
 of from six to twelve inches. Through the gangue, which is calc-spar, 
 galena is found in masses sometimes five or six inches in diameter. A 
 trial shaft of fifty feet, which was sunk upon this lode in 1854, on the land 
 of Mr. Buel, is said to have yielded sufficient ore to pay the expenses of 
 sinking. A branch lode diverges from the main one near the shaft ; and in 
 the same neighborhood there occur four other lead-bearing lodes parallel 
 with the main, the whole being included in a breadth of about 1000 feet. 
 These run obliquely across the lots, and thus intersect the lands of several 
 proprietors. On the fourth lot of the eighth range, Messrs. Eoley & Co. 
 have sunk a small shaft upon one of the lodes. 
 
 On the third lot of the sixth range of Ramsay, a mine has been opened 
 upon a vein holding galena, and cutting a grey dolomite which belongs to 
 the Calciferous formation. The beds of this are nearly horizontal ; and they 
 repose conformably upon the sandstone of the Potsdam formation, the out- 
 crop of which is seen at a distance of about a mile from the mine, where 
 it reposes upon the upturned limestone and gneiss of the Laurentian 
 series. The lode has a bearing of from N. 50 W. to N. 55 W., with an 
 underlie to the northeast of about a foot in a fathom ; and it has a breadth 
 of from two and a half to five feet, the ore-bearing part varying from eight to 
 twenty-four inches. The galena occurs in a gangue of calc-spar, with 
 small portions of iron pyrites, copper pyrites, and blende. A shaft 
 
CHAP. XXL] LEAD ORES. 689 
 
 of thirty-seven feet was sunk upon this vein, and about seventy-five fathoms 
 in the plane of it having been excavated, twenty-six tons of ore, yielding 
 eighty per cent, of lead, were obtained. Some portions of the lode were 
 nearly destitute of ore, while in other parts its amount was estimated at 
 nearly two tons to the fathom. 
 
 This trial was made in 1858, when a smelting furnace was built, and a 
 ten horse-power engine erected for the purposes of a blast, and to remove 
 the water from the mine. The influx of water was however so consider- 
 able, that this was found insufficient, and the mine was for a time aban- 
 doned. More recently however a new engine of fifty horse-power has been 
 erected. About 105 fathoms southeastward from the main shaft, a counter- 
 lode joins the main one, at an angle of about 20 ; its- course being nearly 
 N.N.E. and S.S.W. At the junction of the two lodes, a shaft has been 
 sunk in sandstone to a depth of twenty-one feet ; and in the excavation, in 
 which the united lodes attain a breadth of ten feet, there were obtained 
 about ten tons of twenty per cent. ore. Other lodes holding lead ores, 
 and nearly parallel with the ones described, have since been noticed in 
 the vicinity. 
 
 A lead-bearing lode occurs on the twentieth lot of the eighth range Fitzroy. 
 of Fitzroy, which traverses a crystalline limestone containing mica and 
 graphite. There is a well-defined vein, apparently about six inches wide, 
 in which masses of galena are disseminated through a gangue of calcspar. 
 The existence of galena in several other localities in the region of the 
 Ottawa has been reported. Among others a vein of six or eight inches is 
 said to exist upon the North Petite Nation River, on the seigniory of the 
 Hon. L. J. Papineau. Galena has also been brought from the Gatineau 
 and the Black River ; in the former case, associated with purple fluor-spar. 
 The distance between the lodes of Lansdowne and those of Bedford is 
 about twenty-five miles ; and as they bear for one another, it is not improb- 
 able that they may be continuous, or may belong to one group of veins. 
 If the line which connects these two localities of lead ore were continued 
 for twenty-five miles farther, it would traverse the St. Lawrence, and reach 
 Rossie, in St. Lawrence County, New York ; where a similar group of 
 lead-bearing veins is found traversing Laurentian gneiss. These veins, 
 although now abandoned, were at one time extensively wrought, and two 
 of them afforded for a time great quantities of ore. One, in particular, 
 yielded as much as $142 worth to a fathom. In this vicinity, at Redwood 
 in New York, a lead-bearing lode is found cutting the Potsdam formation. 
 The Ramsay lode belongs to another series of veins, which would run 
 parallel to the Bedford and Rossie group, about forty miles to the north- 
 eastward ; and that of Fitzroy may belong to a third series. 
 
 Veins holding lead ore are found in several localities on the north 
 shore of Lake Superior. Some of these traverse the granitic gneiss of Su P erior ' 
 
 TT 
 
690 
 
 GEOLOGY OF CANADA. 
 
 . XXI, 
 
 Black 
 Hirer. 
 
 Granite the Laurentiaxi series, as on Granite Islet, in Black Bay, where a vein 
 of twelve inches in breadth carries a considerable quantity of galena in a 
 breccia of fragments of the wall-rock, cemented by drusy crystalline 
 quartz. This ore does not appear to contain much silver. Farther to the 
 east, and at a mining location at the mouth of the Black River, to the 
 north of the Slate Islands, the Laurentian rocks are seen near their con- 
 tact with the Huronian series. Here a vein of quartz oocurs in the 
 granitic gneiss. It runs nearly east and west, with a breadth of from 
 one and a half to five feet, and holds galena and iron pyrites. The 
 latter is more abundant near the shore ; but about twenty rods beyond, 
 in the hill, the galena predominates. According to Prof. Hadley, this 
 ore is extremely rich in silver ; the lead reduced from it containing from 
 two to three per cent, of the precious metal. This galena, according to 
 the same authority, contains a trace of selenium. 
 
 In the description of the copper deposits of Lake Superior, mention will 
 be made of several localities where galena occurs in small quantities, 
 generally with blende or with sulphurets of copper. One of these is at 
 
 Mamainse. Meredith's location, Mamainse, where three veins, holding considerable 
 quantities of argentiferous galena, with vitreous copper ore, have been 
 observed. These localities are in the upper copper-bearing rocks. In 
 the Quebec group of Eastern Canada, which is regarded as their equiva- 
 lent, ores of lead have been occasionally met with associated with the 
 copper deposits of the region whose distribution and relation to the 
 stratification will presently be described. In these localities galena is 
 found in small interstratified masses or layers. One of these is on the 
 fifty-first lot of the twenty-first range of Upton, where irregularly distri- 
 buted patches of fine-grained galena, from one to four inches in thickness, 
 occur in the copper-bearing magnesian limestone (page 712). They are 
 sometimes distinctly interstratified with the rock, and overlaid by por- 
 tions of copper pyrites. .Galena occurs in similar masses, also with copper 
 pyrites, and with a little blende, on the thirty-second lot of the fifth 
 range of Acton. A like variety of fine-grained galena is found with cop- 
 per pyrites on the ninth lot of the ninth range of Ascot. These ores of 
 lead contain but little silver. Although the galena in none of these 
 deposits appears to be in workable quantity, its presence in interstratified 
 masses is not to be overlooked in a region where the numerous deposits 
 of copper ore, which occur under similar conditions, are occasionally found 
 to be of very great extent and importance. 
 
 St. Armand. At Cook's Corner, in St. Armand, a vein of white quartz running with 
 the strike, cuts the black slates and limestone of the region (page 240). 
 It has a breadth of five or six inches, and contains small portions of galena, 
 with a little copper pyrites and blende. The lead of this ore was found 
 to contain a notable proportion of silver. 
 
 Upton. 
 
 Acton. 
 
CHAP. XXL] LEAD ORES. 691 
 
 Veins holding lead ore have been found in the slates which belong to 
 the Upper Silurian or Devonian strata, whose position to the southeast of 
 the Quebec group is defined on page 709. One of these localities is 
 described on page 517. The galena is here associated with native gold, 
 mispickel, and sulphurets of iron and zinc, both containing gold. Another 
 locality is at Moulton Hill, on the fifteenth lot of the fourth range of 
 Ascot. Here a vein of white quartz, about four and a half feet wide, Ascot, 
 occurs in a black shale, which is also traversed by numerous small seams 
 of quartz. The galena is here, as at Vaudreuil, associated with mispickel, 
 and is argentiferous. It is too sparingly distributed in the vein to be of 
 importance as an ore of lead, although it may perhaps be wrought for the 
 silver, of which it contains a considerable proportion. 
 
 A similar quartz vein occurs in black slates of the same age as the last, owl's Head, 
 on the eighth lot of the eleventh range of Potton. It is on the shore of Potton - 
 Lake Memphremagog, and is described as being about ten feet wide. 
 The galena is however confined to a small portion of this breadth ; from 
 which fine specimens of solid ore, two or three inches in thickness, have 
 been extracted. Little is however as yet known of the extent of this 
 deposit. The ore, like that from the last two localities mentioned, contains 
 silver ; and this fact, together with the presence of gold in one of these, 
 leads to the expectation that the upper rocks of this region may, when 
 farther explored, become important as sources of the precious metals. 
 
 The veins holding galena, which occur at Indian Cove, and at Little Gaspe* 
 Cove, have been noticed on page 400. Attempts are said to have been 
 made, before the conquest of the country, to mine for lead at Little 
 Gaspe* Cove ; and others have lately been made by Mr. George Desbarats, 
 and since by Mr. C. C. Closter. The lode occurs in a mass of stratified 
 limestone, which dips about S. W. < 24, and rises northward into a hill 
 700 feet in height, which constitutes Gaspe* promontory. It has a 
 breadth of about eighteen inches ; and is composed of calc-spar holding 
 masses of galena, together with small portions of blende and copper ore. 
 A trial shaft was sunk here to the depth of twenty feet upon the main vein ; 
 from which, and from several smaller parallel veins in the vicinity, about 
 twenty tons of sixty per cent, ore were recently obtained. Besides the 
 two localities already mentioned, galena has been observed in veins in 
 several other localities in the limestones on the south side of Gaspe* Prom- 
 ontory ; and also on the north side, in a vein which may perhaps be a 
 continuation of that of Little Gaspe* Cove. Small quantities of galena have 
 been* found in veins in the limestones at Perce* ; and also at the Ance 
 Cousin, in a vein cutting the sandstone, in the vicinity of the greenstone 
 dyke mentioned on page 402. 
 
692 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 COPPER. 
 
 This metal occurs in Canada in the form of native or metallic copper ; 
 the workable .deposits of which are confined to the rocks of the Upper 
 Copper-bearing series on Lake Superior. The three sulphuretted ores are 
 however, more abundant, and widely distributed. They are, first, copper 
 glance, or vitreous copper ore, which is a simple sulphuret, consisting, in 
 its purest state, of copper 79-8, sulphur 20-2. From its blackish-grey 
 color, this mineral is often incorrectly called the grey sulphuret, or grey 
 ore ; but it is not to be confounded with the tetrahedrite, which is also 
 designated grey copper, or fahlerz, and is a comparatively rare ore of cop- 
 per and antimony, not known in Canada. The second ore to be noticed is 
 the erubescite or phillipsite. This, from the color which its surface assumes 
 by exposure to the air, is known by the different names of purple copper, 
 variegated copper, and peacock or horse-flesh ore. In its purest form it 
 contains from fifty-six to sixty-two per cent, of copper, the remainder being 
 sulphur and iron. The third ore to be mentioned is chalcopyrite, or yellow 
 copper pyrites, known also by the names of pyritous copper and yellow 
 copper ore. Like the last, it is a double sulphuret of copper and iron, the 
 purer varieties of which contain from thirty-two to thirty-four per cent, of 
 copper. It Is however often mixed with iron pyrites. 
 
 Copper ores have been observed in several localities among the rocks of 
 
 Burgees, the Laurentian series. In North Burgess, on the second lot of the ninth 
 range, copper pyrites has been met with in three places, within a distance 
 of a few hundred feet, in the crystalline limestone. So far as the slight 
 excavations show, it seems to occur, not in well-defined veins,' but in 
 irregular masses, or in strings throughout the rock. Some of these are, 
 however, four or five inches in diameter. The ore is generally pure and 
 crystalline, mingled with a little calcareous spar, and occasionally stained 
 with blue and green carbonates. An average specimen of one of these 
 masses gave 27 '5 per cent, of copper. The same ore is said to occur 
 under similar conditions, in the limestone, on the fifth lot of the eighth, 
 and on the first lot of the sixth range of North Burgess. 
 
 Bastard. Small quantities of copper ore were some years since found on the 
 twenty-fourth lot of the tenth range of Bastard, near to where a bed of con- 
 glomerate is interstratified with the Laurentian limestone, as described on 
 page 31. Several veins of calc-spar, one of them two or three inches 
 wide, here intersect the strata, and a shaft of twenty feet, and two others 
 of seven or eight feet, were sunk. It is said that a vein of ore, an inch 
 or two in thickness, was visible near the surface ; but the portions now 
 exposed contain only small disseminated grains of copper pyrites. 
 
 Considerable deposits of copper pyrites have also been observed in the 
 township of Escott. One of these is on the seventh lot of the second 
 
CHAP. XXI.] COPPER ORES. 693 
 
 range, and is associated with a bed of magnetic oxyd of iron about six Escott. 
 inches in thickness, which is interstratified with gneiss. The mass of cop- 
 per ore was said to be lenticular in shape, and to have been traced contin- 
 uously for about twelve feet, with a maximum thickness of ten inches. It 
 consisted of nearly pure copper pyrites ; containing in parts, however, thin 
 veins and grains of calc-spar, together with portions of iron pyrites. This 
 increased in amount towards the northwest side, into which the copper ore 
 appeared to run in small strings for short distances. About twenty tons 
 of rich copper ore were quarried from this place ; when the mass seemed 
 to be exhausted, and the working was abandoned. The iron pyrites from 
 this locality contain traces of cobalt. Another deposit of copper ore is 
 described as existing on the sixteenth and seventeenth lots of the second 
 range of Escott ; and, according to the description of Mr . Macfarlane, it occurs 
 in a vein, or interstratified bed, running northeast, and traversing a mica- 
 ceous schist. It consists of orthoclase, with quartz, tourmaline, and a little 
 mica, and has a thickness of four or five feet, including about fifteen inches 
 of solid copper pyrites, mingled only with some iron pyrites and quartz. 
 This vein is seen in the roof of a drift which has been made here. About 
 eighty fathoms to the southwest, in the direction of the strike, is another 
 opening, said to contain a vein three feet in breadth, and to include copper 
 and iron pyrites with tourmaline, quartz, and feldspar. These interesting 
 localities require further investigation. Other deposits of copper ore prob- 
 ably occur in this region, since several rolled masses of copper pyrites 
 have been found on the shore of Gananoque Lake ; one of which, weighing 
 seven or eight pounds, is very pure and crystalline, and closely resembles 
 that found in the first described locality in Escott. 
 
 In the augmentation of Lanoraie and D'Autraye, on the left bank of the Lanoraie, 
 Assumption River, and about three miles above the point where this enters 
 the fifth range of Kildare, an evenly bedded mass of micaceous gneiss, 
 dipping N. 44 W. < 26, is cut by a vein running N. 24 W., which con- 
 sists of calc-spar mingled with pearl spar, and has a breadth of about nine 
 inches. Three reticulating strings of iron pyrites, with a little copper 
 pyrites, run through the vein ; and small portions of these minerals, with 
 others of blende, are observed sparingly scattered through the spar of the 
 vein. A shaft, with a breadth of about nine feet, has been sunk to a depth 
 of sixteen feet on this vein, which appears pretty uniform in character 
 throughout, and exhibits, on either side, numerous strings or leaders of an 
 inch and less in thickness, holding copper pyrites, and sometimes intersect- 
 ing, which run into the main vein. The quantity of ore in this locality 
 does not appear sufficient to warrant farther exploration ; yet the presence 
 of such a well defined metalliferous lode in this region is not without a 
 certain interest. 
 
 Among the copper-bearing veins on Lake Superior, those near the Black 
 
694 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 Lake River, which are described as cutting a stratified granitoid gneiss, com- 
 
 posed of red feldspar and vitreous quartz, are supposed to belong to the 
 
 Black River. Laurentian series. They contain in a gangue of quartz, sometimes with 
 calc-spar and fluor spar, small portions of yellow and vitreous copper ores, 
 with a little molybdenite, blende, and galena, the ktter sometimes argen- 
 tiferous. Copper-bearing veins in a granitoid rock, probably Laurentian, 
 
 Doree River, are also described as occurring on the Dore'e River, in Michipicoten Bay ; 
 but the principal copper veins at this location are in greenstone and slate, 
 supposed to be Huronian ; and the slates in which some of the copper 
 veins of the Black River region occur, are perhaps of the same age. It 
 would appear that both of these localities are at the contact of the Lau- 
 rentian and Huronian rocks. 
 
 The copper deposits of the Huronian series, and their relations to the 
 stratification, have already been described in a general way on pages 59 
 and 515. The few examples of copper veins in the rocks of this series on 
 Lake Superior, just alluded to, will be mentioned in a more detailed man- 
 ner when describing, farther on, the copper deposits of that region, which 
 belong for the greater part to more recent rocks. The most important 
 deposits of copper in this series are met with on the shores of Lake 
 Huron, where the Bruce Mines were discovered in 1846, since which time 
 ores of copper have been found there in a great many other localities. 
 Scarcely any large area throughout this region is destitute of copper- 
 bearing veins, the gangue of which is generally white quartz, sometimes 
 with pearl-spar and sulphate of barytes. None of these have, however, as 
 yet been wrought to any considerable extent, except those of the Bruce 
 Mines, and the adjoining locations. 
 
 Brace Mines. The copper-bearing veins of the Bruce Mines occur along the crown of 
 an anticlinal fold, and traverse a mass of interstratified greenstone, or 
 diorite. The veins, which are numerous and generally parallel, have a 
 gangue of quartz, occasionally mingled with pearl spar and heavy spar. 
 The ore is chiefly copper pyrites, although near the surface both the 
 vitreous and variegated sulphurets were met with. Two of the lodes have 
 been wrought, and have an average breadth of from two to four feet. The 
 proportion of ore contained in these veins is very large. From the results 
 of a careful examination made in 1848, by sampling the rough ores which 
 had been raised, and by borings into the lodes, both at the surface, and at 
 various depths down to twelve fathoms, it was computed that about 3,000 
 square fathoms of these lodes contained an average of six and a half per 
 cent, of copper. The deepest working is now at fifty fathoms from the 
 surface. The total quantity of ore raised from this mine, since its opening 
 in 1847, is stated to be about 9,400 tons of eighteen per cent. In 1861, 
 thirty-five men were employed at the mine, and 477 tons of eighteen per 
 cent, ore were raised. In 1862, the produce was 380 tons. Smelting works 
 
CHAP. XXL] COPPER ORES. 695 
 
 were at one time erected at the mine, by its proprietors, the Montreal 
 Mining Company. Bituminous coal for the purpose of fuel was brought 
 from Cleveland in Ohio, and laid down at the mine at a cost of four dollars 
 the ton. The attempt to smelt the ores on the spot was however aban- 
 doned, and they are now shipped in part to Baltimore, and in part to 
 England. 
 
 Adjoining the Bruce Mines location, to the northwest, and on the lands Wellington 
 of the Montreal Mining Company, is the Wellington Mine, which is leased Mine * 
 to the West Canada Mining Company. The veins at this point resemble 
 those of the Bruce, of which they are probably a continuation, but some- 
 times attain a width of ten feet. They are continued into the adjoining 
 location, which is known as that of Huron Copper Bay, and is worked 
 by the same company as the last. The ore obtained by this company 
 from the Wellington mine, from 1857 to 1862, is stated at a little over 
 5,700 tons, averaging twenty per cent. In 1861 this mine furnished 1,175 
 tons, and the Huron Copper Bay mine 1,300 tons. The deepest shaft at 
 the Wellington mine, in 1861, was twenty fathoms, and the number of 
 men employed was about 260. In 1862, it yielded 1277 tons of ore. 
 
 What is called the Wallace Mine is on the shore of Lake Huron, about Wallace 
 a mile to the west of the mouth of White-Fish River, and on the north Mine * 
 side of a great bay. The strata here consists of quartzose and chloritic 
 slates, dipping northward at a high angle, and including a large mass of 
 greenstone, running with the strike. Strings and bunches of copper pyrites 
 are found in some abundance, both interlaminated with the schists and 
 disseminated in the greenstone. In 1848., a shaft was sunk to a depth of 
 six feet in the chloritic schists, and a quantity of copper pyrites obtained ; 
 together with an arsenical ore of nickel, which was found in small ramify- 
 ing veins adjacent to the southern wall of the mine, and will be further 
 described in speaking of that metal. According to the report of Mr. 0. B. 
 Dibble, a vein of from six to sixteen feet in width was traced for half a 
 mile, and ten tons of copper ore were raised from the shaft. The working 
 of the mine has since been abandoned ; although the presence of a rich ore 
 of nickel should, even in the absence of large quantities of copper, encour- 
 age further trials. A mile and a half farther to the east, near the base 
 of the hills, two veins, of ten and sixteen feet, were observed, similar in 
 aspect to that of the Wallace Mine, and holding iron pyrites, with a little 
 yellow copper ore. Adjoining this location to the eastward, a second one, 
 in which were found three similar veins holding yellow copper ore, was 
 taken by the Upper Canada Mining Company, who were also the explorers 
 of the Wallace Mine. 
 
 About ten miles to the west of the mouth of the Spanish River, the 
 same company acquired another location, which embraced a portion of the 
 main land and a few islands adjacent. .One of these, to the west of the 
 
696 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 Spanish location, is said to be traversed, near its southern extremity, by five well- 
 defined quartz veins, which run in greenstone, and are from one to two and 
 a half feet in breadth. One of these contained a mixture of yellow and 
 variegated copper ores ; while in the others the vitreous ore occurs in 
 strings and grains disseminated through portions of the veins, which are 
 stained throughout by green carbonate of copper. These veins run nearly 
 eastward, showing however a slight convergence, which if continued would 
 cause them to unite in a larger island about 200 yards to the eastward. In 
 the face of this was observed a vein of quartz, four feet in breadth, run- 
 ning also east and west, and supposed to be the continuation of the veins 
 just mentioned. A mile farther to the east, on the south shore of the 
 island, a quartz vein two and a half feet wide, occurs in a cliff of forty 
 feet, containing considerable quantities of copper pyrites, and stained with 
 green carbonate. It was traced for about a quarter of a mile. Several 
 other veins, similar to these, are seen upon the islands and also upon the 
 mainland. Three of the latter were found to contain yellow copper ore* 
 Another lode is described as running northwest, with an underlie to the 
 north-east. It corresponds in dip and strike with the slates which form 
 the walls, but appears to be a true vein, and contains, in a gangue of quartz 
 and pearl spar, considerable quantities of copper pyrites. Delicate crys- 
 tals of what appears to be rutile also occur in druses hi the vein. Quartz 
 veins holding copper ore were also observed in two localities in the Riviere 
 aux Sables, about three miles back from the mouth of Spanish River. 
 
 Echo Lake. On the north side of Echo Lake, about three miles from Lake George, 
 the Huronian quartzites are seen interstratified with the slates and con- 
 glomerates of the series ; and numerous veins of quartz, from one to five 
 feet in breadth, are found cutting the strata. These veins contain yellow 
 copper ore, and more rarely the vitreous and variegated species, in a 
 gangue of quartz, sometimes with pearl spar, and it is said with carbonate 
 of iron. They are described as running nearly west, with a high dip to the 
 north, and traversing alike the chloritic slates and the quartzites of the 
 formation. Some years since an opening was made, and a few tons of ore 
 were raised ; but the working was abandoned. The vein which was 
 wrought runs nearly east and west, and has a thickness of about three 
 feet. On the east branch of the Caribou River, which traverses the 
 location and falls into Echo Lake, several other veins, from two to four 
 feet in thickness, and containing copper ore, have been observed. Another 
 vein of two feet in width, composed chiefly of pink calc-spar, is seen at the 
 eastern extremity of the bluff near the river, which flows into the east end 
 of Echo Lake ; and still another vein, holding a little yellow copper ore, 
 is described as occurring in the limestone rock at Limestone Point, on 
 this location. 
 
 A mine has been opened on Root River, by Mr. A. Rankin, on what 
 
CHAP. XXI.] COPPER ORES. 697 
 
 is called the Emerald location. Here a nearly vertical vein is described Boot River, 
 as occurring in greenstone, and running N. 75 W., apparently with the 
 strike of the rocks. Two shafts have been sunk within a distance of about 
 a hundred yards, and from each a considerable amount of yellow copper 
 ore has been raised. The western shaft, when examined, had been sunk 
 thirty feet, and presented the ore imbedded in soft greenish material, which 
 has the aspect of a chloritic slate. At a depth of seventy feet however, 
 this is said to be almost entirely replaced by quartz. The eastern shaft 
 at a depth of fifty feet showed the vein to have a breadth of more than 
 three feet, with an increase in the quantity of copper ore, the gangue of 
 which was a mixture of quartz and a chloritic substance. 
 
 Small portions of yellow copper ore are met with in many places, dissem- 
 inated in the slates, on the lower lakes of the Maskinongi ; and both there 
 and in the region around Lakes Matagamishing and Wahnapitaeping, the 
 various rocks of the Huronian series are traversed by numerous quartz 
 veins, in which iron and copper pyrites are often met with. The green- 
 stone to the north of White-Fish Lake, as already described on page 595, 
 was found to contain disseminated small portions of the sulphurets of cop- 
 per and iron, with traces of nickel, showing the distribution of these mine- 
 rals throughout the region ; and numerous quartz veins, for the most part 
 however holding only iron pyrites, were met with on the lower lake of the 
 White-Fish River. A promising copper lode is said to exist immediately 
 to the west of Shibahahnahning, but little is known with regard to it. 
 
 Indications of copper ore are met with in a great many other places 
 throughout this region, especially on the Mississagui River. Besides the 
 disseminated copper pyrites observed at various points in the greenstone, 
 the following localities have been noticed. Half a mile above the Hudson 
 Bay Company's post, granitic dykes or veins, running N. 24 E., contain 
 small portions of copper pyrites. The same ore occurs in small calcareous 
 veins, a mile below the Pakowagaming River, which run N. 70 W. ; and 
 in a vein of quartz and bitter spar, having nearly the same direction, and 
 a mile and a half above the same river. Copper pyrites occurs at the 
 second fall of the Mississagui, in a similar vein, two inches in breadth, 
 which traverses greenstone, and runs N. 50 W. At the east end of 
 Lake Wabiquekobing, the same ore occurs in a two-feet vein of quartz, 
 running N. 84 W. ; and in the north portage to the same lake, within 
 twelve or fourteen chains of the Mississagui, is a similar quartz vein, from 
 one to two feet wide, which holds yellow copper, and runs N. 15 W. Like 
 the last two, it cuts greenstone. At the fourth fall is a vein of quartz and 
 bitter spar, a foot wide, with copper pyrites. It runs N. 55 W., and is 
 in quartzite. At the upper end of the portage around this fall, the quart- 
 zite is also traversed by several quartz veins holding copper pyrites. The 
 principal one is from one to two feet in width, and runs N. 72 W. At 
 
698 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 Lake 
 Superior. 
 
 Mines of the 
 south shore. 
 
 the Grand Portage, on the Mississagui, numerous veins are met with, hav- 
 ing a general bearing of about N. 60 W. The largest, which is at the 
 foot of the portage, is from one to three feet in width, and consists of 
 quartz, stained red by scaly hematite, which also discolors the adjacent 
 greenstone. It contains strings and spots of copper pyrites. Near the 
 head of the portage a vein of bitter spar, holding copper pyrites, traverses 
 both the slate and the quartzite. Most of the principal veins here occur 
 in the greenstone, but also run into the other rocks of the series. At the 
 turn of the river, three miles above the Grand Portage, on the right bank, 
 the greenstone is intersected by a calcareous vein, two or three feet wide, 
 which holds portions of copper pyrites, and runs N. 70 W. At the 
 eighth fall of the river, several veins of quartz are seen in the slate con- 
 glomerate. The main ones have a width of from one to two feet, and run 
 from 67 to 77 N. of W. They however exhibit only traces of copper. 
 
 The copper ores of Lake Superior occur, with some few exceptions, in 
 a group of strata which are more recent than the Huronian series, and have 
 been described in the fifth chapter, as the Upper Copper-bearing rocks. 
 They are regarded as of the age of the Quebec group, being the inferior 
 portion of the Lower Silurian series ; and they are divided into two parts, both 
 of which are intersected by numerous metalliferous veins, whose general 
 characters have been noticed on page 74. These veins contain the sulphu- 
 rets of copper, associated with blende, galena, and native silver ; and more 
 rarely with ores of nickel, cobalt, uranium, molybdenum, and a little gold. 
 The most important copper deposits of this group, however, contain the 
 metal in the native state. Of this kind are the mines on the south shore 
 of Lake Superior. As described by Prof. Whitney, the native copper 
 there sometimes occurs in true veins, which cut the strata, and have a 
 gangue of quartz, calc spar, prehnite, and more rarely of datholite. These 
 veins, according to him, occur chiefly in the finer-grained and somewhat 
 amygdaloidal traps or dolerites; but they may be traced across the interca- 
 lated beds of sandstone, conglomerate, and crystalline greenstone. They 
 seldom however extend any great distance in the sandstone, where the 
 gangue is generally calcareous ; and neither in this rock nor in the crys- 
 talline greenstone are they very rich in copper. The width of the pro- 
 ductive veins is from one to three feet ; and occasionally, for short dis- 
 tances, much greater. In the Keweenaw Point region, where these veins 
 prevail, their underlie seldom varies very much from the perpendicular, 
 and their. direction is a little north of west. In some parts, however, the 
 metal is found disseminated in the beds of trap ; and more rarely, in the 
 sandstone or conglomerate. In one case, at Copper Falls, copper forms the 
 cement or matrix of a bed of conglomerate. Large and small masses of 
 native copper are met with in the trap, without any connection with a 
 vein or fissure, and sometimes unaccompanied by any vein-stone. Such 
 
CHAP. XXI.] COPPER ORES. 699 
 
 metalliferous beds of trap are common in the Ontanagan region ; and they cupriferous 
 constitute the whole, of the workable deposits of the Portage Lake district, bede ' 
 where great beds of an earthy amygdaloidal rock are found to be richly 
 impregnated with native copper for distances of a mile or more. Epidote 
 is frequently associated with the copper, both in the veins and in the amyg- 
 daloidal beds. In many cases, the copper forms what are called contact 
 deposits, between the beds of trap and those of sandstone or conglomerate. 
 These are probably, in some cases, veins segregated in fissures running 
 with the stratification ; but more frequently they belong to the same class with 
 the beds just described. Certain of the sedimentary beds thus impreg- 
 nated with native copper, are often designated as volcanic tufa or volcanic 
 ash. From whatever source derived, however, the amygdaloidal rocks Amygdaioids, 
 were deposited from water ; and the copper which is disseminated in them, 
 as well as in the sandstones and conglomerates, was separated by chemi- 
 cal processes from aqueous solutions, either contemporaneously or by 
 subsequent infiltration. There appears to be no doubt that the traps 
 which are interstratified with the sandstones and amygdaloids of this 
 region, are eruptive rocks ; and the sedimentary material of which the 
 amygdaloids and tufas are composed may perhaps have been, to a greater 
 or less extent, erupted in the form of volcanic mud, as many geologists 
 suppose. This origin of the sediment has probably, however, no connec- 
 tion with the source of the copper ; inasmuch as in the Quebec group, 
 Tifhich is regarded as the equivalent of this series, and which over great 
 areas, is destitute of intrusive rocks, the sulphurets of this metal, and even 
 native copper, are found disseminated throughout limestones, diorites, 
 slates, and quartzites. 
 
 The investigations of the copper deposits along the north shore of Lake North shore 
 Superior have been much less minute and extended than those on the ofthe lake - 
 south side. A preliminary examination of the region was however made 
 by the Geological Survey in 1846, and from that time until 1850, nume- 
 rous explorations were made, with a view to the establishment of mining 
 companies. From the results of the survey in 1846, and of a partial exa- 
 mination in 1861, together with the published reports of the early explo- 
 rations already mentioned of Messrs. Forrest Shepherd, Hadley, Cobb, 
 Bristol, Dibble, and others, as well as from notes kindly furnished by Mr. 
 J. S. Willson, who lias spent much time in exploring that region, and also 
 by Mr. Hugh R. Fletcher, now and for many years connected with the 
 mining interests of Lake Superior, the following notices of the principal 
 mineral deposits of that region have been compiled. 
 
 Beginning to the eastward, along the south shore of Bachewanung Bay, 
 is a location of the Upper Canada Mining Company, which exhibits beds 
 of amygdaloid and compact trap, with red sandstone and conglomerate. 
 The last, according to Professor Hadley, contains boulders which are 
 
TOO 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 Bachewanung 
 Bay. 
 
 Mamainsc. 
 
 Section 
 of strata. 
 
 themselves of a conglomerate rock, consisting of red, yellow, and dark 
 colored jaspers, imbedded in a uniform quartzose mass, and identical 
 with the jasper conglomerate of Lake Huron. The hills in the rear are 
 described as gneissic, with chloritic and hornblendic slates, traversed 
 by quartz veins, in which molybdenite occurs. The amygdaloidal trap 
 contains in its cells calc-spar, agate, and portions of vitreous copper ore. 
 Large veins of calc-spar are found cutting the trap and sandstone strata. 
 They however generally contain but little copper ore, which is chiefly in 
 the rock, or in small strings leading to the principal veins. A consid- 
 erable deposit of manganese ore, which will be described under its proper 
 head, occurs on this location. At the east end of the bay, and about a 
 mile from the shore, a perpendicular cliff, facing the bay, exhibits on its 
 surface great adhering masses of a quartzose veinstone, which hold spec- 
 ular iron and vitreous copper ore, and are stained with green and blue 
 carbonates of copper. At the base of the cliff is a vein eighteen inches 
 wide, holding vitreous and variegated copper ores. Small veins contain- 
 ing portions of these ores are also found on many of the streams which 
 fall into this bay, and the region may not improbably become a valuable 
 mining district. 
 
 From the north side of Sand Bay to the south side of Mica Bay, along 
 a distance of about twenty miles, bands of tufaceous rock occupy the 
 greater part of the shore line. About mid distance is the promontory of 
 Mamainse, where explorations have been made on a considerable scale by 
 the Montreal Mining Company. The following is a partial section of the 
 strata at this place, as observed, in descending order, from the northwest 
 extremity of the bay of Mamainse, inland. The dips are to the westward, 
 at from 25 to 35, and the rocks are very unevenly bedded. I. Alter- 
 nations of trap and tufa, with a bed of conglomerate sandstone, the whole 
 occupying a breadth of 300 yards. Large veins of calc-spar, quartz, and 
 laumontite occur in the trap, and sometimes hold small portions of native 
 copper and silver, with galena. Native copper is found in the vesicles of 
 an amygdaloidal bed. II. Argillo-arenaceous beds, passing in some cases 
 into a fawn-colored jaspery rock, and in other parts into mottled argilla- 
 ceous sandstone, the whole occupying a breadth of 220 yards. III. Crys- 
 talline and amygdaloidal traps, with a bed of conglomerate, occupying 
 together a breadth of 440 yards, and rising to an elevation of 300 feet ; 
 the lower parts being apparently tufaceous. This includes the workable 
 deposit of copper. IV. A very coarse syenitic conglomerate, forming, like 
 the last, a ridge, and having a breadth of 160 yards. The whole section 
 probably represents a thickness of about 2000 feet. According to Dr. 
 Dawson, to whom this description is due, the principal deposit of native 
 copper occurs in a fissure running nearly north and south, along the sum- 
 mit of the ridge of hard semi-crystalline greenstone, III. The greatest 
 
CHAP. XXI.] COPPER ORES. 701 
 
 breadth of this fissure is about six inches ; and in some parts it is nearly Native 
 filled with native copper, which occurs in a vein-stone of calc-spar and copper - 
 quartz. A shaft was sunk here to the depth of twenty-seven feet, without 
 galleries, and yielded about a ton of native copper ; the largest mass weigh- 
 ing 600 pounds. The shaft was sunk upon an excavation, which seems to 
 have been the work of some aboriginal miners. A little to the west of 
 this, the vein of native copper divides into two parts. These, like many 
 other veins along this coast, are marked by depressions or trenches, result- 
 ing, according to Dr. Dawson, from the effects of erosion by the waters of 
 the lake, at a former period, acting upon the soft materials of the veins. Ancient 
 They are often regarded as excavations of ancient miners ; but these, which workin s 8 - 
 are also frequently met with, are distinguished by being surrounded with 
 broken fragments of veinstone, along with which are occasionally found 
 stone hammers. These are merely rounded pebbles of hard rock from the 
 beach, around' which shallow grooves have been made, to hold the withes 
 used as handles. Some of these hammers measure from five to twelve 
 inches in their longest diameter. About a hundred yards from the shaft, 
 excavations have been made at the intersection of two veins, one running 
 north-west and the other north. The former is unproductive ; but the lat- 
 ter, which is six inches in width, contains small masses of variegated cop- 
 per, and a little copper pyrites, in a gangue of quartz and calc-spar. 
 About thirty yards farther to the east is another vein, running northeast, 
 and wider than the others. It is very irregular in its width ; and it contains, 
 besides the two ores just mentioned, a little native copper. At the place 
 where it has been opened, one of the walls of the vein is of amygdaloid, 
 and the other of compact trap ; indicating apparently a fault in the strata. 
 On the north side of the bay at Mamainse, a vein of calc-spar, three or 
 four feet wide, rises from the water, cutting the upturned strata, and after 
 crossing a part of the location of the Montreal Mining Company, appears 
 on the adjoining one belonging to the Quebec Mining Company, where it 
 was found by Mr. Fletcher to contain sulphurets of copper in considerable 
 quantity. On the northwest corner of this location, a vein of calc-spar 
 rises from the shallow water of the lake, and is seen on the shore cutting 
 an inclined band of conglomerate. This vein is described as containing 
 argentiferous galena and copper pyrites. On the Meredith location, belong- Meredith 
 ing to the Montreal Mining Company, three veins of calc-spar and laumon- 
 tite contained variegated copper ore and galena. The lead from the latter 
 yielded thirty ounces of silver to the ton. An open cutting, twenty feet 
 long and four wide, supposed to have been made by early French explo- 
 rers, was found upon this vein, near the lake ; and when discovered a few 
 years since, the marks of the drills were still visible upon the rock. Other 
 pits, apparently of a similar origin, were found several hundred feet to the 
 east of the cutting, on what appeared to be another small vein, in which 
 
702 GEOLOGY OF CANADA. [Cm?. XXI. 
 
 no ore could be detected: The beds of tufa in this vicinity sometimes 
 contain native copper in fine grains, and in pieces an ounce in weight. At 
 Mamainse also occurs the vein of uranium ore described on page 504. It 
 is evident, from these abundant metalliferous indications, that this locality 
 is deserving of further and careful exploration. 
 
 Pointe aux At Pouite aux Mines, eight miles to the north of Mamainse Island, several 
 interesting veins are met with ; and trials of some of them were made a 
 few years since by the Quebec Mining Company. At the base of the 
 point, according to Mr. Willson, a shaft has been sunk to the depth of 
 seventy feet, on a small vein running east and west. Its gangue consists 
 of calc-spar, with quartz and mica, containing small quantities of native 
 copper with the yellow and variegated sulphurets, and occasionally small 
 scales of native silver. About 120 fathoms north of this shaft, on the 
 pathway leading to the miners' houses, are two parallel veins, from three 
 to four feet wide, and four or five yards asunder. They exhibit, at the 
 surface, a large amount of gozzan, with some green carbonate and vitreous 
 copper ore. About half way down the point, and eighty fathoms from the 
 water, at the foot of a bluff, occurs a vein, eight or ten inches wide, which 
 contains a considerable proportion of vitreous copper ore, and zinc blende. 
 Near to the end of the point, on the south side, a similar vein is found, 
 which, in addition to blende and vitreous copper, contains small amounts 
 of copper pyrites. The ore, which is unmixed with gangue, hangs from 
 the west wall ; while an open space of four or five feet intervenes between 
 it and the east or foot wall, which is at the level of the lake. It would 
 seem probable that this space was once filled with some vein-stone, which 
 has been washed out by the waters of the lake. Some early miners, prob- 
 ably the French, had blasted out a considerable quantity of the ore from 
 this vein ; and about three tons of blende, left by them, are said to have 
 been found in the chasm. 
 
 Mica Bay. On the north side of the Pointe aux Mines, in Mica Bay, the quartzose 
 gneiss is described by Mr. Willson as being overlaid successively by a bed 
 of grey tufa, one of greenstone, and one of a reddish-brown tufa, all dip- 
 ping to the north at an angle of about fifty degrees. Between the green- 
 stone and the underlying tufa, were found rich bunches of vitreous copper 
 ore, seven or eight inches in thickness ; but on sinking to a distance of ten 
 fathoms, the ore was found sparingly diffused through a thickness of eight 
 or ten feet of the rock. A considerable sum of money was here expended 
 by the Quebec Mining Company, and a quantity of rich ore obtained. 
 Three shafts were sunk, and an adit was driven 200 feet ; but the working 
 was finally abandoned. The reddish tufa contains disseminated a small 
 amount of native copper ; but a shaft of seventy feet sunk in it, showed a 
 quantity too small to be remunerative. 
 
 Proceeding northward along the coast, at Cape Gargantua an amyg- 
 
CHAP. XXI.] COPPER ORES. 703 
 
 daloid containing native copper forms the projecting point ; and in the older 
 rocks near, small veins holding copper pyrites and vitreous ore are met 
 with. In the green slates on the east side of Michipicoten Bay, Mr. Will- 
 son mentions two interstratified beds containing small portions of yellow Bay> 
 copper ore, with iron pyrites. On the north side of Michipicoten Bay, and 
 upon the Dore River, is a location which was formerly examined by the 
 Upper Canada Mining Company. Here, on the west side of the river, is 
 seen the contact between what appears to be the Laurentian gneiss, occu- 
 pying the western part of the location, and the chloritio slate and slate 
 conglomerate of the Huronian series, interstratified with two beds of what 
 appears to be greenstone. The latter rock is traversed by numerous 
 quartz veins holding yellow copper ore, and more rarely the vitreous 
 species. The slate is much impregnated with iron pyrites ; and numerous 
 quartz veins, often of considerable size, and running in an east and west 
 direction, are seen cutting this rock, and including iron pyrites, with a 
 little yellow copper ore : others have a gangue of calc-spar. Irregular 
 quartz veins in the gneiss are found to contain a little iron and copper 
 pyrites ; and in one case, specular iron ore. The gneiss is traversed by 
 numerous trap dykes running about north and south. 
 
 The island of Michipicoten may next be noticed. On the north side of 
 this island there is a considerable mass of greenstone and amygdaloid in- Island - 
 terstratified with sandstones, the whole dipping eastwardly. Towards the 
 west end of the island, the rocks present a low surface for a breadth of 
 four or five hundred feet, and then rise into a cliff two or three hundred 
 feet in height, in which the greenstone is marked by druses containing 
 analcime and quartz. A soft amygdaloidal bed holding native copper, is Native 
 traceable for some miles along the shore, sometimes beneath the surface of c PP er - 
 the water in the bays, and again running a little distance inland. In this 
 bed in the North Bay, an attempt was made, a few years since, to work a re- 
 markable deposit of native copper and silver, which were found disseminated 
 in grains through a green hydrous silicate of nickel. The ore being Nickel and 
 stamped, the nickel, whose value was not suspected, was washed away from sUver * 
 the residue of native metals, which gave, in one trial, twelve parts of silver 
 and eighty-eight of copper. A shaft was sunk here to a depth of seventy 
 feet ; but after a considerable outlay, the working was abandoned. Nothing 
 very definite is known as to the mode of occurrence of this curious metallic 
 deposit, which is stated however to have been associated with calc-spar. From 
 the same mine were said to be obtained the specimens of mingled arseniurets 
 of nickel and copper, which, with the preceding nickeliferous ore, are 
 noticed on page 506, and again on page 737. At a point near the west end 
 of the island, and about seven miles from the working just mentioned, the 
 cupriferous stratum again appears, and fragments of the native metal are 
 scattered along the shore. Mining operations on a small scale were under- 
 
704 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 Fletcher's taken here ten years since by the Quebec Mining Company, and a shaft 
 Mine> was sunk at a little distance from the shore, by which the copper-bearing 
 beds were reached at a depth of forty-five feet. The mine is now leased 
 to Mr. Hugh R. Fletcher, who is engaged in working it, and has kindly 
 furnished the following particulars. Beneath the principal copper-bearing 
 bed, is a soft argillaceous rock known as an ash-bed, which is six feet, and 
 perhaps much more, in thickness, and is underlaid by a massive greenstone. 
 The ash-bed itself contains from one half to one per cent, of disseminated 
 metallic copper, 'which it is supposed can be economically extracted by 
 crushing and washing the soft rock. Upon this reposes the principal cop- 
 per deposit. The metal is found in a bed of greyish amygdaloid of from eight 
 to eighteen inches in thickness, and an overlying bed of sandstone of from 
 twelve to twenty-four inches ; the united thickness of the two being on an 
 average about three feet. The proportion of copper is the same in the two 
 rocks, and averages two and a half per cent. The copper is in larger grains 
 in the amygdaloid, and is sometimes surrounded by calc-spar ; while in the 
 quartzose sandstone, it is in fine particles, or in filaments. Small specimens 
 of the sandstone are occasionally found containing ten or fifteen per cent, 
 of copper. This bed is overlaid by a massive compact greenstone, to which 
 succeed amygdaloid and conglomerate. The dip of the copper-bearing 
 stratum is about three feet in a fathom. Three shafts have been sunk 
 upon it, one to sixteen fathoms, one to twelve and a half, and a third to 
 eight and a half fathoms. From 300 to 400 tons of two and a half per 
 cent, ore have been raised ; and in the spring of 1863 it is proposed 
 commence operations on a larger scale, with proper machinery. Small 
 portions of native silver and of vitreous copper ore have been found in this 
 vicinity ; and according to Mr. Willson, native copper occurs in a second 
 band of amygdaloid about a mile and a half south of Mr. Fletcher's mine, 
 and 200 feet above the surface of the lake. Vitreous copper ore is also 
 found with calc-spar and sulphate of barytes on the eastern extremity of th "> 
 island, in a reddish porphyritic rock, near which occurs a pitchstonc 
 porphyry, and pitchstone with veins of agate. 
 
 On the mainland to the north of the west end of Michipicoten Island is 
 a location of the Upper Canada Mining Company, the southwestern cornei* 
 of which is on the shore of Lake Superior, in longitude 85 49' W. 
 Rocks which appear to belong to the Huronian series extend along this 
 Near otter coast from Otter Head, which is about ten miles west of this location, 
 to some distance to the east. Dykes of granite and trap are said to 
 intersect the slates ; and along the whole extent, veins of calc-spar and 
 quartz are frequently met with, but are most abundant and rich in 
 ores at the location just named. The veins are described as of two 
 classes. The one runs east and west, parallel to the dykes of trap, 
 and holds iron pyrites, with a little yellow copper, in a gangue of 
 
 Head. 
 
CHAP. XXL] COPPER ORES, 705 
 
 quartz. The veins of the second class, running north and south, are 
 divided by the trap dykes, generally with but slight dislocations. These 
 veins are very numerous and well defined, and three among them have 
 a width of ten feet. They contain, in a gangue of quartz and calc-spar, a 
 great variety of ores. Besides yellow and vitreous sulphurets of copper, 
 iron pyrites, blende, and galena were met with, and in one vein, molybden- 
 ite. The galena is said to be somewhat argentiferous. The above descrip- 
 tion is taken from the reports of Messrs. Cobb and Hadley. 
 
 A locality is mentioned by Mr. Willson, in a shallow bay along the coast 
 in this vicinity, where several well-defined veins are observed to radiate 
 from a point, which is distant about a hundred feet from the shore, and in 
 shallow water. Three of these veins run to the shore. The first vein is 
 about eighteen inches wide ; and, in a gangue of calc-spar and quartz, it holds 
 a considerable quantity of blende, with copper pyrites. The second vein, of 
 calc-spar, is ten feet wide, but exhibits no metallic ores. The third, which 
 runs in a north and south course, directly inland, is from five to six feet 
 wide. The vein-stone near the water is calc-spar ; which, in ascending the 
 hill, is replaced by quartz. In the shoal water, the vein contains variegated 
 and yellow copper ores, with blende and galena. A few feet above the 
 water the copper disappears ; a little higher up, the galena ; and finally, the 
 blende : so 'that before reaching the top of the hill, which is not more than 
 forty feet above the lake, the vein appears destitute of metallic ores. 
 
 Farther to the northwest occur the Slate Islands, which are described siate Wands. 
 as affording roofing slates, white satiny talcoid schists, and a pale green 
 amorphous epidote rock ; all of which recall the strata of the Quebec group. 
 On the shore to the north-east, at Ance a la Bouteille, well-characterized 
 mica schists and roofing slates are said to occur. About five miles to the 
 northwest of this place is a location belonging to the Upper Canada Min- 
 ing Company, which includes the mouth of the Black River, and is joined Bljwk Kiver 
 on the west by a second location, belonging to the same company, and 
 including a part of Terrace Bay. The rock of the first of these is de- 
 scribed as granitic gneiss, with slates and greenstone ; and presents along 
 the lake a great number of metalliferous veins, remarkable for regularity 
 and persistence in width and direction. Near the centre of the front are 
 two veins, of twenty-five and thirty feet, in gneiss ; in one of which, por- 
 tions of copper pyrites and blende were found in a breadth of two feet, 
 near the centre of the veins. These veins are said to have been traced 
 about two miles, and to appear in the river bluffs. Several veins holding 
 purple fluor-spar are also noticed as being equally continuous ; and numer- 
 ous small veins along the lake and the river were observed, holding yellow 
 and vitreous copper ores. 
 
 The adjoining location to the west is described as consisting of red feld- 
 spathic gneiss, traversed by large dykes of black trap, and intersected by 
 
 uu 
 
706 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXL 
 
 Terrace 
 Bay. 
 
 St. Ignace 
 Island. 
 
 Native 
 copper. 
 
 two sets of veins. One of these appears to occupy the joints of the rock, 
 dipping at a high angle to the northward. These veins are from one to 
 three or four inches in breadth ; and they carry, in a gangue of quartz, con- 
 siderable quantities of yellow and vitreous copper ores, with molybdenite. 
 One vein is however described as having a breadth of eight inches, and as 
 having been traced N. 15 E. for a mile and a half, bearing a considerable 
 amount of yellow copper ore, with molybdenite. The other veins are de- 
 scribed as running from the shore to a considerable distance inland, and as 
 in many cases remarkable for a breadth of from ten to thirty feet : others 
 attain but a few inches. The gangue of this series of veins is quartz, con- 
 taining copper pyrites, with occasionally a little galena and blende. In the 
 larger veins, calc-spar and purple fluor spar were observed. These how- 
 ever were less rich in ore than the smaller ones. 
 
 The next region to be mentioned is the island of St. Ignace, to the south 
 of Neepigon Bay, with the mainland to the west, and Simpson's Island to 
 the east. Here, in 1846, explorations were made, and numerous locations 
 taken up by the Montreal Mining Company. Instead of the older rocks 
 of Laurentian and Huronian age, which occur in the vicinity of the Black 
 River, the Upper Copper-bearing series is met with, with its sandstones, 
 greenstones, and amygdaloids, as on the south shore, and at Michipicoten 
 Island and Mamainse. The strata are intersected by dykes of trap (see 
 pages 72 and 78). At the eastern extremity of St. Ignace Island, on 
 the Chenal Ecarte*, copper occurs in a vein cutting a thick mass of amyg- 
 daloidal trap, which lies conformably to the strata, here dipping south 
 at an angle of nine degrees. The vein, which has an underlie of seventy 
 degrees to the north, is four or five inches wide, and holds masses of native 
 copper, occasionally more than one hundred pounds in weight, in a gangue 
 of calc-spar, sometimes with native silver. About forty-seven feet to the 
 south of this vein, is another about twelve inches wide, of which the vein- 
 stone is calc-spar, with a little quartz, including fragments of the wall- 
 rock, and holding imbedded masses of vitreous copper ore, with native 
 silver. The underlie of this vein is sixty degrees to the north, so that 
 it should meet the former one at a depth of about twenty-five fathoms. In 
 1846, the Montreal Mining Company, to whom this location belongs, sunk 
 a shaft about twenty-four feet, to the north of the vein of native copper, 
 to the depth of ten fathoms. A drift to the southward then intersected 
 the vein at a distance of about twenty feet, thus showing its continuance 
 to a depth of ten fathoms. Having however directed their whole attenr 
 tion to the Bruce Mine, the company abandoned this working. The veins 
 just described can be traced to the westward for nine miles, along the whole 
 length of St. Ignace Island ; carrying native copper and silver, with the 
 vitreous sulphuret of copper, in greater or less quantity, the whole distance. 
 Crossing Neepigon Strait, the same minerals are met with at two locations 
 
CHIP. XXI.] % COPPER ORES. 707 
 
 on the mainland opposite. Fluor Island, at the southern extremity of the Fluor island. 
 Strait, consists of the same rock as the adjoining country ; and it is traversed 
 by numerous veins, in which vitreous copper ore has been found. It 
 receives its name from the fluor spar which is said to abound in these veins. 
 To the eastward of St. Ignace, the copper-bearing strata are traced across 
 to Simpson's Island ; where the vitreous and yellow ores, with native cop- gimpson'8 
 per, have been found in several localities. The latter is often associated Island - 
 with laumontite, or imbedded in prehnite. These minerals, together with 
 agates, are common in the amygdaloid, which is here interstratified with 
 sandstone. Native copper has also been found on the Battle Islands. 
 Specimens of the native copper from St. Ignace, and from the mainland 
 opposite, gave, in several assays, from one fourth to one fifth of one per 
 cent, of silver. In other specimens from the same region, the quantity of 
 salver was scarcely appreciable. It exists in the native state, and is irregu- 
 larly distributed. Metallic silver likewise sometimes occurs in grains with 
 the sulphurets of copper from this region. 
 
 Proceeding southwestwardly along the coast to Point Porphyry, at the Point 
 entrance to Black Bay, is a mining location, which includes several small 
 islands, the largest of which is known as Edward's Island. Here the 
 amygdaloidal rocks are described as being traversed by numerous brec- 
 ciated veins, containing yellow, variegated, and vitreous copper ores, in a 
 gangue of quartz, calc-spar, and sulphate of barytes. Besides these, are 
 veins of calc-spar, which are sometimes seven or eight feet in thickness, and 
 often contain vitreous copper ore. Native copper is also met with here. 
 The veins appear to be most developed on the west side of Edward's Edward's 
 Island. Another location in this vicinity includes the coast and the adja- s ind ' 
 cent islands, lying immediately to the northeast of Thunder Cape. ' Sev- Thunder 
 eral metalliferous veins are said to have been observed on these islands ; Cape> 
 and among them is a very prominent lode, holding galena and green car- 
 bonate of copper, which crosses a long narrow island near the shore. A 
 valuable deposit of limestone occurs interstratified with sandstone in the 
 northern part of this location. 
 
 Metalliferous veins are observed in various localities along the shores of Thunder 
 Thunder Bay. One of these, which is noticed on page 76, is co- Bay * 
 incident with the stratification, and has a breadth of sixty feet. In a 
 gangue of amethystine quartz, calc-spar, and sulphate of barytes, it contains 
 small quantities of iron and copper pyrites, with blende and galena. To 
 the southwest of the mouth of the Kaministiquia, several mining locations 
 have been taken along the coast. ' The most interesting of these is that 
 known as Prince's Mine, where there occurs a remarkable metalliferous 
 vein, which is seen both on the mainland, and on Spar Island opposite. 
 On the south side of this island the vein has a breadth of fourteen 
 and a half feet ; and from its whiteness, it contrasts strongly with the 
 
708 GEOLOGY OF CANADA, [CsAP. 
 
 Prince's wall-rock, which is a dark-colored slate holding cone-in-cone. Its course 
 
 Mine. Is about N. 32 W. The greater part of the vein is here occupied by a 
 
 coarsely crystalline calc-spar ; but near the middle are two bands, each of 
 about twelve inches, the one composed of heavy-spar, and the other of 
 quartz, mixed with calc-spar. Between these, is a band of six inches of 
 calc-spar, which is the only metalliferous part of the lode, and contains 
 small quantities of yellow and variegated copper ores, with native silver. 
 Two shafts, one of twenty-four, and the other of forty-seven feet, were 
 sunk here. On the mainland, about two miles distant, and a little way 
 back from the shore, the vein re-appears, somewhat split up ; but a 
 few rods farther to the northwest the parts re-unite, and the vein is 
 wider than on the island, and more quartzose, affording fine specimens 
 of amethyst. It here contains small quantities of variegated and vit- 
 reous sulphurets of copper, with blende, and some native silver. A level 
 copper. was driven 165 feet in this vein ; and at one place, in sinking a shaft 
 of ninety feet, a bunch of several hundred pounds of ore was met with, 
 which contained native silver disseminated in thin laminae through the cal- 
 careous spar and blende. This mass yielded, on an average, three and a 
 half parts of silver for one hundred of the rock. The silver, in one 
 assay, yielded an amount of gold equal to one part in seven thousand, 
 but is said in another sample to have given nearly eight parts of gold 
 to one thousand of silver. This mass of rich ore was soon exhausted. 
 Crystallized sulphuret of silver was also found in this vein ; and the calcar- 
 eous spar was stained with blue and green carbonates of copper, and 
 with red arseniate of cobalt. Some farther explorations were attempted 
 after the discovery of this silver, but without success ; and the mine 
 has since been abandoned, although the characters of the lode are cer- 
 tainly such as should encourage farther working for silver, if not as a 
 copper mine. Adjoining this location to the westward, is another in which 
 the slates are intersected by large veins of calc-spar, sometimes associ- 
 ated with quartz, fluor-spar, and sulphate of barytes, and holding yellow 
 pigeon BiTr. and vitreous copper ores. At the mouth of Pigeon River is another loca- 
 tion, where numerous veins holding yellow and vitreous copper ores are 
 met with, sometimes associated with blende. 
 
 Kamanis- The argillaceous slates on the Kamanistiquia River are traversed by 
 
 tiquia. numerous mineral veins, some of which have a course to the north of 
 east, while others have a transverse direction. They vary from a few 
 inches to two or three feet in thickness, and usually contain a breccia of 
 the wall-rock cemented by calc-spar, together with quartz, sometimes 
 amethystine, heavy spar, and occasionally purple fluor spar. Blende, 
 galena, copper ores, and iron pyrites are met with in these veins. 
 
 In Eastern Canada the rocks of the Quebec group, which is regarded 
 as the equivalent of the Upper Copper-bearing strata of Lake Superior, 
 
CHAP. XXL] COPPER ORES. 709 
 
 constitute an important metalliferous region, in which numerous deposits 
 of copper ore occur. The characters and distribution of this group have 
 already been described with considerable detail in the eleventh chapter of 
 this volume, while the chemical and mineralogical history of its constituent 
 rocks will be found on pages 598-618. To render more intelligible the 
 order which will be followed in describing the copper deposits of this 
 region, it may be well to recall the principal facts relative to the geogra- 
 phical distribution of this series of rocks. The Quebec group, with the Quebec 
 exception of a small portion on the north shore, between Cape Rouge and group * 
 Quebec, and the greater part of the island of Orleans, is entirely confined 
 to the south side of the St. Lawrence ; where its northwestern limit may 
 be nearly defined by a line running from the northern extremity of Mis- 
 sisquoi Bay to Cape Rouge. This boundary corresponds to the great 
 dislocation, which has been described on page 233 as bringing up this 
 lower group to overlie, along their southeastern border, the newer forma- 
 tions belonging to the upper portion of the Lower Silurian series. The 
 southeastern limit of the Quebec group in Canada is the band of slates and 
 limestones of Upper Silurian and Devonian age, which, starting from 
 Stanstead, passes to the east of Lake Massawippi, thence along the river 
 St. Francis to the lake of that name. From this the southern boundary 
 of the group is traced to Vaudreuil, on the Chaudire ; thence to the 
 northern part of Lake Temiscouata ; and following closely the province 
 line, to Lake Metis. The Quebec group thence stretches eastward, 
 including the Shickshock Mountains, to the extremity of the continent 
 at Cape Rosier. 
 
 This long belt of rocks thus defined attains its greatest breadth, which 
 is about sixty miles, on the Chaudidre ; while near Rimouski, in one place 
 it is not more than seven miles wide. It is a continuation of the Green 
 Mountains of Vermont, and includes in Canada the Shickshock and Notre structure. 
 Dame Mountains. The strata of this region, which include both the Que- 
 bec group and some dark colored slates supposed to underlie it, are, from 
 the effect of undulations, arranged in long narrow parallel synclinal and 
 anticlinal forms, with many overturn dips. The latter circumstance renders 
 it difficult to determine which of these folds are synclinal, and which 
 anticlinal, inasmuch as the outcrop in both cases present a similar arrange- 
 ment. The weight of evidence, however, at present, goes to show that 
 the strata dip toward the centre of the areas about to be described, and 
 they will therefore be designated as synclinals. These, in the part of the 
 region which has been most examined (extending from the boundary 
 line of Vermont to the Chaudidre River) , are three in number ; and although 
 they are described at length in the eleventh chapter, they may be briefly 
 defined as follows : 
 
 I. The synclinal extending from the township of Farnham, near Missis- 
 quoi Bay, to the seigniory of Lauzon, on the St. Lawrence. This, where it 
 
710 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. XXI. 
 
 Second 
 synclinal. 
 
 Thirdl 
 
 synclinal . 
 
 is traversed by the St. Francis, is nearly or quite separated into two parts, 
 by the appearance of the underlying slates. The southwestern portion 
 appears to be divided by an undulation into at least two subordinate 
 troughs, thus giving in Roxton and Ely an additional breadth to the expo- 
 sure of these rocks. The copper deposits of Upton, Acton, Wickham, 
 Roxton, and Durham occur in this synclinal ; while in its northeastern 
 extension are those of Wendover, Somerset, Nelson, and St. Flavien. 
 
 II. The second synclinal extends from St. Armand to the seigniory of 
 St. Mary, on the Chaudiere. In it are the copper deposits of Sutton, 
 Shefford, Stukley, Melbourne, Cleveland, Shipton, Halifax, Leeds, Inver- 
 ness, and St. Mary. In its southern extremity this synclinal is divided 
 into two by Sutton Mountain ; and while one part occupies Sutton valley, 
 the other extends southward into Potton. 
 
 III. Farther to the southeastward is the third synclinal, extending from 
 the Owl's Head Mountain, on Lake Memphremagog, to Ham, and includes 
 the Stoke Mountains. An extension of this is traced northeastward to 
 Vaudreuil and St. Joseph, on the Chaudiere ; and beyond it, into Buckland. 
 Between the southwestern portion of this synclinal and the second one, is 
 a large area occupied by newer rocks, of the same age as those which limit 
 the belt to the southeast. They include the slates and limestones which 
 occupy the northern part of Lake Memphremagog, and, extending through 
 parts of Orford and Brompton, cover a considerable area in the contig- 
 uous parts of the townships of Windsor, Wotton, Ham, and Stoke. These 
 unconformable rocks overlie and conceal a large portion of the strata of 
 the third synclinal ; but along the eastern limit of this are exposed the 
 copper deposits of Ascot, Ham, and Garthby. 
 
 The contour of these synclinal areas is very irregular, and they vary 
 considerably in breadth in different parts of their extension. Their struc- 
 ture is such, that the strata which dip down on one side come up again on 
 the other side of the basin ; and they may also be repeated in the interme- 
 diate portions by subordinate undulations. The copper is confined to cer- 
 tain beds in the series ; so that it becomes of great importance to trace out 
 the undulations of the region, which govern the distribution of the metal- 
 liferous deposits. Various other important mineral products accompany 
 the copper-bearing strata. Such are the iron slates of this region, already 
 described on page 679, which are chiefly found among the altered rocks 
 of the second synclinal. The serpentine,, steatite, and magnesite, with 
 their associated chromic iron and nickel, belong also to a portion of the 
 series near to the copper, and have a similar distribution. Besides the newer 
 unconformable rocks above mentioned, the accumulations of sand and gravel 
 in many parts conceal the outcrop of the copper-bearing strata. It should 
 however be remarked, that these newer rocks are not destitute of metals ; 
 but in some places they are cut by metalliferous veins, containing argeixtife- 
 
CHAP. XXI.] COPPER ORES. 711 
 
 rous galena, blende, and native gold, as at Potton, Ascot, an)d Vaudreuil, 
 localities which have already been noticed under the head of Lead. At 
 Barford also, they contain copper ore in well-defined lodes ; which will be 
 described farther on. 
 
 The copper of the Quebec group occurs chiefly in interstratified beds, copper- 
 These are often in the limestones of the series, which are generally mag- 
 nesian ; and are frequently associated with serpentines and diorites, both 
 of which also sometimes contain copper. These rocks are accompanied by 
 slates, which in many localities are themselves the copper-bearing strata ; 
 and in certain parts of their distribution are so much altered as to take the 
 form of chloritic or micaceous schists. The latter are sometimes soft, with 
 a pearly lustre, and are called nacreous or talcoid slates. At other times 
 they are highly silicious, so that the copper-bearing bed is occasionally a 
 micaceous quartzite. Beds of a true talc-slate or steatite also sometimes 
 contain copper ; and the metal is also found in the red and green argillites 
 of the series. The chloritic schist is occasionally calcareous, and passes 
 into an impure limestone. The great mass of the chloritic rocks is sup- 
 posed to overlie the magnesian limestone of the series ; but chloritic schists 
 also to occur beneath it. 
 
 The metal throughout these various rocks is generally in the form of the 
 yellow, variegated, or vitreous sulphuret. The blue and green carbonates 
 of copper, and the red oxyd, are only met with in small quantities, and 
 near to the surface. The native metal, which is so abundant in the rocks of 
 this group on Lake Superior, is rare in Eastern Canada. It is however 
 sometimes seen in the red slates ; and at St. Flavien it occurs with calc- 
 spar in an amygdaloidal rock, under conditions which resemble closely 
 those of the western region. 
 
 In many parts of the country, the copper-bearing beds are traversed copper ores, 
 by quartz veins ; but these are often destitute of metal. In other districts 
 they carry large quantities of very rich ore, in a gangue of quartz or of 
 bitter spar, more rarely with orthoclase. The ores of these veins are the 
 yellow, variegated, and vitreous sulphurets. At Harvey's Hill, however, 
 a dark steel-grey foliated ore, with a black streak, has recently been met 
 with, which is a sulpharseniuret of copper and iron, with a trace of zinc, 
 and may belong to the rare species enargite. Sulphuret of molybdenum, 
 specular iron, and native gold have also been met with in these veins, or 
 courses, as they are locally called. They are seldom continuous for great 
 distances ; and the most reliable source of copper in this region has hitherto 
 been found in the beds. The relations of the two will be readily under- 
 stood from the plans and description of the Harvey Hill mine, to be given 
 farther on. The copper in the slaty beds generally occurs in disseminated 
 grains, or in thin, irregular, and interrupted layers. In some cases, as in 
 Button and Melbourne, beds of a dark colored slate occur, in which the sul- 
 
712 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 phuret of copper is so finely divided as to be visible only on minute inspec- 
 tion, and which nevertheless contains from five to ten per cent, of copper. 
 In the magnesian limestones or dolomites, a schistose structure is sometimes 
 seen, and the copper is occasionally arranged as in the slates ; but more 
 often these dolomites are massive, and the ore is found in nodules, or is 
 irregularly intermingled with the substances of the rock. In these rocks 
 however, as well as in the more schistose strata, veins often occur, in 
 which the copper ores appear to be concentrated, generally in a gangue 
 of calc-spar, and occasionally with quartz. Sometimes, as in Acton, the 
 sulphurets of copper form the cement of a limestone breccia or conglome- 
 rate. Many other peculiarities connected with the occurrence of the ores 
 will be mentioned in describing diiferent localities, and other facts will 
 be found on page 515. 
 
 In describing the various copper deposits of this region, it is proposed 
 to follow the three synclinals just enumerated, beginning with each at its 
 southwestern extremity, and proceeding towards the northeast. On the 
 eastern margin of the Farnham and Lauzon synclinal, small portions of 
 copper pyrites and of galena have been observed in a quartz vein, cutting 
 chloritic slate, on the eighth lot of the eighth range of Granby. On 
 the western border of this synclinal, small portions of vitreous copper 
 ore are found in the red slates in Milton; but copper first appears 
 Upton * n considerable quantity in Upton. It here occurs in the magnesian lime- 
 stone or dolomite of the series, which in this portion of the synclinal has a 
 thickness of from 200 to 300 feet. It is somewhat crystalline ; and is divided 
 into massive beds, which often contain chert. The upper portion of this 
 limestone often presents a brecciated or conglomerate character ; and it con- 
 sists of rounded or irregular masses of limestone intermixed with irregular 
 fragments of chert, the whole re-cemented. This structure may in some 
 cases have resulted from the breaking up and re-aggregation of previously 
 formed conglomerates, such as are common in this group, as may be seen 
 in the section on page 227. It is chiefly in this upper portion of the lime- 
 stone that the copper ores most abound. The copper of Upton was first 
 described and reported upon by the Survey in 1847 (and again in 1849), 
 when an assay of the ore was given, and the place recommended for a 
 crop trial. These early examinations at Upton were made on the fifty- 
 first lot of the twenty-first range. On this two shafts have since been sunk 
 in the limestone, to the depths of twenty-five and forty-two feet. Good spe- 
 cimens of ore were obtained from these ; but the working is for the present 
 suspended. Within about one hundred feet from one of these excavations, 
 explorations have, been made for copper on the fifty-first lot of the twen- 
 tieth range, in what is called the Prince of Wales mine. Here about 
 twenty feet of the upper portion of the limestone band contain copper 
 pyrites, which is most abundant in the lower part of this thickness. In 
 
CHAP. XXL] COPPER ORES. 713 
 
 some places bunches of pure ore, eight or ten inches in thickness, are met Prince oi 
 with. The bed is intersected with reticulating veins or strings, which also 
 hold yellow copper ore, with calc-spar and quartz, sometimes with 
 small portions of the blue carbonate. Copper pyrites is also found in 
 shales which here accompany the dolomite. The only working of this 
 mine has hitherto been by an open cut, which was carried to a depth 
 of forty and a width of thirty feet. According to Mr. Robb, about 900 
 tons of rock, holding more or less copper, have been excavated. This has 
 been sorted, and a considerable quantity of ore got ready for the market, 
 estimated hi all at forty tons, yielding twelve and a half per cent, of cop- 
 per. One lot of fifteen tons gave to his assay fourteen and three quarters 
 per cent. The value of this ore is much more than is required to pay the 
 whole expense of mining and dressing ; besides which, there remains a large 
 quantity of rock, less rich in copper, which requires machinery for stamp- 
 ing and washing. 
 
 The limestone band in this vicinity is sometimes associated with red 
 slates ; and it occasionally takes the form of a breccia, in which yellow copper 
 ore appears to enter into the cement. It is traced to the northeastward 
 for nearly a mile ; when it is carried half a mile to the northwest, appa- 
 rently by a dislocation. Here, on the forty-ninth lot of the twentieth 
 
 A TV L > TVT- -j. v J T-- i Bissonette's 
 
 range, at Bissonette s Mine, copper pyrites again appears in a bed, which Mine . 
 seems, as before, to be at the top of the limestone. The bed is about 
 three and a half feet thick ; and the ore lies in disseminated masses of vari- 
 ous sizes, up to twenty inches long by six and nine inches thick. It may 
 probably yield from ten to fifteen hundred-weight of ten per cent, ore to 
 the fathom. Yellow copper ore has also been found in limestone on the 
 fourteenth lot of the twentieth range of Upton, and variegated ore on the 
 twenty-sixth or twenty-seventh lot of the twelfth range of Wickham. 
 
 These localities are all on the west side of the supposed synclinal. About 
 six miles to the southeast, the limestone re-appears in Acton ; where at the 
 Acton vale mine, which is on the thirty-second lot of the third range, it is 
 seen dipping to the northwest at an angle of from 35 to 40. The hill 
 to the southeast of the mine is composed of the massive beds which, as 
 already mentioned, make up the lower portion of the band. The copper- 
 bearing limestone overlies this, and occurs in irregular elongated masses, 
 running parallel with the great body of the limestone beneath, but variable 
 both in thickness and texture. As may be seen in the section given below, 
 it is interstratified with portions which are nearly destitute of copper. 
 This upper limestone, at the mine, is underlaid by shales, which contain 
 more or less copper ore, and are sometimes interstratified to a small extent 
 with the limestone. With these shales also occur masses and beds of 
 greenstone or diorite, whose description and analysis have been given on 
 page 604. This rock has an olive-green color, with darker spots, and 
 
714 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXL 
 
 Section at 
 Acton Vale. 
 
 Diorite. weathers of a yellowish-brown, resembling many of the serpentines of the 
 region. Some masses of the diorite seen at the Acton mine are one hun- 
 dred and fifty feet in length by thirty feet in thickness ; but thin layers of 
 it are occasionally interstratified with the slates. In some portions of this 
 diorite, masses of calc-spar are disseminated, giving it the characters of an 
 amygdaloid, and, on the weathered surfaces, a cellular aspect. At other 
 times it appears to be a conglomerate, with small pebbles running in the 
 direction of the bedding, which is in some cases very apparent in this rock. 
 Diorites similar in character to that of Acton, and occupying the same 
 stratigraphical position, occur with the copper-bearing limestones in Upton, 
 Wickham, Somerset, Nelson, and St. Flavien ; and the fact that at the 
 latter place, and at Drummondville, they are found to contain copper ore, 
 gives to these rocks an economic importance. 
 
 The following descending section of the copper-bearing strata at Acton 
 was obtained in an early surface cutting at right angles to the strike, made 
 at the mine. The measurements of the beds are reduced to the vertical 
 thickness. 
 
 Feet. 
 
 1. Limestone partially concealed, enclosing small portions 
 
 of copper pyrites, 8 
 
 2. Aggregations of angular fragments of limestone and 
 variegated copper ore, dipping with the stratification, 
 but terminating- in a wedge below, 2 
 
 3. Brecciated limestone, in which fissures, from a quarter 
 of an inch to three inches wide, are filled with variega- 
 ted copper ore, calc-spar, and quartz crystals, 15 
 
 4. Aggregations of fragments of limestone and chert, both 
 rounded and angular, united by a paste of variegated 
 and vitreous copper ores, mingled with silicious matter. 
 The sulphurets were seen, on polished surfaces, to run in 
 more or less parallel bands through the matrix, 4 
 
 5. Limestone, 2 
 
 6. Breccia or conglomerate, like 4, 4 
 
 7. Limestone, 3 
 
 8. Slate, with green stains of copper 12 
 
 9. Fin-egrained diorite, 14 
 
 10. Slate, like 8, 4 
 
 11. Concealed to the underlying limestone, 25 
 
 93 
 
 shales. The limestone of the above section is overlaid by a considerable thick- 
 
 ness of black shales, containing small quantities of copper pyrites, which 
 often fills little veins, and are sometimes stained with red oxyd of copper. 
 These overlying shales, three or four miles to the northward, contain 
 numerous and well-preserved fucoids (page 244). Masses of the diorite 
 are sometimes found above, as well as below the copper-bearing limestone ; 
 which in the above section is shown to have an aggregate thickness 
 
CHAP. XXL] COPPER ORES. 715 
 
 of thirty-eight feet. This, however, as will be seen in the succeeding 
 description, is subject to great variations ; being sometimes reduced to a 
 few feet, or even a few inches. Portions of a cupriferous slate are some- 
 times interlaminated with the base of the limestone, and with the under- 
 lying diorite. 
 
 Several faults or dislocations, not however of great magnitude, are Faults 
 found to cut the strata at this locality. Some of them appear to run with 
 the strike ; and others in two parallel series, oblique to the strata and to 
 one another. These disturb the regular continuity of the copper-bearing 
 limestone, producing apparent undulations in the dip, and causing the dio- 
 rite and the upper portions of the limestone to protrude into the ore-bearing 
 beds, or to interrupt them. The underlying limestone at this mine is 
 intersected by quartz veins, which occasionally hold small portions of galena 
 and of copper pyrites; but the workable ore of copper is found hi 
 the conglomerate already described, of which it sometimes forms the 
 cement ; or in portions of limestone highly charged with sulphuret of cop- 
 per, which occur in the immediate vicinity of the conglomerate masses, 
 and partially surrounding them. The limestone is often cut by short 
 irregular veins, holding the sulphurets of copper mixed with calc-spar ; veins, 
 and sometimes enclosing small masses of the black carbonaceous matter, 
 whose description and analysis have been given on page 525. The ores 
 which have been wrought up to the present time were found concentrated 
 in three large masses, occurring in a length of about 120 fathoms. These 
 may belong to one continuous stratum which has been divided by dislo- 
 cations, or may have been originally distinct. 
 
 Of these masses, the most northern one, beginning with a breadth of a 
 few inches, gradually extended, in a distance of about forty fathoms along 
 the surface, to forty-five feet. Upon this a long open working, known as 
 Flowers's Pit, was made to a depth of twenty feet, at which the limestone 
 was reduced to a breadth of four feet. In the northeast part of this open 
 working, a shaft, designated as No. 5, was then sunk down the incline of 
 the limestone, (which here dips at from 70 to 80,) to a depth of ninety-one 
 feet from the surface ; where the bed was twenty-four feet in breadth, but 
 poor in copper. At fifty-four feet, however, where it was ten feet wide, it 
 was a conglomerate rich in ore. At a depth of sixty feet a gallery was car- 
 ried thirty feet to the westward, where the limestone, which was sixteen feet 
 in thickness, was cut off by the overlying shale. At the southwest end of 
 the open working, and about 150 feet from the last shaft, a second one 
 was sunk seventy-five feet on the incline of the bed. For the first twenty- 
 five feet the rock was rich in copper ; and by subsequent drifting and stop- 
 ing, a large quantity of ore was obtained near this shaft, from the upper 
 part of the bed, which had a thickness of from fifteen to twenty feet. 
 
 A little to the south of this last shaft the beds appear to be thrown about 
 
716 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 Harvey's 
 
 Produce 
 of mine. 
 
 a hundred feet obliquely to the westward, by one or more dislocations ; and 
 the cupriferous limestone next appears in Harvey's Pit, which is an open 
 working about one hundred feet long, fifty-six deep, and eighty feet across 
 the strike. This great breadth at the surface is probably the result of a 
 fold, since it becomes much narrower in descending. This working is now 
 abandoned, and employed as a reservoir for water ; although still exhibiting 
 ore at the west end, and also in the middle, at the deepest point. To the 
 southwest of this pit masses of diorite afford evidence of a fold or a dislo- 
 cation ; and beyond this are Williams's and Pike's Pits, now thrown into 
 one by the removal of the barrier of rock which divided them, and 
 both excavated to a depth of sixty-five feet. In the former of these the 
 limestone occupies a breadth of from 135 to 150 feet, corresponding 
 to a vertical thickness of about seventy-five feet. This great breadth 
 is ascribed by Mr. Macfarlane to a folding in the strata. Great quan- 
 tities of a rich copper conglomerate were found in the upper part of this 
 pit ; but at a depth of forty feet, the ore occurred in more solid masses in 
 the limestone. A little to the west of this open working a shaft was sunk 
 seventy-eight feet, through the upper shale into the limestone beneath ; at 
 which depth a drift was carried forty-two feet to the overlying rock, and 
 sixty feet to the underlying rock or foot-wall. This which was partially 
 cut through, and found to consist of alternating layers of diorite, and of a 
 shale holding copper pyrites was followed by a gallery for twenty-seven 
 feet, The drift had been carried, not across the strike, but nearly with it. 
 It was however continued for sixty feet farther in the same direction, keep- 
 ing between the shaly diorite and the cupriferous limestone, and then sixty- 
 three feet farther, ascending the slope of the foot-wall, which dipped to 
 the northwest about 40. This drift had been carried beneath the cupri- 
 ferous limestone ; and on sinking a shaft in the middle of Pike's Pit, it was 
 met below a deposit of rich ore-bearing rock, which was underlaid by a 
 few feet of barren limestone. The drift near this shaft was then widened, 
 and its roof removed ; and the overlying cupriferous limestone, which was 
 thus exposed, has recently yielded large quantities of rich ore. 
 
 In preparing the above description, many details are taken from an 
 account of the mine prepared at the end of October, 1862, by Mr. Thomas 
 Macfarlane, the manager of the mine, and published hi TJie Canadian 
 Naturalist, vol. vii, page 447. The author has since kindly furnished 
 details of the results of the mine up to the close of the year ; from which it 
 appears that during thirteen months, from the 1st of September, 1861, to 
 the 1st of October, 1862, the total amount of ore sold was 2336 tons of 
 twenty-one hundred-weights or 2352 pounds each; the average copper 
 content of the ore being 12*0 per cent. For the month of October, 1862, 
 the produce was 397 tons, of 15-2 per cent. ; for November, 337 tons, of 
 12-5 ; and for December, 357 tons, of 13-2 per cent. Of this last, 88 
 
CHAP. XXL] COPPER ORES. 717 
 
 tons averaged 22-2 per cent*, 124 tons 13'0, 35 tons 10-6, and 110 tons 
 7*1 per cent, of copper. The whole amount of ore raised from this mine 
 from its opening in 1859 to the close of 1861, including a portion of the 
 above period, is stated to have been nearly 6000 tons, averaging 17*0 per 
 cent, of copper. During the thirteen months, according to Mr. Macfar- 
 lane, the average produce for the cubic fathom was 1*6 tons of ore, of 12-0 
 per cent. ; and the average cost of mining and bringing to the surface 
 $11-28 the fothom, or $7*03 the ton of ore. It is however to be borne in 
 mind that these figures are chiefly deduced from the results obtained by 
 quarrying out in open cuttings the productive parts of the cupriferous 
 bed ; and that no allowance is made for exploration or work in unproduc- 
 tive portions, with a view to the future of the mine. Except in the drift 
 already mentioned, but very little work of this kind has been done ; and the 
 whole cost of such explorations is estimated by Mr. Macfarlane at about 
 f 1*50 for each ton of ore obtained ; so that this being added to the estimate 
 already given, the cost was $ 8-50 for the ton of 12-0 per cent. ore. 
 
 The ores raised from this mine are chiefly, as before stated, vitreous and Assays of 
 variegated sulphurets. The following analyses by Mr. Macfarlane will ores ' 
 serve to give an idea of the ore and its gangue. The first three are 
 dressed ores of different qualities ; the fourth is an analysis of the mate- 
 rial obtained in drilling a large mass of the copper conglomerate ; while 
 the fifth is the cement of a breccia, which enclosed angular fragments of 
 limestone. These fragments contained no copper, but yielded carbonate of 
 lime 73-20, carbonate of magnesia 15-50, alumina and oxyd of iron 2-75, 
 silica 8-25; = 99-70. 
 
 
 I. 
 
 24 -75 
 
 II. 
 
 13-07 
 
 III. 
 9-95 
 
 IV. 
 34-20 
 
 V. 
 
 37-20 
 
 
 5-81 
 
 4-06 
 
 3-36 
 
 7-01 
 
 7-31 
 
 Sulphur (by difference),.. 
 
 11-22 
 33-10 
 
 12-88 
 63-07 
 
 7-17 
 63-10 
 
 16-33 
 4-64 
 
 15-89 
 95 
 
 " magnesia, .. 
 
 
 traces 
 
 2-10 
 
 
 38-65 
 
 Alumina. . 
 
 
 
 
 84 
 
 
 Silica, ....25.12 16-92 24-32 36-98 
 
 100-00 100-00 100-00 100-00 100-00 
 
 From the workings at Acton, the outcrop of the limestone is traced, with 
 a very sinuous course, to Wickham Mine. The sulphurets of copper have 
 been found in a great number of places in the intermediate distance, and 
 they are rarely absent from the limestone. Trials have been made at some 
 of these points on the thirty-second and three succeeding lots of the fifth 
 range of Acton. The quantity of ore obtained was however small ; which 
 may be due to the fact that the openings have been made near the base of 
 the limestone band ; for it is the summit of this which, both at Acton Vale 
 and Upton, appears to be most productive of copper ore. At the Wickham 
 
718 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. XXL 
 
 wickham Mine, which is on the fifteenth lot of the tenth range of the township 
 of that name, the yellow, variegated, and vitreous sulphurets occur dis- 
 seminated in a bed of limestone. The ores are however more abundant 
 in what appear to be veins, running through the rock in a northeast 
 direction, with a high inclination. The working here has not yet been 
 sufficient to determine the thickness of the bed, nor the extent of the 
 deposit ; but from a shaft, which was sunk to a depth of thirty feet, about 
 four tons of ore of thirty per cent, were obtained. 
 
 It has already been mentioned that to the southeast of that portion of the 
 synclinal which holds the copper of Upton, Acton, and Wickham, there 
 exists a subordinate fold, which extends from Durham, through Roxton and 
 
 Durham. Ely. On the twenty-first lot of the seventh range of Durham, the copper- 
 bearing limestone, underlaid by a black shale, is exposed on what appears 
 to be the southeast side of this synclinal ; and it is intersected by several 
 veins, which contain copper pyrites in a gangue of calc-spar, mixed with 
 a little quartz, and fragments of the wall-rock. These veins have a gene- 
 ral northeastward bearing ; and trial shafts have been sunk upon three of 
 them, whose breadths vary from six to thirty inches. On the most north- 
 westerly of these, an excavation reached the underlying black shale at a 
 depth of twelve feet. Eighteen feet to the southeast, in a second shaft, 
 the black shale was found at a depth of thirty-six feet ; and at the third, 
 twenty-four feet farther in the same direction, a shaft of twenty-four feet 
 has been sunk without reaching the shale. In this last, the vein has an 
 underlie to the southeastward of about a foot in a fathom ; and in a breadth 
 of from six to twelve inches, it shows good masses of yellow copper ore. 
 
 Roxton. Farther to the southwest, on the twenty-third lot of the third range of 
 Roxton, the limestone appears in a nearly vertical position, with shales both 
 above and below, and having a breadth of about 100 yards. Near the 
 summit of the band, and also in contact with the overlying shale, rich 
 specimens of variegated ore were found disseminated in the limestone, an 
 associated with calc-spar in irregular veins. A considerable mass of the 
 rock has been excavated, but it is difficult to ascertain the amount of 
 ore obtained. 
 
 Wendover. In the continuation of the Fafnham and Lauzon synclinal to the north- 
 east of the St. Francis, the diorite of the series is found developed 
 to a great extent along the river, opposite Drummondville. The rock has 
 here a breadth of about half a mile, and dips to the southeast at a moderate 
 but variable angle. Besides the varieties of it described on page 243, 
 some portions have a dark maroon or purplish color ; and are interstratified 
 with shaly layers, into which the more compact diorite passes by insensible 
 degrees. In the lower part of the section, these slates sometimes contain 
 concretionary or nodular masses, somewhat resembling those of the shale at 
 St. Joseph described on p. 255, but smaller. To these succeed black shales 
 
CHAP. XXI.] COPPER ORES. 719- 
 
 containing graptolites, underlaid by a band of about ten feet of diorite, and Diorite. 
 by a second layer of graptolitic shales, with two undetermined bivalve shells. 
 Much of the diorite is broken and shattered, as if by numerous small faults ; 
 and the surfaces exhibit what is called slickensides, the result of the move- 
 ment of the parts on one another. This diorite' is supposed to correspond 
 with those of Upton and Acton, from which many beds of it cannot be dis- 
 tinguished ; but the cupriferous limestone which there accompanies it, seems 
 to be wanting, and it is the diorite which holds copper. In this exposure, 
 on the first lot of the first range of Wendover, six or more ore-bearing 
 veins or courses are met with in a breadth of about 350 yards. They 
 have a width of from three to twelve inches, and in some cases consist of 
 little more than shattered fragments of the wall-rock, cemented by copper 
 pyrites. In other cases the interstices are filled up with calc-spar holding 
 yellow, variegated, and vitreous copper ores. Several small excavations 
 have here been made upon these veins, and good specimens of ore obtained. 
 The locality appears to deserve a more effectual trial than has yet been 
 given to it. 
 
 In the continuation of the synclinal to the northeast, the rocks are in 
 many parts concealed by the overlying drift. On the fourteenth and fif- 
 teenth lots of the eighth range of Somerset, however, a band of diorite is Somerset 
 met with resting upon the limestone conglomerate ; which is here ten feet 
 in thickness, and contains copper pyrites. In the adjoining township of 
 Nelson, on the eighth lot of the eleventh range, copper has lately been dis- Nelgon 
 covered, and explorations have been commenced in rocks said to resemble 
 those found farther to the northeast in the parish of St. Flavien. The st Havien 
 Black River mine which is situated in this parish, is about five leagues 
 west of the Chaudire River, and two leagues south of the St. Lawrence. 
 Here is a band of dioritic rocks, similar in many respects to that of Wen- 
 dover, and about a quarter of a mile in breadth, dipping to the northwest 
 at a moderate angle. As this is supposed to be on the northwest side of 
 the synclinal, the inclination of the strata would here be the result of 
 an overturn. The band has been traced for two miles on the strike, and 
 is overlaid by red slates. Much of this band is a fine-grained greenish- 
 grey amygdaloid, holding numerous small spheroidal masses of calc-spar, 
 with which the mass of the rock in these portions seems also to be pene- 
 trated. Some portions of the strata are reddish-brown ; and resemble an 
 indurated and altered argillite, being slightly or not at all amygdaloidal, and 
 made up of reniform masses from a few inches to a foot or more in diameter. 
 
 On the northwest side of the band the diorites are seen interstratified 
 both with red slates and limestone. Beds of the latter a few feet in thick- 
 ness are also met with at what appears to be the base of the series. 
 These limestones are often conglomerate, enclosing fragments or rounded 
 masses of diorite. In one portion angular fragments of a fine-grained 
 
720 GEOLOGY OP CANADA. [CHAP. XXI, 
 
 diorite, often reddish, are imbedded in a finely granular reddish limestone 
 base. Another portion near the southeast side of this band consists of both 
 angular and rounded masses of diorite, often amygdaloidal, and sometimes 
 two feet in diameter ; the spaces between which are lined with a layer of 
 columnar calc-spar, within which crystalline quartz fills the interstices. 
 These minerals often enclose small portions of copper pyrites ; and of a 
 black carbonaceous matter, or indurated bitumen, which is also common in 
 quartz veins here. The mode in which this latter substance occurs at St. 
 Flavien, has been detailed on page 525. In other cases, the whole of the 
 interstices in the breccia or conglomerate are filled with lamellar calc- 
 spar ; in which small grains and filaments of native copper, and stains of 
 the green carbonate, are disseminated. 
 
 Black River This great mass of rocks is cut by veins holding copper ore, of which 
 more than a dozen have been observed. Some of these are filled with a 
 breccia of the wall-rock, in which the interstices contain yellow and varie- 
 gated sulphurets of copper. In other veins these same ores occur in a gan- 
 gue chiefly of quartz ; and in others still, with calc-spar. This calc-spar is 
 sometimes lamellar and cleavable, and at other times drusy ; holding, besides 
 the sulphurets of copper, little masses of fibrous malachite, and small crys- 
 tals of the blue carbonate. The carbonaceous matter already mentioned is 
 frequently associated with these ores, and sometimes fills an inch or two of 
 the veins. The dimensions and directions of these veins are very variable ; 
 the underlie of some being nearly south, or to the east of south, at high 
 angles ; while others have a northwest ; and others still, a northeast underlie, 
 or are nearly vertical. Some of the veins are from three to six inches in 
 breadth ; while others attain two feet or more. Striae, produced by the 
 sliding of the surfaces, are occasionally found on their walls. Small 
 excavations have been made upon several of these veins, and the por- 
 tions of rich ore which have been obtained are such as give considerable 
 promise for the future. The resemblance between these amygdaloidal 
 diorites, with quartz, calc-spar, and native copper,, and some of the Upper 
 copper-bearing rocks of Lake Superior, is worthy of notice. 
 
 In the continuation of this synclinal to the northeast, small portions of 
 copper are observed hi several places. Thus on the shore of the St. Law- 
 rence, a little below St. Nicholas church, the green carbonate occurs in 
 red slate, and again in the same rock a mile above Point Levis. About 
 ten miles from the St. Lawrence copper pyrites occurs on the ChaudieYe, 
 at the Narrows, in a calcareous sandstone ; and the same ore is found in a 
 red limestone on the Etchemin, four miles from its mouth. On the same 
 
 St. Henry, river, a little below St. Henry, small portions of native copper occur in red 
 shale ; and the metal has been found in a similar rock at Point Levis. On 
 the north side of the St. Lawrence copper pyrites is found in red shale 
 and sandstone, a mile below Cape Rouge ; and at Quebec in a cutting made 
 
CHAP. XXL] COPPER ORES. 721 
 
 for the aqueduct at Coteau Ste. GeneviSve, vitreous copper ore was found Quebec, 
 associated with a limestone conglomerate. The small portions of copper 
 which occur in the places just mentioned are not of economic importance, 
 but are interesting as showing the persistence with which the metal accom- 
 panies the rocks of this portion of the Quebec group. 
 
 In the second synclinal, which extends from St. Armand to St. Mary 
 on the Chaudidre River, copper ores are found in small quantities in various 
 localities in Sutton and Brome. The iron slates of this region (page sutton. 
 679) often contain a little disseminated copper pyrites, or are stained 
 with the green carbonate ; which also sometimes occurs in the dolomites 
 associated, with these specular schists. On the eighth lot of the tenth range 
 of Sutton, on the eastern side of the synclinal, copper ore is found in 
 larger quantity, and mining operations have been commenced in a band 
 of fine micaceous or nacreous slates ; which run in a northward direction, 
 and dip at a high angle to the westward, or are nearly vertical. These 
 strata are exposed for 500 feet, and* may be traced for half a mile along 
 the strike, running parallel with a band of dolomite, which is seen about 
 half a mile to the eastward, across the strike. Nodules of magnesian lime- 
 stone are however disseminated in the slates immediately to the east 
 of the portions which hold the copper ores. These, which consist of 
 the yellow, variegated, and vitreous sulphurets, are disseminated in grains, 
 or in small thin lenticular masses. The proportion in which the ores occur 
 is variable. The bed in which the principal excavations have been made 
 is said to vary from six inches to nearly three feet ; and about eight feet 
 to the east of this another cupriferous bed, of six inches in width, has been 
 observed. The copper may however be disseminated through a greater 
 breadth than these measures indicate. In one excavation made here, the 
 ore appeared to be more or less diffused through a breadth of four and a 
 half feet ; and the assay of a sample from this cutting, gave four and a 
 half per cent, of copper as the average from this thickness of rock. A 
 layer of fine-grained blackish slate, an inch in thickness, from this place, 
 which seemed to owe a portion of its color to vitreous ore, so finely divided 
 as to be scarcely apparent to the eye, yielded on assay ten per cent, of 
 copper. A shaft of ten fathoms has been sunk on the incline of the bed, 
 and a small quantity of ore extracted. Small quartz veins, holding varie- 
 gated copper ore, are met with cutting these cupriferous slates. 
 
 To the northward, the continuation of the synclinal shows copper ore in Shefford. 
 Shefford, and in Stukley. Good specimens of vitreous copper in a gangue 
 of quartz and calc-spar, cementing a brecciated vein of fine micaceous 
 schist, are said to come from the land of Major Wood, a little to the east 
 of Frost Village in Shefford. In Stukley, on the seventh and eighth lots 
 both of the first and second ranges, copper pyrites is described as occur- 
 ring in a band of limestone, interstratified with slates. An excavation in 
 
 w 
 
722 GEOLOGY OP CANADA. [CHAP. XXI. 
 
 stnkiey. one place, to a depth of ten feet, showed promising quantities of the ore, 
 which has also been observed on the second lot of the fourth range. 
 From the sixth to the eleventh range of the township, a belt of chloritic 
 slates, having a dip to the northwest of from 30 to 60, and includ- 
 ing quartzose and limestone bands, is marked in a great many localities by 
 the presence of copper ores. Certain beds in these slates present segre- 
 gated veins, sometimes cutting the strata, but more frequently running 
 with them, in irregular masses or bunches. The veins consist of quartz, with 
 bitter spar, calc-spar, and chlorite, often containing also feldspar and epi- 
 dote, and carrying small quantities of vitreous and variegated copper ores 
 in strings and grains, sometimes with specular iron. On the ninth and 
 tenth lots of the sixth range, two excavations have been made, one fifteen 
 feet long, and thirty feet deep on the slope of the bed ; which is to the 
 northwest, at an angle of forty-five degrees. From these pits, more than 
 700 tons of rock were raised, which gave a few barrels of marketable ore, 
 but too little to pay the expense of working. On the eighth lot of the 
 seventh range, copper ore occurs in two bands of dolomite, dipping as 
 before to the northwest : one of these is about thirty feet wide. The second, 
 which is greenish and chloritic, holds variegated and vitreous ores in larger 
 quantities than most of the localities observed in this vicinity. Two bands 
 of dolomite, probably the same, are also described as occurring on the 
 eighth range, both of which hold vitreous copper ore. Several small 
 pits have been sunk upon these, with encouraging results. On the ninth 
 lot of this range, a band of the chloritic slate contains small quantities of 
 variegated and vitreous ores in a gangue of quartz, with feldspar and bitter 
 spar. Copper has been noticed under similar conditions in chloritic slates 
 on the second, fifth, and eighth lots of the ninth range, and the fourth, 
 fifth, sixth, and seventh of the tenth. On the last-named lot the copper 
 ore is found with specular iron, in a bed of hard chloritic slate, through 
 a breadth of two feet, hi which quartz and spars predominate. A pit 
 has been sunk here to a depth of twenty-two feet. On the fifth lot of 
 the eleventh range of Stukley, there is a band of soft purple slate, barred 
 with black, and marked by films of a greenish chlorite-like mineral. It 
 dips northwest < 65, and in its upper portion holds strings of quartz and 
 calc-spar, with a little copper ore. 
 
 Melbourne. To the northeast of Stukley, the copper-bearing strata of the second 
 synclinal are continued across Ely, where they are concealed, for the most 
 part, by the superficial deposits. They however re-appear in Melbourne, 
 where the chloritic and micaceous or nacreous slates are traced across the 
 northwestern portion of the first six ranges, and are found to contain dis- 
 seminated sulphurets of copper in a great number of places, often with 
 epidote and specular iron. At the Coldspring Mine, on the sixth lot of the 
 second range of Melbourne, the strata dip to the northwestward at an angle 
 
CHAP. XXI.] COPPER ORES. 723 
 
 of about forty-five degrees, and exhibit in a breadth of two hundred feet 
 several parallel bands, in which the quartzose mica-slate is colored green by Mine> 
 carbonate of copper, and contains portions of the vitreous and variegated 
 ores disseminated in grains and lenticular masses. A shaft has been sunk 
 here, which intersects one of the beds at a. depth of six fathoms, and sev- 
 eral trenches have been made across the beds. A vein yielding rich speci- 
 mens of vitreous copper is also described as here cutting the strata at a small 
 angle. Some of the beds of slate just noticed, like those of Sutton, con- 
 tain sulphuret of copper in a state of minute division. Such a band 
 impregnated with the vitreous ore, gave, according to Mr. Robb's assay, 
 seven per cent, of copper. 
 
 On the second lot of the fourth range, is what is called the Balrath Mine. Bairath 
 Here the cupriferous strata include a vein from two to four feet wide, M 
 which is described as conformable to the stratification, and as consisting 
 of quartz and calc-spar, carrying in certain portions considerable quan- 
 tities of variegated copper ore. A trench twenty feet long and ten feet 
 deep was first dug on the strike of this vein, and a shaft then sunk to 
 about fifty feet, from which about a ton of good ore was obtained. Four 
 other smaller openings parallel to this also afforded indications of copper. 
 On the second lot of the sixth range, a shaft was sunk at a little distance 
 from a copper-bearing bed, intersecting it at a depth of fifty feet, where 
 the quantity of the ore was found to augment. 
 
 Beyond the St. Francis, the cupriferous band is continued in the town- Cleveland, 
 ship of Cleveland. On the twenty-sixth lot of the thirteenth range of this 
 township, variegated and vitreous copper ores are found disseminated in a 
 bed of chloritic rock twelve inches in thickness, which dips to the northwest 
 at a high angle. A shaft has been sunk upon this to a depth of about twenty 
 feet. Sixty feet to the eastward of this is a cupriferous bed of three feet, 
 and ninety feet to the west another of five feet hi thickness. In these the 
 same ores are more sparingly disseminated in a chloritic rock. On the 
 twenty-fifth lot of the twelfth range, is what is known as the St. Francis st. Francis 
 Mine. Here, a vein slightly oblique to the stratification is found traversing M 
 chloritic beds, which are associated with an argillite holding nodules of 
 qu,artz and orthoclase feldspar. These rocks are described on page 606. 
 The vein, which is of quartz, has been traced in a north-east direction about 
 ninety fathoms, with an average thickness of three feet. Five or six small 
 excavations, which have been made along its outcrop, exhibit the variegated 
 and vitreous ores of copper, mixed with yellow sulphuret. In the continu- 
 ation of the synclinal through Shipton and Tingwick, indications of copper 
 have as yet been observed in but few places ; but in Chester the chloritic 
 slates on the eleventh lot of the tenth range contain small portions of 
 variegated and yellow copper ores in quartz veins. The second lot of the 
 ninth, and the eighth lot of the seventh range have also afforded small 
 
724 GEOLOGY OP CANADA. [CHAP. XXL 
 
 Chester. quantities of copper ; and the vitreous ore is said to be found in chloritic 
 slates on the sixth and ninth lots of the fourth range. On the eighth 
 lot of the fifth range, these slates hold a vein of quartz about two feet 
 in width, which appears to run with the strike, and contains masses of 
 the vitreous copper ore, with green carbonate. In the adjacent township 
 
 Halifax, of Halifax, copper ores are met with in the chloritic and nacreous slates, 
 which, as before , dip to the northwest at a high angle, and are asso- 
 ciated with dolomite ; in which rock, a vein of quartz holding copper 
 pyrites is found on the sixth lot of the seventh range. .Variegated ore 
 is also reported as existing on the fourth and sixth lots of the ninth 
 range, and on the sixth lot of the eleventh range. The Halifax Copper- 
 Mining Company has lately been established to work a quartz vein, 
 which is described as being from eight inches to three feet wide, and as 
 containing promising quantities of vitreous ore, with copper pyrites, and 
 portions of green carbonate and red oxyd of copper ; the latter two occur- 
 ring at the surface of the vein. This synclinal, with its copper-bearing 
 
 Ireland. strata, is traced from Halifax, through contiguous parts of Ireland and of 
 Inverness, into Leeds. On the fourth lot of the eleventh range of Ireland, 
 variegated ore is found ; and on the ninth lot of the ninth range, copper 
 pyrites occurs in dolomite. It is also met with in similar conditions on the 
 second lot of the fourth range of Inverness. On the fourth lot of the 
 second range, variegated copper ore occurs in a quartz vein two feet wide 
 in nacreous slates. This locality was, in 1847, recommended by the 
 Survey for a crop trial. 
 
 Leeds. In Leeds the copper-bearing rocks are exposed in a great number of 
 
 places, and have been more carefully examined than in any other locality 
 
 Harvey Hiii along this synclinal. The explorations at the Harvey-Hill Mine, on 
 the seventeenth lot of the fifteenth range, now the property of the English 
 and Canadian Mining Company, are the most extensive which have 
 as yet been made in the Eastern Townships. The shafts, and the long 
 adit which has been opened, afford an opportunity not elsewhere pre- 
 sented for studying the structure of this mining region, and it is pro- 
 posed therefore to give a detailed description of this mine. The accom- 
 panying plan and sections are reduced from drawings furnished to the 
 Survey, on a scale of one inch to a chain, by Mr. Herbert Williams, 
 the skilful director of the Harvey-Hill Mine ; who has also kindly 
 given many details to complete the description. The copper ores at 
 this locality occur both in courses or veins, and in beds. The strata 
 are here, for the most part, finely micaceous slates, which, from their 
 unctuosity, are often called talcose, but are generally not magnesian. 
 A bed of steatite is however met with, and dark bands, approaching to 
 argillite, occur in some parts, while others are whitish or light grey in 
 color, and contain a large amount of chloritoid disseminated. The dip of 
 the strata appears to be from 25 to 80 W. of N. ; with an average inclin- 
 
CHAP. XXL] COPPER ORES. 725 
 
 ation of from fifteen to thirty degrees. The courses are really irregu- veins. 
 lar and interrupted veins, which do not coincide with the strata either in 
 dip or strike. The bearings of eight of them are from north, to N. 20 E., 
 while others run nearly eastward. Their underlie is generally to the 
 westward, at from fifty to nearly ninety degrees. These veins, which 
 appear to have filled up fissures in the slates, are more or less lenticular 
 in shape. Some of them have been traced for as much as 100 fathoms 
 on the surface, and are occasionally six or seven feet wide in the thickest 
 part, thinning out however both horizontally and vertically. 
 
 These veins have a gangue of quartz, occasionally mixed with calc-spar, 
 pearl-spar and chlorite, and contain rich ores of copper; some of 
 them yielding the variegated and vitreous species, and others, copper 
 pyrites. These are sometimes so abundant that as much as two tons of 
 twenty per cent, ore have been obtained from a fathom. Within an area 
 of about thirty acres, open cuttings have been made upon as many as 
 fifteen distinct courses, and shafts have been sunk on two others. Notwith- 
 standing the richness of portions of these veins, the ore is disseminated in 
 them in such an irregular and uncertain manner, that they are considered copper beds, 
 secondary in importance to the interstratified beds, hi which the sulphurets 
 of copper are disseminated in the slate rock. The first of these beds has Upper bed. 
 a thickness of from two to six feet. Twenty fathoms below it, occurs a bed 
 of three inches, followed, in descending, by fifteen feet of barren slate. This 
 separates it from another ore-bearing bed of six inches, which rests upon a 
 stratum of soapstone or steatite, six feet in thickness. In the plans and Second bed. 
 descriptions here given, the stratum of steatite, with the two layers of 
 copper-bearing rock, and the intervening fifteen feet, will be represented 
 as a single band, and designated as the second. This band, characterized 
 by the bed of steatite, can be traced for a distance of two miles along the 
 outcrop, but is lost sight of to the eastward of Fremont's shaft. An adit 
 has been carried horizontally into the side of the hill for a distance of 248 
 fathoms, intersecting in its course the upper bed. The second bed, however, 
 was not seen in the adit, and is perhaps displaced by some fault in the strata. 
 Near the place where it might have been looked for, a quartz course occurs. 
 Several of these courses were met in the adit, but they appear to have no 
 connection with those at the surface, and, according to Mr. Williams, thin 
 out both vertically and horizontally. At about twenty fathoms from the 
 extremity of the adit, after traversing about twelve fathoms of soft, dark 
 "bluish slate, a light grey band was met with, holding chloritoid, and a little 
 copper pyrites. A rock similar to the last also occurs at the end of the Third bed. 
 adit, and contains, besides a little disseminated ore, some quartz courses 
 holding copper pyrites. This band of greyish chloritoid slate is marked 
 in the plans. The strata in this part of the adit appear much disturbed ; 
 and the dip varies, being in some places from 10 to 14, and in others 
 from 35 to 40. 
 
726 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. XXI. 
 
 439. FLAW ov HARVEY-HILL COPPER MINE, LEEDS. 
 
 . . Outcrop of copper beds. 
 
 Ditto of quartz courses. 
 
 = Open cuttings on ditto. 
 
 ::::::.-:: Under-ground workings. 
 
 = = = Roads. 
 
 Jj Jl, Upper copper bed. 
 
 B, Second copper bed. 
 
 C C, Lowest copper bed. 
 
 D E, Morrison's adit ; line of section No. 2. 
 
 a, 1st shaft in adit, with quartz course. 
 
 6, Sewell's level, on a lode. 
 
 c, 2nd shaft in adit, with bed j&. 
 
 d, Level on a quartz course. 
 
 F, Fremont's shaft. 
 
 G, Harvey-Hill shaft. 
 
 e, 10-fa thorn cross-cut, and level. 
 
 H, Kent's shaft, with level on bed Jt. 
 /, 30-fathom levels on bed J. 
 g, 10-fathom levels. 
 IK, Line of section No. 1. 
 h, i, Reservoirs. A:, Dressing floors, 
 I l t Lines of tramways. 
 
CHAP. XXL] 
 
 COPPER ORES. 
 
 727 
 
 The interstratified beds contain the yellow and variegated ores, the latter The ores, 
 generally predominating. These sulphurets are disseminated through the 
 slate in small masses, often of a lenticular form, running with the bed- 
 ding. They are generally thin and small, but sometimes attain from one 
 half to three fourths of an inch in thickness ; and occasionally present in 
 
 
 
 It 
 
 J. d 
 
 ? S a 
 
 
 5 
 
 .22 
 
 S * 
 
 fi S ^ - O 
 
 oo ^ r 
 o o d ^ O 
 
 " S 
 
 section, a length of six or even twelve inches. Besides plates and lenticu- 
 lar masses, which interlock, and overlap one another, numerous small grains 
 of ore are scattered through the beds, and the average amount of copper 
 in the layer may be stated at from three and a half to five per cent. 
 The copper-bearing beds are sometimes light grey and quartzose, and have 
 at other times a chloritic aspect. 
 
728 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 In the second shaft of Morrison's adit, the upper copper-bearing bed 
 was met with at a depth of fifteen fathoms. Immediately beneath it was 
 found a quartz course, which contained some very rich copper ore ; while 
 the bed itself at this point held scarcely a trace of copper, and could only 
 be distinguished from the adjacent slate by its lighter color and quartzose 
 
 Kent's shaft, nature. In sinking Kent's shaft, which is about 170 fathoms to the 
 westward, the same bed is met with at a depth of about twenty fathoms. 
 It has also been intersected by two levels or cross-cuts from the shaft, the 
 lower at thirty fathoms, and followed upwards for a distance of over 
 twenty fathoms on the incline. The working of the bed is now being con- 
 tinued up toward the shaft, as well as east and west from the thirty- 
 fathom level ; where it has been wrought for about twenty-five fathoms on 
 its strike, and for ten fathoms in the level above. In the early part of 
 1862, ten superficial fathoms of the rock from this upper level were broken, 
 weighed, and sampled, and were found to average 258 hundred-weights 
 of ore yielding three and a half per cent, of copper (equal to over 1000 
 pounds of metal) to the fathom of ground. The ore now removed from the 
 working at thirty fathoms averages about five per cent, of copper. In 
 driving the lower cross-cut, a lenticular quartz course was met with, from 
 which there were taken over fifty tons of rich ore, yielding forty-three per 
 cent. It thinned out as it approached the interstratified bed ; and on work- 
 ing this on the incline, it was found to be greatly impoverished for some 
 distance on either side of its contact with the quartz course. In driving 
 east on the bed, from the thirty-fathom level, another lenticular quartz 
 course is met with, running nearly with the dip of the bed, which last is 
 almost destitute of copper on both sides. The course, however, which is 
 being followed, and has a breadth of from eighteen to twenty-four inches, 
 yields about a ton and a half of forty per cent, ore to the fathom. This, with 
 the other two instances already mentioned, seems to show that these veins 
 or courses have been filled with ore derived from the bed. In working this 
 bed, masses of quartz are occasionally met with imbedded in it. These, 
 which are probably in some cases courses running with the strata, and in 
 others small lenticular beds, vary from a few inches to six or seven feet in 
 length, and from a quarter of an inch to a foot or two in thickness. They 
 contain, on an average, from seven to eight per cent, of copper ; while the 
 adjacent slate, for a thickness of five or six feet, does not contain more 
 than five per cent. The various workings in Kent's shaft may be said 
 to have tested the bed over an area of over 600 square fathoms ; while the 
 extension of this same bed to the adit, a distance of 170 fathoms, and the 
 fact that it has been traced along its outcrop for more than 500 fathoms, 
 show that much may be expected from working this copper-bearing bed! 
 
 Molybdenite. In some courses in this working, a considerable quantity of sulphuret 
 of molybdenum is found, with a little copper ore, in a gangue of 
 
CHAP. XXL] COPPER ORES. 729 
 
 quartz and bitter spar. Not unfrequently, these courses hold large masses 
 of the copper ores, which are sometimes perfectly pure and homogeneous, 
 and at other times enclose cleaveable masses of bitter-spar, or of limpid 
 transparent quartz, giving to the ore a porphyritic aspect. This quartz, Quartz 
 on examination, is found to be in regular prismatic crystals, which however cr - vstals - 
 have their angles rounded. In one case, a mass of compact variegated 
 copper ore was penetrated by several terminated prisms of quartz, from 
 one fourth to one half an inch in diameter. All the angles of these were 
 much rounded, and the planes of the crystals, which were in close contact 
 with the ore, were concave, and had lost their polish ; retaining only a some- 
 what greasy lustre, precisely like crystals which have been exposed to the 
 action of a solvent liquid. A thin shining green layer, apparently of 
 a silicate of copper, covers the surfaces of the ore in contact with the 
 crystals. Similar specimens of quartz have been found in the vitreous 
 copper ore of this locality, and also at the Ham Mine. 
 
 Fremont's shaft was sunk upon a quartz vein, which had an underlie Fremont's 
 of 75 to the eastward. After following this for forty-five feet, the Bhatt 
 underlie changed to the westward, still with the same angle ; but the shaft 
 being continued vertically for seventy-five feet more, the second copper bed, 
 with its underlying stratum of steatite, was met. The layer in contact 
 with the steatite was excavated for five fathoms on the incline, in the course 
 of which the vein from the surface was again met with. At the bottom of 
 the incline, a level was driven in the bed for about five fathoms ; and the 
 copper ore being continuous throughout these distances, its presence may 
 be said to be shown over about twenty-five square fathoms of the bed. In 
 some parts of this working, the copper ore is found in the steatite ; a layer 
 of which, several inches in thickness, sometimes becomes a highly crystal- 
 line green talc, holding bitter spar, and rich in disseminated sulphurets of 
 copper. The shaft at G was sunk upon a quartz ^course, which abounded 
 in vitreous ore. In a cross-cut from this shaft, at a depth of ten fathoms, 
 a second quartz course was met with. 
 
 The following quantities of ore, averaging about thirty-five per cent., 
 have within the last five years been shipped from this mine to England* 
 The fractions of tons are here disregarded. In 1858, 10 tons ; in 1859, 
 43 tons ; in 1860, 104 tons ; in 1861, 70 tons ; and in 1862, 95 tons ; 
 equalling in all 322 tons of ore. In addition to this, there was at the sur- 
 face, at the close of 1862, about 1000 tons of poor material, supposed to 
 contain about two and a half per cent, of copper; besides 500 tons of 
 material raised from the upper copper bed, and containing from four to 
 five per cent, of copper. 
 
 Besides the copper-bearing beds whose course has just been described, 
 quartz courses holding the various sulphurets of copper have been observed 
 on a great number of lots from the eighth to the eighteenth of the ranges 
 
730 GEOLOGY OF CANADA. [CHAP. XXT. 
 
 from ten to fifteen, inclusive. In the western part of the township, 
 copper pyrites occurs in dolomite on the fourth lot of the fourth range. 
 On the fifteenth lot of the fourteenth range, a shaft was sunk by the 
 predecessors of the present Mining Company, on the land of Mr. Nutbrown, 
 
 Native on a remarkable vein, which cuts a band of steatite, and contains vitreous 
 
 copper, specular iron, and native gold. This vein has already been 
 noticed on pages 516 and 257. Farther to the northeastward, the 
 copper-bearing slates, with their quartz, courses, are continued into the rear 
 
 chaudiere of the seigniory of St. Giles ; where the Chaudiere Mining Company has 
 lately been formed for working several quartz veins, which are found on a 
 portion of the seigniory known as the Handkerchief. According to a 
 report of Mr. Wm. Williams, made in September 1862, eight well-defined 
 quartz veins are here exposed, traversing the slates, in a trench cut at right 
 angles to them, in a breadth of 1100 feet. Two of these are three feet 
 wide, and have been traced 1200 and 1500 feet. All of the veins con- 
 tain, in greater or less abundance, the same ores of copper as have been 
 described at the Harvey-Hill Mine. A little farther, on the first three 
 
 st. Margaret, lots of the St. Margaret range of the same seigniory, openings have 
 been made upon several quartz veins, which run in a northeast direc- 
 tion, and are from one to two feet in breadth. They contain portions 
 of vitreous and variegated copper ores, occasionally with green car- 
 bonate, and with specular iron, and are more or less stained and impreg- 
 nated with earthy oxyd of manganese. In some of the veins, crystals of 
 quartz occur, in the interstices of which is found a black carbonaceous mat- 
 ter, like that already described at St. Flavien. The rock adjoining the 
 veins, is chloritic slate, in which there are said to be two interstratified 
 quartzose beds, of about six feet each, marked by chlorite and manga- 
 nese, and holding small portions of variegated and vitreous copper ores. 
 Beyond this, the rocks of the synclinal are traced across the Chaudiere 
 
 st. Mary. River, where, in the front of the third concession of St. Mary, and north of 
 east from the church, red and green nacreous slates are interstratified with 
 beds of red limestone. These, which are much disturbed and broken, are 
 traversed by little veins of quartz and calc-spar, holding small portions of 
 yellow and variegated copper ores, with green carbonate. Fissures are 
 here filled with an impure earthy oxyd of manganese ; and patches both of 
 specular iron and of jasper are found in the limestone. 
 
 Potton. In the description of the second synclinal, it has been stated that what 
 
 is regarded as a division or spur of this passes down^o the east of Sutton 
 Mountain. Here its eastern outcrop is seen on the western side of the 
 river Missisquoi, as a band of slates, sometimes chloritic, with serpentine 
 and steatite, and occasionally with small portions of copper ore. To the 
 east of the Missisquoi these same strata are repeated on the eastern side 
 of the anticlinal axis, which separates the second from the third synclinal. 
 
CHAP. XXI.] COPPER ORES. 731 
 
 The western outcrop of this latter, marked by the same rocks, is traced Third 
 northward through the eastern parts of Potton, Bolton, and Stukley, into B7nc 
 Orford ; and thence, through Brompton, to the southeast parts of Melbourne, 
 Cleveland, and Shipton. The copper ores already described in the north- 
 western parts of the last three townships, belong, like those of the northern 
 part of Ireland, to the second synclinal, and have been already noticed. 
 The outcrop of the third is continued through Ham and Wolfestown ; and 
 farther on, there is a great development of the rocks of this series, which 
 may be regarded as a continuation of the third synclinal, and consist of 
 dolomites and serpentine, with steatite, chloritic, and epidotic rocks. These 
 are traced to the northeast, and include large portions of the townships 
 of Garthby, Coleraine, Ireland, Thetford, and Broughton, the northwestern 
 parts of Adstock and Tring, and the contiguous portions of the seigniories 
 of St. Joseph and Vaudreuil ; beyond which the rocks of this synclinal are 
 traced into Frampton, Cranbourne, Standon, and Buckland. This distribu- 
 tion of these strata is important, inasmuch as copper and -other valuable 
 minerals will probably be discovered hi many parts of their course. Vit- 
 reous and variegated ores are found in quartz veins on the twelfth and 
 thirteenth lots of the fifth and sixth ranges of Broughton ; and in St. Joseph, st. Joseph, 
 a mile west of the ChaudiSre River, and opposite to the road above the 
 church, leading to Frampton, vitreous copper ore occurs with quartz, chlo- 
 rite, and earthy oxyd of manganese, filling small fissures in red and green 
 shales, which are associated with red limestone. On the east side of the 
 river, the red limestone in the vicinity of the peculiar concretionary argil- 
 lite described on page 255, contains a little green carbonate of copper. 
 
 The principal discoveries of copper in this synclinal, have, up to the 
 present time, been in its southwestern portion, and in the townships of Ascot, 
 Ham, and G-arthby. Along its western margin however, on the fourteenth 
 lot of the tenth range of Potton, small quantities of copper pyrites occur in 
 a quartzose rock, on the north side of the Owl's Head Mountain ; and on the 
 twenty-eighth lot of the eighth range of Stukley, the same ore is met with in 
 a band of limestone intermixed with chloritic slates. Near to this, in Orford, Or ford. 
 on the ninth lot of the eighteenth range (according to the Crown Land 
 survey), a quartzose chloritic rock near the band of serpentine, contains 
 a small amount of copper pyrites. The chloritic slates in the vicinity often 
 weather black from the presence of manganese. On the ninth lot of the 
 road range A (Land Company's survey), and near the junction of the ser- 
 pentine with a diallagic diorite, six quartz veins occur in the latter rock, 
 within a breadth of twenty-five feet. Some of these are ten inches wide, 
 and they all contain portions of yellow copper ore, which is associated with a 
 greenish serpentine-like material. These veins are nearly vertical, but seem 
 to converge towards the south, and also in descending. 
 
 The eastern side of the third synclinal is traced northeastward in a 
 
732 GEOLOGY OF CANADA. [CflAP. XXL 
 
 Ascot narrow belt between the two overlying portions of unconformable newer 
 M ! ne ' rocks, through Stanstead and Hatley, into Ascot. Here, in the vicinity of 
 Sherbrooke, the micaceous and chloritic slates contain copper ores in several 
 places. On the eighth lot of the eighth range, at Haskell Hill, is what is 
 now known as the Ascot mine. The ore-bearing bed, which is about five 
 feet in thickness, is an impure limestone, associated with chloritic schists. 
 The dip of the strata at the mine is northward, at an angle of 72, and a 
 shaft has been sunk forty-three feet on the incline. From this a drift has 
 been carried along the ore-bed, about fifty feet to the west and thirty-five feet 
 to the east. A transverse cutting was made from the bottom of the shaft 
 twenty-five feet to the northward, the rock containing copper ore throughout, 
 which may indicate a thickening of the bed. At the end of this distance 
 the copper-bearing bed had a southward dip at an angle of 75 ; showing 
 apparently an upward turn towards the surface, on the north side of a small 
 synclinal fold. The bed has been traced for some distance on each side 
 of the shaft. A little to the southeastward of this shaft, another has been 
 sunk for a few feet on a bed of ore, which dips southward at an angle 
 of about 45, and appears to be a repetition of the previous bed on the 
 southern side of a small anticlinal. The ore of this locality consists of 
 copper pyrites, which is disseminated in small strings and grains through a 
 mixture of limestone and chlorite. Considerable quantities of the rock 
 sent to market without dressing yielded eight per cent, of copper. 
 
 On the ninth range of Ascot, and on the tenth lot, near the line of the 
 eleventh, there is a considerable breadth of fine white micaceous or nacreous 
 slates, with which is interstratified a bed of greenish and greyish quartzose 
 mica schist. This is in parts chloritic or talcose, and contains large quan- 
 tities of a mixture of iron pyrites, with yellow copper ore, the latter 
 being irregularly disturbed. A few tons of the rock having been removed 
 from the bed by blasting, selected portions of this gave, when dressed, 
 one half their weight of ore, which contained one third of silicious matr- 
 ters, and 7*3 per cent, of copper, the remainder being iron and sulphur. 
 The breadth of this bed, which has an eastward dip of about thirty degrees-, 
 is not far from six feet, and it is estimated that it will yield two tons of 
 dressed ore, similar to the above, to the fathom. A great bed of the 
 same ores is found on the sixth lot of the ninth range ; and copper pyrites 
 also occurs, with galena, on the ninth lot of the same range, 
 
 On the seventeenth lot of the seventh range, on the road between Sher- 
 brooke and Lennoxville, a vein or bed of white quartz is found running 
 with the stratification, nearly north and south, and having a dip of 65 to 
 the eastward. The associated rocks are micaceous and chloritic slates. 
 The bed, which was recommended for a crop trial in 1847, is marked at 
 the surface with gossan, and contains disseminated copper pyrites. 4- 
 portion of this, separated by washing, was found to contain 30*3 per cent. 
 
CHAP. XXL] COPPER ORES. 733 
 
 of copper, with minute quantities of both gold and silver (page 517). 
 On the thirteenth lot of the same range, in a continuation of this deposit, 
 copper pyrites like the last is disseminated through thirty feet of chloritic 
 rock. Copper pyrites also occurs in reins of quartz, in several places on 
 the ninteenth and twentieth lots of the sixth range of Ascot. 
 
 On the twenty-eighth lot of the fourth range of Ham, and near the line of 
 Wolfestown, copper ore occurs in a dolomite ; which rests upon chloritic 
 schists, and is overlaid by black glossy slates. The general course of the 
 beds in the vicinity is nearly north and south, with an eastward dip ; but Ham Mine 
 near the mine, a turn in the stratification gives them an east and west 
 direction, with a southward dip of forty-five degrees. The thickness of 
 the dolomite band is about 100 feet. It is somewhat slaty in structure, 
 and towards the summit becomes interstratified with thin layers of 
 micaceous and quartzose schists. In the upper thirty feet of the limestone, 
 yellow and variegated sulphurets of copper are disseminated in nodules 
 and lenticular masses, which have often an extent of several inches, with 
 a thickness of an inch or more. Quartz veins are also found cutting the 
 beds, and contain rich specimens of the yellow and variegated ores ; while 
 in some cases, small veins are entirely filled with the vitreous sulphuret. 
 Excavations have been made here which show the continuation of the ore- 
 bearing stratum for a distance of about 500 feet, and have yielded several 
 tons of rich ore. The north branch of the Nicolet River falls over the band 
 of dolomite at this place, furnishing an available water-power, and the 
 deposit may not' improbably prove to be of considerable importance. 
 Copper ore is also found on the twenty-second lot of the seventh range of 
 Ham, in quartz veins cutting micaceous slates. 
 
 In the township of Garthby, on the twenty-second lot of the first range, Garthby. 
 north, a large mass of iron and copper pyrites is found subordinate to the 
 stratification of the enclosing rock, which is a calcareous serpentine, dip- 
 ping to the southeast at an angle of 50. The extent of the deposit has 
 not yet been determined ; but there appears to be a breadth of about 
 twenty feet in which the two ores occur, more or less mtermingled 
 with rock. Large masses of the mineral consist of a fine-grained iron 
 pyrites, without any copper, while in other portions there is such an admix- 
 ture of copper pyrites as to afford eight per cent, of the metal. The iron 
 pyrites of this locality, when exposed to the ah*, is slowly oxydized, and 
 falls to pieces from the formation of sulphate of iron ; for the manufacture 
 of which it might be used with advantage. 
 
 The rocks of the Quebec group, from the vicinity of Quebec to the 
 extremity of Gaspe", have been studied chiefly along the coast, where 
 copper ore has as yet been found in one place only. At the mouth of the 
 Great Capucin River, four miles above Cape Chatte, small portions of copper 
 pyrites are observed in a vein of quartz in red shale. The Shickshock 
 
734 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 Mountains are composed of the chloritic and epidotic rocks of the Quebec 
 group, with serpentines containing chrome and nickel ; and similar rocks 
 occur near Gaspe* Bay, where a hill has received the name of Mount 
 Serpentine. In the vicinity of this, and about six miles from the head of 
 Gaspe* Bay, good specimens of copper pyrites are said to have been 
 obtained. The same probabilities of deposits of copper exist throughout 
 this eastern region as in the townships farther to the southwest. 
 
 In this connection, it may be mentioned that the shales and limestones 
 of the Gaspe* series at Port Daniel (page 443), contain in their lower 
 portion, small quantities of copper. This occurs both in the form of stains of 
 green carbonate, and of small nodules of vitreous copper ore, which, with 
 others of iron pyrites, are found in the shales. These Devonian rocks are 
 here cut by a small vein of heavy spar, containing a little copper pyrites, 
 with malachite. This mode of occurrence of copper ore recalls a similar 
 locality in the Carboniferous rocks of Bathurst, noticed on page 451. 
 
 It has already been stated that veins of copper ore exist in the altered 
 rocks of the Upper Silurian and Devonian age, which overlie the strata of 
 the Quebec group to the southeast. On the third and fourth lots of the 
 sixth range of Barford, the fine-grained argillaceous and micaceous slates 
 of the region dip to the northwest at an angle of about forty degrees, and 
 are traversed 'by several quartz veins, which have an underlie to the south- 
 ward at a high angle. In three of these veins, copper ore has been 
 observed ; and two of them have been opened by small excavations, and 
 have been traced considerable distances. They are about three feet in 
 breadth, and very well defined. The gangue is quartz, often translucent 
 and somewhat brownish. It is associated with a white mica, in large 
 foliated masses, and with white or greenish-white crystalline apatite. The 
 metallic contents of the vein are copper pyrites, magnetic iron pyrites, 
 molybdenite, and spathic iron, besides which small portions of dendritic 
 native copper have been found in the joints of the quartz. The quantity 
 of copper ore met with thus far in the workings is said to be encouraging, 
 and the locality is well worthy of being proved. The strata in which these 
 veins occur are geologically distinct from those of the Quebec group, and 
 their investigation may lead to important results in connection with the 
 economic mineralogy of these upper rocks ; whose age is supposed to be the 
 same with those which contain the copper and tin of Devonshire and of 
 Cornwall. It may here be remarked that the small quantities of tin ore 
 which have been found in New Hampshire, and in Maine, are supposed to 
 belong to these same upper rocks, of which they are a continuation. 
 
 The evidence which has been presented in the descriptions of the copper 
 deposits of the Quebec group, appears to show that the metal, like the iron, 
 manganese, nickel, and chrome which so often accompany it throughout 
 these rocks, was held in solution by the waters from which the sediments 
 
CHAP. XXI.] COPPER ORES. 735 
 
 of the period were deposited. By the agency probably of organic matters origin of 
 (page 574), it was reduced to the condition of a sulphuret, and precipi- 
 tated with the sediments, either in a finely divided state, or more frequently 
 in small nodules or patches,; which became interstratified with the lime- 
 stones, the slates, the diorites, and other rocks of the series. A subse- 
 quent action, probably contemporaneous with that which has metamor- 
 phosed and crystallized the rocks over a great part of their extent, 
 dissolved out portions of the copper sulphurets from these beds ; and in cer- 
 tain cases deposited them, with quartz and various spars, in the fissures of 
 the rocks ; giving rise to the veins or courses which have been described. 
 There appear to be, in this region, no facts to sustain the ancient notion 
 of the connection of metalliferous deposits with eruptive rocks ; which are 
 absent from great portions of the district. The diorites and serpentines of 
 the Quebec group have already been shown to be rocks of sedimen- 
 tary origin ; and the same may be said of the amygdaloids, which are evi- 
 dently altered argillites. The frequent similarity of these rocks, and of 
 their associated minerals, to the cupriferous strata of the same age on 
 Lake Superior, has already been alluded to as a reason for supposing that 
 the copper of the latter region is in no way connected with the intrusive 
 rocks which there accompany it (page 699). 
 
 The copper deposits of the Eastern Townships are unlike those of 
 Cornwall and of Lake Huron, in which the metal has been concentrated in 
 well-defined lodes. They are however very similar in their structure and 
 mode of occurrence to those of the same age in Norway and Sweden. 
 The analogous copper ores in the Permian slates of Mansfeld and Hesse, and 
 those of both sides of the Ural Mountains, are in like manner disseminated 
 in beds, and not in veins. Copper-bearing beds similar to those of Canada, 
 are also wrought in schistose rocks of the Quebec group, in Maryland, 
 in Tennessee, and in other parts of the United States. 
 
 With regard to the working of the copper deposits of Eastern Canada, Mining, 
 but little has yet been done. The Acton mine has afforded large quan- 
 tities of rich ores quarried from open cuttings ; and profitable workings, 
 on a smaller scale, have been undertaken at Ascot. In Leeds, the English 
 and Canadian Mining Company has expended considerable sums in system- 
 atic mining operations, which, although they have not yet been remuner- 
 ative, have proved the extent and richness of the copper beds in that vicin- 
 ity to be such as to give hopes of profit for the future. In numerous 
 other localities, as in Upton, Wickham, Durham, St. Flavien, Sutton, 
 Melbourne, Halifax, and Ham, the explorations which have been made 
 by various parties have- shown the existence of considerable quantities of 
 copper ore. In many of these localities it occurs hi peculiar conditions, 
 namely as a variegated or vitreous sulphuret, rich in copper, and spar- 
 ingly disseminated through a quartzose or argillaceous rock. Such ore 
 
736 GEOLOGY OF CANADA. [CHAP. XXL 
 
 Metallurgy, demand a particular metallurgical treatment. The loss by dressing is 
 considerable ; and in order to separate the copper from the gangue by 
 smelting, they require an addition of ores rich in sulphur ; such as those 
 from Clarke's mine in Ascot, or from Garthby. The ore of the Ascot 
 mine, with its copper pyrites and calcareous gangue, would also be an advan- 
 tageous admixture. It is much to be desired that some one of the various 
 methods which have been proposed for removing the copper in a soluble 
 
 Humid form, could be applied to these ores. In one of these processes, the cal- 
 cined or roasted ores are exposed to the combined action of air, watery 
 vapor, and the sulphurous acid evolved from the roasting of other portions 
 of the same or of other sulphurets. The sulphuric acid thus formed dis- 
 solves the oxyd of copper from the calcined ore, converting it into 
 sulphate of copper. This process is adopted at Linz, in Rhenish Germany, 
 for pyritous ores which are mixed with a great deal of quartz. In 
 Norway, iron pyrites containing three per cent, of copper, or less, is 
 partially roasted at a low heat, by which the copper, and a part of the iron, 
 are converted into soluble sulphates. Still another process is based upon 
 calcining, in a current of air, the pyritous ores (which, if very poor in 
 copper, are previously deprived, by roasting, of a part of their sulphur) with 
 a mixture of common salt, and thus converting the copper into a chlorid, 
 which is soluble in water. From the soluble copper salts obtained by 
 these various processes, the metal is afterwards precipitated, generally by 
 iron, which separates it in the metallic state. In applying any of these 
 methods to the vitreous and variegated ores of Canada, however, the quan- 
 tity of sulphur present would be insufficient to convert the whole of the 
 copper into sulphate or chlorid ; and it would be necessary to make use, 
 as in smelting them, of some poorer and more sulphurous ore. 
 
 It can hardly be doubted, that, when the copper deposits of Eastern 
 Canada are thoroughly explored, and proper means of working them and 
 of smelting their ores are adopted, they will become a source of great wealth, 
 and furnish employment to a large population. The same may be said of 
 the copper deposits along the north shores of Lakes Superior and Huron, 
 although these have the disadvantage of being farther removed from the 
 great markets. As the mining industry of that region becomes developed, 
 the sulphuretted ores which abound there, and which, unlike the native 
 copper of Michigan, require a lengthened metallurgical treatment, will be 
 smelted where fuel is most accessible. Chicago and Cleveland, which are 
 not far from great deposits of coal, will be favorable positions ; while the 
 coal-field of Michigan, which comes upon Lake Huron in Saginaw Bay, may 
 probably make that vicinity the site of copper-smelting works. Ores which 
 contain a small proportion of copper, and which cannot by dressing, or by 
 a partial smelting, be advantageously raised to a high percentage, must 
 be reduced near the mines, by some process like those already indicated; 
 
CHAP. XX NICKEL ORES. 737 
 
 but the quantity of fuel required by the present mode of treatment, is such 
 that the richer ores will still be carried to the vicinity of coal. It may 
 therefore be anticipated that those from Eastern Canada will eventually 
 find their way to the coal mines of the Lower Provinces. 
 
 The principal facts with regard to the distribution of nickel have been 
 given on pages 505-507, and it now remains to notice those localities which 
 may prove to be available sources of this valuable metal. The arsenical 
 ore already described as occurring on Michipicoten Island, has been shown 
 to be an intimate mixture of the arseniurets of copper and nickel ; different 
 portions of the same mass containing from seventeen to thirty-six per cent. 
 of nickel. These results have been confirmed by Prof. Whitney ; who, 
 on visiting the locality, found this ore in the form of nodules, having a con- 
 centric structure, and imbedded in coarsely crystalline calc-spar. These, 
 according to him, were irregularly distributed in the trappean rock, and 
 did not form a regular vein. He found in two specimens, respectively 
 thirty-one and thirty-three per cent, of nickel. Of the second nickel ore 
 from the same locality, already described as a greenish earthy ^silicate 
 of nickel, and yielding about twenty-four per cent, of nickel, little is 
 known, except that the specimens brought from the mine were filled with 
 small grams of native copper and of native silver ; and that large quan- 
 tities of the green earthy material were said to have been crushed and 
 washed to obtain these metals, the valuable ore of nickel being lost in the 
 process. The analysis of a specimen, from which the native metals had 
 not been separated, gave for one hundred parts: silver 2-35, copper 18-51, 
 and oxyd of nickel 20-85. At the present price of the latter metal, it 
 would be worth nearly as much as the accompanying silver. 
 
 The nickel ore from the Wallace Mine on Lake Huron has already been Wallace 
 noticed as a steel-grey pyritous ore, whose mineralogical composition is Minc - 
 uncertain. A mass, weighing forty-five ounces, which was regarded as an 
 average sample, was reduced to powder, and gave iron 24-78, nickel 
 8-26, arsenic (mean of two determinations) 3-57, sulphur 22-63, copper 
 0.06; = 59.30: besides silica 28-40, carbonate of lime 4-00, magnesia 
 4-40, alumina 3-21 ; = 99-31. Taking the 59-3 per cent, to represent 
 the metalliferous portion, this evidently contains 13-93 per cent, of nickel, 
 and 6-02 per cent, of arsenic ; the remainder being chiefly sulphur and 
 iron. From the small proportion of arsenic, the nickel must,, in part at 
 least, be present in the state of sulphuret ; a fact which is indeed made 
 evident by the formation of sulphate of nickel by the spontaneous oxyda- 
 tion of the ore. The nickel from this source contained about three parts 
 in a thousand of cobalt. 
 
 ww 
 
738 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 The general diffusion of nickel throughout the magnesian rocks of the 
 Quebec group has been already noticed. It has however never yet 
 been met with in any considerable quantities in these rocks, although work- 
 able deposits of its ores may reasonably be looked for in some parts of 
 Orford. their distribution (page 709). On the sixth lot of the twelfth range 
 of Orford, the sulphuret of nickel, millerite, is met with in small grains 
 and crystals, disseminated through a mixture of green chrome-garnet 
 with calc-spar, and through the adjacent rock. This ore has a brass- 
 yellow color, is soft, and somewhat resembles copper pyrites : it contains 
 sixty per cent, of nickel. Explorations were made at this place a year or 
 two since, in the hope of obtaining copper, which was supposed to be indicated 
 by the brilliant green of the garnet ; and lead, small quantities of which are 
 found in the vicinity. The ore of nickel is sparingly disseminated in small 
 grains through the garnet and calcareous spar ; and the masses submitted 
 to analysis did not yield more than one per cent, of nickel. It is perhaps 
 doubtful whether this small quantity could be extracted with profit ; but 
 the high price of nickel will allow very poor ores to be wrought to advan- 
 tage, and the deposits at Michipicoten, and at the Wallace mine, yield an 
 ore of such richness as to be worthy of farther and careful explorations. 
 The wholesale price of commercial nickel, containing ninety-six per cent, of 
 pure metal, was, in the commencement of 1861, quoted at from $1*15 to 
 $1'20 the pound ; but it is said to have since augmented in value. The 
 increasing demand for it in the manufacture of German silver and of 
 similar alloys, and its use in the coinage of the United States, of Switzer- 
 land, and of Belgium, explain its rise in price. The alloy used in the 
 Belgian mint consists of three parts of copper to one of nickel. 
 
 Native But little can be added to the facts already detailed in previous pages 
 sliver, ^h regard to the occurrence and distribution of this precious metal in 
 Canada. On page 517 will be found notices of the native silver which is 
 sometimes associated with the native copper in Lake Superior. It has there 
 already been pointed out that the copper ores of the Quebec group at 
 Upton, Acton, and Ascot have afforded small portions of silver. Fila- 
 ments of native silver have been observed at the Acton mine. As yet 
 however the quantity of silver found with these ores has not been sufficient 
 to be advantageously separated by the ordinary metallurgical processes. 
 The deposit of native silver found with copper ores at Prince's Mine, is 
 noticed on pages 517 and 708. 
 
 The argentiferous galena from Black River on Lake Superior, and that 
 from Mamainse, which gives thirty ounces of silver to the ton of lead, are 
 noticed on page 690. The lead ores which are associated, in the form 
 of interstratified masses, with the ores of copper of the Quebec group, 
 as seen from the assays of tike galena from Upton and Acton, contain but 
 
CHAP. XXL] GOLD MINES. 739 
 
 two or three ounces of silver to the ton ; a quantity which is not worth the siiver-iead. 
 cost of extracting. It is otherwise however with the galena which occurs 
 in quartz veins cutting the upper slates of this region (page 691). That 
 found with auriferous pyrites in Vaudreuil on the ChaudiSre, gave thirty- 
 seven ounces of silver to the ton of lead ; and that from Moulton Hill 
 in Ascot, sixty-five ounces. A decomposing pyrites from the latter locality 
 yields a little gold. Small quantities of gold and silver are also found 
 with copper ore in the rocks of the Quebec group in Ascot (page 517). 
 Argentiferous galena occurs in a quartz vein in St. Armand, and at the 
 Owl's Head Mountain in Potton. 
 
 It is well known that with the present improved processes so small a 
 quantity as four ounces of silver may be profitably extracted from a ton of 
 lead. The lead ores of the Laurentian rocks, with the exception of that 
 from Lake Superior just mentioned, do not however appear to contain 
 more than three or four, ounces of silver to the ton (page 518). 
 
 GOLD. 
 
 The principal facts known with regard to the geological distribution of 
 gold in Canada will be found on pages 518-520. Mention is there made 
 of a quartz vein at St. Francis, on the Chaudire ; where small grains of 
 native gold have been found imbedded in quartz, together with argentif- Gold in vein*, 
 erous galena, and sulphurets of zinc and iron, both containing gold, and with 
 arsenical pyrites. Since writing the above pages, much larger specimens 
 of gold have been found in quartz, about one hundred yards from the loca- 
 lity just mentioned. It is probable that this, and similar quartz veins, may 
 be wrought with profit ; but the gold hitherto obtained from this region has 
 been from the superficial deposits of clay, sand, and gravel, which abound 
 there, and appear to be derived from the breaking up of the rocks that 
 contain the gold-bearing veins. These deposits probably belong, in part 
 to the ancient glacial drift, or boulder formation, and in part to newer strati- 
 fied clays and gravels, which consist of the materials of this, modified 
 and arranged by the subsequent action of water. On the Magog River, drift> 
 above Sherbrooke, particles of gold occur in a hard-bound gravel, 156 feet 
 above the level of the St. Francis, near by. On the Famine Eiver, there 
 is met with an extensive deposit of clay, everywhere overlaid by sand and 
 gravel. Along the banks of the river, a stratum of the oxyds of iron and 
 manganese, in some parts six or eight inches thick, is seen near the top of 
 the gravel, filling interstices among pebbles of the rocks of the region. 
 Gold is found in this overlying gravel, as well as in the clay beneath ; both 
 of which deposits appear to belong to the modified drift. It is met with in 
 similar conditions throughout the banks of stratified material on the Met- 
 germet, which attain a height of fifty feet above the bed of the river. 
 Gold also occurs still more abundantly in the recent alluvions, found in the 
 beds and along the flats of the streams which traverse this region, and in 
 
T40 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 time of floods wash down the clay and sand from their banks, depositing 
 the heavier portions along their course. In this way the gold is often 
 caught in the fissures of the clay slates, which frequently form the under- 
 lying rock, and are rich in alluvial gold. 
 
 The auriferous drift of Eastern Canada is spread over a wide area 
 on the south side of the St. Lawrence, including the hill country belong- 
 ing to the Notre Dame range, and extending thence south and east to 
 the boundary of the province. These wide limits are assigned, inasmuch 
 as although gold has not been everywhere found in this region, the same 
 mineralogical characters are met with throughout ; and, in its continuation 
 southward, in Plymouth and elsewhere in Vermont, considerable quantities 
 of gold have been obtained from the alluvial deposits. In Canada, gold has 
 been found on the St. Francis River from the vicinity of Melbourne to 
 Sherbrooke,in the townships of Westbury, Weedon, and Dudswell, and on 
 Lake St. Francis. It has also been found on the Etchemin, and on the 
 Chaudire and nearly all its tributaries, from the seigniory of St. Mary to 
 the frontier of the state of Maine ; including the Bras, the Guillaume, the 
 Riviere des Plantes> the Famine, the Du Loup, and the Metgermet. Sev- 
 eral attempts have been made to work these alluvial deposits for gold, in the 
 seigniories of Vaudreuil, Aubert-Gallion, and Aubert de 1'Isle, but they have 
 been successively abandoned, and it is difficult to obtain authentic accounts 
 of the result of the various workings, although it is known that very consid- 
 erable quantities of gold were extracted. The country people still, from 
 time to time, attempt the washing of the gravel, generally with the aid of a 
 pan, and are occasionally rewarded by the discovery of a nugget of consid- 
 Rivieredu erable value. In the years 1851 and 1852, an experiment of this kind, 
 Loup. on a considerable scale, was tried by the Canada Gold Mining Company, in 
 
 the last named seigniory, on the RiviSre du Loup, near its junction with 
 the Chaudiere. The system adopted for the separation of the gold from the 
 gravel was similar to that used in Cornwall in washing for alluvial tin, and 
 the water for the purpose was obtained from a small stream adjoining. 
 Great difficulties were however met with, from a deficient supply of water 
 during the summer months. The gravel from about three eighths of an 
 acre, with an average thickness of two feet, was washed during the summer 
 of 1851, and yielded 2,107 pennyweights of gold ; of which 160 were in 
 the form of fine dust, mingled with about a ton of black iron-sand, the 
 heavy residue of the washings. There were several pieces of gold 
 Gold washings, weighing over an ounce. The value of this gold was $1,826, and the 
 whole expenditure connected with the working $1,643 ; leaving a profit of 
 $182. In this account is, however, included $500 lost by a flood, which 
 swept away an unfinished dam ; so that the real difference between the 
 amount of the wages and the value of the gold obtained should be stated 
 at $682. The average price of the labor employed was sixty cents a day. 
 
CHAP. XXL] GOLD MINES. 741 
 
 In 1852, about five eighths of an acre of gravel were washed at this 
 place, and the total amount of gold obtained was 2,880 pennyweights, 
 valued at 82,496. Of this, 307 pennyweights were in the form of fine 
 'dust mixed with the iron-sand. A portion was also found in nuggets or 
 rounded masses of considerable size. Nine of these weighed together 
 468 pennyweights, the largest being about 127, and the smallest about 11 
 pennyweights. Portions both of native platinum and of iridosmine were Platinum, 
 obtained in the washing, but the quantity of these was too small to be of 
 any importance. The washing season lasted from the twenty-fourth of May 
 to the thirtieth of October, and the sum expended for labor was $1,888, 
 leaving a profit of $608. A part of this expenditure was, however, for 
 the construction of wooden conductors for bringing the water a distance of 
 about 900 feet from the small stream. As this work would be available 
 for several years to come, a proper allowance made for it would leave a 
 profit in the year's labor of about $680. It thus appears that from an 
 acre of the gravel, with an average thickness of two feet, there were taken 
 $4,323 of gold; while the expenses of labor, after deducting, as above, all 
 which was not directly employed in extracting gold, were $2,957, leaving 
 a profit of $1,366. The result of a week's working at this place, under 
 the inspection of a member of the Geological Survey, in 1852, showed a 
 yield of 143 pennyweights of gold, valued at $124 ; while the amount paid 
 for wages to the miners during that time was $60. In a previous trial on 
 the Touffe des Pins, a small tributary of the Chaudi^re, sixty bushels of 
 the gravel from the bed of the stream were washed in a day, by means of 
 a rocker, or kind of shaking table, and yielded 440 grains of gold, or about 
 seven and one third grains to the bushel. The gold of this region is, as 
 usual, alloyed with a portion of silver. The fineness of the gold-dust was 
 871 thousandths. Another sample of gold, in thin scales, gave 892, and 
 small masses 864 ; while a nugget from Vaudreuil yielded 867 thou- 
 sandths of gold. 
 
 The composition of the heavy black sand, which is obtained in the slack sand, 
 washing of the gravel, has been noticed on page 520. It is a mixture of 
 magnetic oxyd and peroxyd of iron, with chromic and titanic iron ores. 
 Rolled masses of these ores, sometimes several pounds in weight, are also 
 met with in the gravel. Small crystals of rutile were obtained in the wash-' 
 ings ; and grains of red and pink sand, chiefly composed of grains of gar- 
 nets, but including a few minute crystals having the form of zircon. The 
 gold was not unfrequently incrusted with an earthy coating of black oxyd 
 of manganese ; and some specimens were white on the surface, from a 
 coating of mercury ; which is, however, at once driven off by heat, leaving Mercury, 
 the gold of its natural color. A single well-worn and rounded mass of copper, 
 native copper, several ounces in weight, was found in the gravel in this 
 region ; and in the washings at the Rividre du Loup, were large quantities 
 of leaden shot of various sizes, probably scattered by sportsmen. 
 
742 GEOLOGY OP CANADA. [CHAP. XXI. 
 
 Although the greater part of the gold at the RiviSre du Loup was 
 extracted from the gravel on the alluvial flats by the river side, a portion was 
 obtained by washing the material taken from the banks above. As has 
 been before remarked, the distribution of the gold-bearing drift over the 
 surface of the country took place before the formation of the present water- 
 courses ; and the greater richness of the gravel from their beds is to be 
 ascribed to the fact that these rapid streams hare subjected the earth to a 
 partial washing, carrying away the lighter materials, and leaving the gold 
 with the heavier matters behind. According to Mr. Blake, it is found in 
 California that the gold in the diluvial deposits, which have not been subse- 
 quently disturbed by the streams ? is not uniformly distributed, but is 
 accumulated here and there in quantities greater than in other places. 
 During the first deposition of the earth and gravel, the precious metal 
 became accumulated in depressions of the surface rock, constituting what 
 are there called pockets by the miners. 
 
 It would appear from the facts here given that the quantity of gold in 
 the valley of the Chaudire is such as would be remunerative to skilled 
 labor, and should encourage the outlay of capital. There is no reason for 
 supposing that the proportion of the precious metal to be found along the 
 St. Francis, the Etchemin, and their various tributaries, is less considerable 
 Hydraulic than that of the Chaudire. What is called the hydraulic method of 
 process. was hing such deposits is adopted on a great scale in California, and to some 
 extent in the states of Georgia and North Carolina. "In this method, 
 the force of a jet of water, with great pressure, is made available, both for 
 excavating and washing the auriferous earth. The water, issuing in a con- 
 tinuous stream, with great force, from a large hose-pipe, like that of a fire- 
 engine, is directed against the base of a bank of earth and gravel, and 
 tears it away. The bank is rapidly undermined, the gravel is loosened, 
 violently rolled together, and cleansed from any adhering particles of gold ; 
 while the fine sand and clay are carried off by the water. In this manner 
 hundreds of tons of earth and gravel may be removed, and all the gold 
 which they contain liberated and secured, with greater ease and expedition 
 than ten tons could be excavated and washed in the old way. All the 
 earth and gravel of a deposit is moved, washed, and carried off through 
 long sluices, by the water, leaving the gold behind. Square acres of earth 
 on the hill sides may thus be swept away into the hollows, without the aid 
 of a pick or a shovel in excavation. Water performs all the labor, moving 
 and washing the earth, in one operation ; while in excavating by hand, the 
 two processes are of necessity entirely distinct. The value of this method, 
 and the yield of gold by it, as compared with the older one, can nardly be 
 estimated. The water acts constantly, with uniform effect, and can be 
 brought to bear upon almost any point, where it would be difficult for men 
 to work. It is especially effective in a region covered by trees, where the 
 
CHAP. XXL] GOLD MINES. 743 
 
 tangled roots would greatly retard the labor of workmen. In such places, Blake's 
 the stream of water washes out the earth from below, and tree after tree d< 
 falls before the current, any gold which may have adhered to the roots 
 being washed away. With a pressure of sixty feet, and a pipe of from 
 one and a half to two inches aperture, over a thousand bushels of earth 
 can be washed out from a bank in a day. Earth which contains only one 
 twenty-fifth part of a grain of gold, equal to one fifth of a cent in value, 
 to the bushel, may be profitably washed by this method ; and any earth or 
 gravel which will pay the expense of washing in the old way, gives enor- 
 mous profits by the new process. To wash successfully in this way requires 
 a plentiful supply of water, at an elevation of from fifty to ninety feet 
 above the bed-rock, and a rapid slope or descent from the base of the 
 bank of earth to be washed, so that the waste water will run off through 
 the sluices, bearing with it gravel, sand, and the suspended clay." 
 
 The above description has been copied from a report on the gold mines 
 of Georgia, by Mr. William P. Blake, who had carefully studied this 
 method of mining in California, and by whose recommendation it has been 
 introduced into the Southern States. He tells us that in the case of a 
 deposit in North Carolina, where ten men were required, for thirty-five days, 
 to dig the earth with pick and shovel, and wash it in sluices ; two men, with 
 a single jet of water, would accomplish the same work in a week. The 
 great economy of this method is manifest from the fact that many old 
 deposits in the river beds, the gravel of which had been already washed 
 by hand, have been again washed with profit by the hydraulic method. He California, 
 tells us that in California the whole art of working the diluvial gold deposits 
 was revolutionized by this new method. The auriferous earth, lying 
 on hills, and at some distance above the level of the water-courses, would, 
 in the ordinary methods, be excavated by hand, and brought to the water; 
 but, by the present system, the water is brought by aqueducts to the gold 
 deposits, and whole square miles, which were before inaccessible, have 
 yielded up their precious metal. It sometimes happens, from the irregular 
 distribution of the gold in the diluvium in California, that the upper portions 
 of a deposit do not contain gold enough to be washed by the ordinary 
 methods ; and would thus have to be removed, at a considerable expense, 
 in order to reach the richer portions below. By the hydraulic method, 
 however, the cost of cutting away and excavating is so trifling, that there 
 is scarcely any bank of earth which will not pay the expense of washing 
 down, in order to reach the richer deposits of gold beneath. 
 
 The aqueducts or canals for the mining districts of California are sel- 
 dom constructed by the gold workers themselves, but by capitalists, who 
 rent the water to the miners. The cost of one of these canals, carrying 
 the waters of a branch of the Yuba River to Nevada County, was esti- 
 mated at a million of dollars ; and another one, thirty miles in length, 
 
744 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 cost of running to the same district, cost 1500,000. The assessed value of these 
 various canals in 1857 was stated to be over four millions of dollars, of 
 which value one half was in the single county of Eldorado. The Bear 
 River and Auburn Canal is sixty miles in length, three feet deep, and 
 four feet wide at the top, and cost in all 11,600,000 ; notwithstanding 
 which, the water rents were so great that it is stated to have paid a yearly 
 dividend of twenty per cent. ; while other similar canals paid from three to 
 five and six per cent., and even more, monthly. The price of the water 
 was fixed at so much the inch, for each day of eight or ten hours. This 
 price was at first about three dollars, but by competition it has now been 
 greatly reduced. 
 
 From these statements, it will be seen that the great riches which have 
 of late years been drawn from the gold mines of California, have not been 
 obtained without the expenditure of large amounts of money and engineer- 
 ing skill. This last is especially exhibited in the construction of these great 
 canals, and the application of the hydraulic method to the washing of 
 auriferous deposits, which were unavailable by the ordinary modes of 
 working, on account of their distance from water-courses, or by reason of 
 the small quantity of gold which they contain. 
 
 In order to judge of the applicability of this method of washing to our 
 own auriferous deposits, a simple calculation based upon the experiments 
 upon the Riviere du Loup will be of use. It has been shown that the 
 washing of the ground over an area of one acre, and with an average 
 depth of two feet, equal to 87,120 cubic feet, gave, in round numbers, 
 about 5000 pennyweights of gold, or one and thirty-eight hundredths 
 grains to the cubic foot ; which is equal to one and three-quarters grains of 
 gold to the bushel. Now, according to Mr. Blake, earth containing one 
 forty-fourth part of this amount, or one twenty-fifth of a grain of gold, 
 can be profitably washed by the hydraulic method ; while the labor of two 
 men, with a proper jet of water, suffices to wash one thousand bushels 
 in a day ; which, in a deposit like that of Riviere du Loup, would contain 
 about seventy-three pennyweights of gold. It is probable however that a 
 Certain portion of the finer gold dust, which is collected in the ordinary 
 process, would be lost in working on the larger scale. It has already 
 been shown that the gold in Canada is not confined to the gravel of the 
 river channels, and the alluvial flats ; but is found on the Metgermet and 
 St. Francis Rivers, at from fifty to a hundred and fifty feet above their 
 beds ; and although its proportion were to be many times less than in the 
 gravel of the Riviere du Loup, these thick deposits, which extend over great 
 areas, might be profitably worked by the hydraulic method. The fall in 
 most of the tributaries of the Chaudidre and of the St. Francis, throughout 
 the auriferous region, is such that it would not be difficult to secure a supply 
 of water with a sufficient head, without a very great expenditure in the 
 
CHAP. XXI.] GOLD MINES. 745 
 
 construction of canals ; and it may reasonably be expected that before long 
 the deposits of gold-bearing earth, which are so widely spread over south- 
 eastern Canada, will be made economically available. 
 
 It has been already mentioned on page 517, that the native silver from Lake 
 Prince's Mine on Lake Superior contains small portions of gold. The Su P erior < 
 parallelism in age and mineral contents between the Upper copper-bearing 
 rocks of this region, and the Quebec group of Eastern Canada, makes it 
 not improbable that gold may one day be added to the list of the mineral 
 riches of Lake Superior. The gold of Eastern Canada appears not how- 
 ever to.be confined to the rocks of the Quebec group. Although it occurs 
 in these with the copper ores of Ascot and Leeds, and in the garnet-rock 
 of Vaudreuil, it is also found with mispickel and argentiferous galena in 
 veins of quartz which traverse the upper slates. 
 
 The gold of Nova Scotia occurs with pyrites, mispickel, and native cop- Nova 
 per, in quartz veins, which traverse a great belt of schistose rocks along the Scotia< 
 Atlantic coast. These rocks, which were described by Dr. Dawson in his 
 Acadian Geology, and were by him regarded as altered palaeozoic strata, 
 perhaps of Lower Silurian age, consist of gneiss with argillites and mica- 
 schists holding staurotide, interstratified with quartzites, and penetrated by 
 granite. In the general absence of anything like the magnesian strata of 
 Eastern Canada, and in its other lithological characters, this series 
 appears distinct from the Quebec group. The age of these rocks is thus 
 uncertain. At Cape Canseau, dark colored argillites holding crystals of 
 ciiiastolite are met with ; and the chiastolite of Eastern Canada belongs to 
 the upper slates, which are also gold-bearing. In Nova Scotia, although 
 tibe gold occurs throughout this coast series, it is also said to be found at 
 Cape Porcupine in rocks of the same age as these upper slates. This 
 probable identification of a part of the gold formation of Nova Scotia with 
 the altered Upper Silurian and Devonian strata of Eastern Canada, gives an 
 additional economic interest to these rocks, whose metalliferous character 
 has already been insisted upon, on pages 711 and 734. Besides forming 
 the southeastern limit of the Quebec group from Stanstead to Gaspe* 
 they occupy a considerable area in the third synclinal, extending from Lake 
 Memphremagog northward into Ham and Stoke (page 718). 
 
 II. MINERALS USED IN CERTAIN CHEMICAL MANUFACTURES. 
 
 Under this head it is proposed to notice several substances which could 
 not be considered in the previous class, and which are employed in cer- 
 tain chemical processes, or require peculiar chemical treatment to render 
 them available. The present class will include iron pyrites, and the ores 
 of chrome, cobalt, manganese, titanium, and molybdenum ; together with 
 the native carbonate of magnesia, which may be used for the preparation 
 of magnesia and of its salts. 
 
746 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 IRON PYRITES. 
 
 Of the three species which are mentioned under this head on page 513, 
 only one is of economic importance, the common cubic pyrites or bi- 
 
 suiphuret sulphuret of iron. This mineral, when in a state of purity, consists of 46-7 
 
 of iron ' parts of iron, and 53-3 of sulphur in 100-0 parts. It is never resorted to 
 as an ore of iron, but is extensively employed as a source of sulphur, and 
 for the manufacture of copperas, which is a sulphate of iron. When iron 
 pyrites is exposed to an intense heat, in proper vessels, it gives off one 
 half of its sulphur, which, by proper arrangements, may be collected in the 
 form of commercial sulphur, or brimstone. The temperature required to 
 obtain this result is, however, very elevated ; and in practice it is found 
 convenient to distil at a less heat, by which means only thirteen or four- 
 teen per cent, of sulphur are obtained from the pyrites. This process is, 
 however, but seldom resorted to at present ; and as the great use of sulphur 
 in the arts is in the fabrication of sulphuric acid, it is found more advan- 
 tageous to calcine the iron pyrites in furnaces of a peculiar construction. 
 By this means, almost the whole of the sulphur is expelled in the form of 
 sulphurous acid,which is conducted at once to the leaden chambers employed 
 
 its uses. in the fabrication of sulphuric acid. Formerly large quantities of sulphur 
 were imported from Sicily for this manufacture ; but within the last few 
 years it has been almost entirely replaced by pyrites, which is brought in 
 large quantities from Spain and Portugal, and also from Belgium and Ire- 
 land. In a recent note on the statistics of the alkali manufacture in the 
 United Kingdom, it is stated that the consumption of pyrites for the year 
 1862 reached 264,000 tons. The value of good iron pyrites in England is 
 said to be a little over ten dollars the ton ; but the pyrites imported from 
 Spain and Portugal, contains a small but variable amount of copper, which 
 is extracted from the calcined residue, and thus adds very much to the 
 value of the mineral. Formerly, from eight to ten per cent, of sulphur 
 remained behind in the calcined pyrites, and was lost; but by recent 
 improvements this loss is reduced to two per cent. 
 
 sulphuric In order to give some idea of the great importance of iron pyrites and of 
 its products, in a manufacturing point of view, it must be said that sulphuric 
 acid, which is now for the most part manufactured from pyrites, is the 
 agent used for decomposing common salt for the manufacture of soda ; in 
 its various forms of soda-ash, carbonate of soda, and caustic soda. 
 From this decomposition is also obtained hydrochloric acid : this is used 
 in the manufacture of chlorine, and of bleaching powder or chlorid of 
 lime, which are indispensable in the bleaching of cotton, linen, and the 
 materials for paper. Besides this, the manufactures of soap and glass, 
 and many other chemical products, are dependent upon the soda thus 
 obtained. The sulphuric acid is also used for the manufacture of nitric acid, 
 
CHAP. XXI.] IRON PYRITES. 747 
 
 of superphosphate of lime, of alum, and many other products ; all of which 
 are generally manufactured in the vicinity of sulphuric acid and alkali 
 works. Large quantities both of sulphuric acid and soda are now con- 
 sumed in the refining and de-odorizing of petroleum and of coal oil. 
 
 The value of the products of the alkali manufacture in Great Britain 
 during the last year is stated at 2,500,000. Of this about 1,000,000 
 was manufactured in South Lancashire ; where 3,110 tons of sulphuric acid 
 are consumed weekly for the decomposition of 2,600 tons of salt. Besides 
 this, 700 tons of the acid are employed for other purposes, making a 
 weekly total of 3,810 tons of sulphuric acid manufactured in that district 
 alone : the greater part of this is from pyrites. These details are taken 
 from a report on the chemical manufactures of South Lancashire made to 
 the British Association in September, 1861, by Messrs. Schunck, Roscoe, 
 and Smith, and serve to show the immense importance, to a manufacturing 
 country, of an abundant source of sulphur. The time will come, sooner or 
 later, when our increasing industry will be sufficient to warrant the estab- 
 lishment in Canada of manufactures of chemical products ; and should the 
 present processes still continue to be employed, the deposits of iron pyrites 
 will then become available. 
 
 Iron pyrites is also employed in another important manufacture ; that of copperas, 
 sulphate of iron or copperas, which is very extensively used in dyeing and 
 m other chemical processes. According to the report cited above, eighty 
 tons of this salt were in 1861 manufactured weekly in South Lancashire. 
 For half a century the American market has been to a large extent sup- 
 plied by the copperas which is manufactured from a bed of iron pyrites in 
 Stafford, Vermont. The process of manufacture is very simple. The 
 pyrites, which in some cases is subjected to a preliminary roasting, is 
 broken into small pieces, and placed in heaps beneath sheds, and upon 
 water-tight floors. It is then from time to tune moistened with water, 
 which favors the oxydation of the mass at the expense of the oxygen of 
 the air. After some time, the pyrites heats, crumbles, and is in great part 
 converted into a soluble sulphate of iron, which is dissolved out by water, 
 and, from the floors below, is led into boilers, in which it is evaporated to 
 such a point, that by cooling, crystals of the sulphate of iron are deposited. 
 
 The most considerable deposit of pyrites known in Canada is one occur- Eiizabethtown. 
 ring on the nineteenth lot of the second range of Eiizabethtown, near 
 Brockville. It probably forms a great interstratified mass in the rocks of 
 the Laurentian system ; but the locality has not been sufficiently explored 
 to determine either its extent, or its relations to the strata. According to 
 Mr. Macfarlane, an excavation of fifty by thirty feet has been made in the 
 mass without coming to the limit of it in either direction. The pyrites, 
 which is very pure, and free from earthy admixture, is of two varieties, the 
 one being somewhat porous and dull, with a greenish hue, and the other 
 
T48 GEOLOGY OF CANADA. [CHAP. XXI 
 
 compact, massive, with a brilliant lustre, and a somewhat conchoidal frac- 
 ture. Both varieties contain a small proportion of cobalt, which in the latter 
 is equal to five or six thousandths of the oxyd of cobalt, besides traces of 
 copper. These metals might be extracted from the residue left after the 
 calcination of this pyrites for the manufacture of sulphuric acid ; and under 
 the head of Cobalt, it is proposed to give some account of the mode of 
 separating this valuable material from the pyrites. It is said that other 
 large deposits of this mineral occur in this vicinity ; and localities which have 
 not yet been examined are mentioned on page 513. The great bed of 
 Garthby. iron and copper pyrites occurring at Garthby (page 733), and another on 
 the sixth lot of the ninth range of Ascot, will also furnish large amounts 
 of iron pyrites. These 'beds occur in the same formation as the pyrites of 
 Stafford in Vermont, which like them is associated with copper pyrites. 
 Iron pyrites also abounds in the syenitic gneiss near Portage du Fort, 
 particularly on the twenty-first lot of the second range of Clarendon. 
 
 CHROMIUM. 
 
 chromic The occurrence of the compounds of chrome, or chromium, in the rocks 
 
 of Canada, is described on page 504. The chrome used in the arts is always 
 obtained from the substance which is known as chromic iron ore, or some- 
 times, incorrectly, chromate of iron. This is a black mineral, somewhat 
 resembling magnetic iron ; from which however it is distinguished by the 
 color of its streak and powder, which are dark brown, and by the fact that 
 it is not attracted by the magnet. This ore is composed of the oxyds of 
 chrome and iron ; which are however occasionally replaced, in part, by alu- 
 mina and magnesia ; so that its composition is variable. The analyses of 
 different specimens of the pure ore give from forty to over sixty per cent, 
 of the green oxyd, or sesquioxyd of chrome ; but inasmuch as the ore is 
 often mingled with a greater or less amount of earthy matter, the propor- 
 tions of oxyd of chrome in many commercial samples, may fall considerably 
 below the numbers just given. 
 
 chromate of The compound of chromium chiefly used in the arts is the combination 
 of chromic acid with potash, known as the bichromate of potash, from which 
 are prepared both red and yellow chromates of lead ; the latter being the 
 pigment known as chrome-yellow. The green oxyd of chromium is also 
 prepared from this salt, and is used as an indellible green color in painting, 
 and for the preparation of an indestructible green printing-ink. Large 
 quantities of the bichromate of potash are used in dyeing, and in calico- 
 printing ; and according to the report above cited, the quantity of this salt 
 manufactured weekly in South Lancashire was, in 1861, fourteen tons. 
 This salt consists of one equivalent or forty-seven parts of potash, and two 
 equivalents or one hundred and two parts of chromic acid. Of this latter, 
 
CHAP. XXI.] CHROMIC IRON. 749 
 
 fifty-one parts correspond to thirty-nine parts of the green or sesquioxyd 
 of chrome ; and although the metal exists in this latter form in the ores, it 
 is now usual for commercial purposes to give the percentage of chromic 
 acid which these will yield. Thus the chromic iron from Bolton, which 
 gives by analysis 45*9 per cent, of oxyd of chromium, would yield sixty 
 per cent, of chromic acid. Rich ores of this kind are said to be worth hi 
 Baltimore, from whence large quantities are shipped, one dollar per ton, 
 for each unit of chromic acid. This agrees closely with the price offered 
 for the chromic iron from Ham, to be noticed below. Samples of two 
 barrels from this locality, sent to Glasgow and to London in 1861, gave 
 from 43*7 to 44-1 per cent, of oxyd of chrome. The mean of these, 43-9, 
 equals 57*4 per cent, of chromic acid, and the prices offered for this ore 
 in London, and in Glasgow, were respectively 11 10s. and <12 sterling 
 the ton. 
 
 This valuable mineral is met with in considerable quantities in several 
 localities among the serpentines of Eastern Canada. On the fourth lot of Ham. 
 the second range of Ham is found the ore mentioned above. It forms a 
 lenticular bed hi the serpentine, having a thickness of about fourteen 
 niches. About ten tons of the ore, of which that sent to England was a 
 sample, were extracted from seven square fathoms in the plane of the bed. 
 Farther to the northeast, on a small island in Breeches Lake in Garthby, 
 there is a considerable amount of chromic iron in disseminated crystals, 
 running in bands through serpentine. It is not however probably in 
 sufficient quantity to be wrought with profit. On the twenty-third lot of 
 the seventh range of Bolton is a bed of chrome ore from one to two feet hi Boiton. 
 thickness, in serpentine. The bed dips eastward, at an angle of about 
 eighty degrees, and the ore appears to occur in detached masses of from 
 fifty pounds to half a ton in weight. The assay of a portion of. this ore, 
 as stated above, gave 60-0 per cent, of chromic acid. Chrome ore has 
 also been met with on the twenty-second lot of the sixth range of Mel- Melbourne, 
 bourne, where lenticular masses of it, from six to nine inches in thickness 
 are found running in beds in serpentine. It is probable that the ore will 
 be met with in many other parts of this region. A boulder of several 
 hundred pounds weight was many years since found near Lake Memphra- 
 magog, and was very rich in chrome, yielding not less than 65'0 per cent. 
 of chromic acid. On Mount Albert in Gaspe*, which is composed of Gasps, 
 serpentine, loose masses of chrome ore, sometimes weighing twenty pounds, 
 were traced for half a mile along the strike of the rock, and probably 
 indicate the presence of a bed of the mineral in the vicinity. 
 
 The principal supplies of this ore are now obtained from the states of 
 Pennsylvania and Maryland, and from Norway. The annual consump- 
 tion for the manufactories of South Lancashire alone, must be equal to 
 about 1000 tons of ore , yielding fifty per cent, of chromic acid. The process 
 
750 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 of manufacturing the bichromate of potash is one which might, as Mr. 
 Macfarlane has suggested, very well be carried on in this country. It 
 consists simply in calcining the finely ground ore with crude potash, in a 
 proper furnace, exposed to a current of air> by which the chromic oxyd is 
 acidified, and unites with the potash. The resulting mass is lixiviated 
 with water, and the solution, being mixed with a certain amount of sul- 
 phuric acid, furnishes by evaporation crystallized bichromate of potash. In 
 the absence of sulphuric acid, a crude neutral chromate of potash might 
 readily be prepared by simple evaporation, and shipped to England, to be 
 there converted into bichromate. The cheapness and facility with which 
 the ore, the potash, and the requisite fuel may be obtained hi the Eastern 
 Townships, are such as to offer encouragement for the working of the 
 chrome ores in the country. 
 
 COBALT. 
 
 This metal is associated in small quantities with the ores of nickel in 
 Canada, as has been noticed on page 506. The only mineral as yet known 
 which can be made available as a source of cobalt is, however, the great 
 deposit of iron pyrites already described as occurring at Elizabethtown ; 
 cobaitiferous the brilliant compact variety of which yields from 0'5 to 0-6 per cent, of 
 pyrites. oxyd of cobalt. Mr. Macfarlane has made some experiments on the prac- 
 ticability of extracting profitably this small amount of cobalt from the ore. 
 According to him, 1,000 parts of the finely pulverized pyrites are mixed 
 with 100 parts of sea-salt, and calcined in a muffle, until the perchlorid of iron, 
 at first formed, begins to be decomposed with the evolution of chlorine gas. 
 The matter being then removed, and cooled, gives to water a solution, 
 which, besides unaltered sea-salt and sulphate of soda, contains a trace 
 of perchlorid of iron, with chlorids of cobalt and copper, equal to 6'0 parts 
 of oxyd of cobalt and 1*5 of oxyd of copper. By the careful -addition of a 
 solution of carbonate of soda, the iron and copper may be first separated, 
 and the cobalt subsequently thrown down as a carbonate, and converted 
 by calcination into the black oxyd, in which form it is sold in commerce ; 
 its price in the English market being from eleven to thirteen shillings, or 
 about three dollars, the pound. It is employed in giving a blue color to 
 glass and porcelain, and in the preparation of the blue pigment known as 
 smalt, and the rare and costly color called The'nard's blue, which is a phos- 
 phate of cobalt. Mr. Macfarlane estimates the cost of treating a ton of 
 the cobaitiferous pyrites to be as follows : excavation, $ 3*00, roasting 0-25, 
 freight to the factory $2*50} stamping 0'50, calcining $6-00, lixiviation, 
 precipitation, etc., f 1-25, freight to market, agency, etc., 0-50 ; = $14'00. 
 Supposing that, in the large way, two thirds only of the cobalt are sepa- 
 rated, there would be obtained from a ton, eight pounds of the oxyd, which, 
 at $3.00 the pound, is equal to $24-00 ; leaving thus a large margin for 
 profit. (Canadian Naturalist, June, 1862.) 
 
CHAP. XXL] COBALT AND MANGANESE. 751 
 
 In this calculation the sulphur is supposed to be for the most part expelled cobalt. 
 in the roasting, after which the ore is crushed and mixed with a small pro- 
 portion of salt, and calcined in a reverberating furnace. In this way the 
 sulphur is entirely lost ; but in case this pyrites were used for the manufac- 
 ture of sulphuric acid, the cobalt could be advantageously extracted from 
 the residue, and in this way the ore might probably be shipped to Liver- 
 pool with advantage. Cobalt ores are now rare, and much sought after, so 
 that an abundant supply of any cobaltiferous mineral attracts the attention of 
 the English manufacturers, who applied for, and received for trial, a portion 
 of the large specimen of this pyrites which was sent to the International 
 Exhibition of 1862. It will be recollected that cobaltiferous pyrites has 
 been described as occurring with the copper ores of Escott, and also in 
 D'Aillebout ; so that it is not improbable that other and more abundant 
 sources of cobalt may be found among the minerals of the Laurentian 
 rocks. 
 
 MANGANESE. 
 
 The few localities in^which the peroxyd of manganese has been met Manganese, 
 with in Canada, are noticed on page 507. It has not as yet been found in 
 sufficient purity or abundance to be of economical importance ; but is men- 
 tioned in this chapter to call attention to the importance of the native 
 oxyds of manganese, and to the fact that valuable mines of them have been 
 found in the adjoining state of Vermont, in the continuation of the rocks of 
 the Eastern Townships, so that it is not unreasonable to expect that simi- 
 lar deposits of manganese may be met with in that part of the province. 
 Large amounts of the oxyd have been raised in Brandon and Chittenden, 
 Vermont, and shipped to England ; where great quantities of it are con- 
 sumed, chiefly in the manufacture of chlorine for bleaching purposes. 
 Manganese, in different forms, is also used to some extent in dyeing and in 
 calico-printing, and in the coloring of glass and earthen ware. The supply 
 of manganese is in great part obtained from Germany ; and for the year 
 1862, it is said to have equalled 33,000 tons for Great Britain alone. 
 
 At Bachewanung Bay, on Lake Superior, near the southwest end of the Bachewanung 
 Upper Canada Mining Company's location, and not far from the shore, is Bay - 
 a large vein of manganese ore, running north and south, and from fifty to 
 sixty feet wide. It is described as presenting the aspect of a succession 
 of small knobs, in which, mixed with a reddish trappean rock, are numerous 
 strings of the ore, associated with quartz and calc-spar, and occasionally 
 with octahedral crystals of fluor. The ore, which is massive with small 
 geodes of crystals, is described by Prof. Hadley as manganite, or hydrous 
 sesquioxyd of manganese, which for manufacturing purposes is inferior to 
 the peroxyd. A specimen was found by assay to be equal to sixty per cent, 
 of peroxyd of manganese. 
 
752 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 The following are the localities in which deposits of oxyd of manganese 
 have been met with in Eastern Canada. It is generally in the form of the 
 earthy hydrated peroxyd, commonly known as wad or bog manganese, and 
 
 man* 17 a PP ears to nave formed under conditions similar to bog iron ore. Like this 
 
 ' substance, it includes more or less sand and clay, and it is often mixed 
 
 with a considerable proportion of peroxyd of iron. On the twenty-second 
 
 Boiton lot of the twelfth range of Bolton, a layer of earthy manganese, from 
 three to six inches in thickness, was observed, resting upon the edges of a 
 mass of clay-slate, and filling up the interstices. Its extent was only a few 
 hundred yards, and the ore contained but twenty-six per cent, of peroxyd 
 of manganese. A deposit of this material was also observed on the twenty- 
 
 stanstead. fourth lot of the fourth range of Stanstead, but it did not appear to be more 
 important than the last. On the ninth lot of the tenth range of the same 
 township, the same ore is met with near the surface of a bed of sand, over 
 an area of about two acres, in which it occurs in patches, sometimes two 
 or three yards in diameter, and a foot in thickness. These are made up 
 of irregular nodular masses, which, when washed from the adhering sand, 
 contain thirty-seven per cent, of peroxyd of manganese. 
 
 In the township of Tring, near its eastern limit, and along the road 
 leading from Lambton to St. Francis, manganese was observed for a little 
 distance on both sides of the road, and to the north became a foot in thick- 
 ness. It gave by analysis twenty-five per cent, of peroxyd. The same 
 ore was observed in the seigniory of Aubert-Grallion, for nearly half a mile 
 along the west bank of the Chaudiere River, opposite the mouth of the 
 Famine. As in the locality mentioned in Stanstead, it occurs in nodular 
 masses, which in some places form patches of a few feet in breadth, with a 
 
 st. Mary, thickness of from two to four inches. It contains twenty per cent, of per- 
 oxyd. In the seigniory of St. Mary, at the junction of the Frampton road 
 with that between the second and third ranges, manganese was observed 
 over an area of a few yards, with a thickness, in some places, of two feet, 
 and was also found in other places near by. This ore gave thirty per cent, 
 of peroxyd. In the seigniory of St. Anne de la Pocatiere, a bed of man- 
 ganese was observed about three fourths of a mile southeast from the 
 church, beneath a cultivated field. Its extent could not well be deter- 
 mined, but it contained thirty-eight per cent, of peroxyd. In the seigniory 
 of Cacouna, at the village of La Plaine, on the land of Mr. Stanislaus 
 Roy, manganese was observed over an area of a few yards, forming a bed 
 four or five inches in thickness, of nodules imbedded in sand. In the 
 neighborhood of Quebec, on the St. Louis road, about four miles from the 
 city, on the land of Mr. Michel Hamel, is a small deposit of earthy man- 
 ganese, extending over two or three hundred yards, and having in the 
 middle a thickness of twelve inches, but being thinner towards the edges. 
 It has the form of black porous masses imbedded in sand. 
 
CHAP. XXI.] TITANIUM. 753 
 
 TITANIUM. 
 
 Titanium has hitherto received but few applications in the arts ; and 
 until within the last few years, during which large quantities of titanic iron 
 ore have been found in the Laurentian rocks of Canada and of Norway, it 
 was comparatively a rare substance. Within two years however, attention 
 has been turned to the probable importance of small portions of titanium 
 in improving the qualities of iron and steel ; and Mr. Mushet has obtained 
 several patents for certain modes of using the native ores of titanium and 
 iron, and for obtaining alloys of the two metals. Experiments with the 
 titanic iron ore from Norway, are said to have been undertaken on a 
 considerable scale, for the purpose of determining the value of these Titanium, 
 new combinations ; but as yet, no practical results appear to have grown 
 out of this application of titanium. 
 
 A compound was, in 1846, described by Eisner, under the name of fer- 
 rocyanid of titanium, as a green paint ; and it has recently been again 
 brought into notice as a safe substitute for the poisonous arsenical green 
 color now so much used. In Eisner's process, which is said to be patented 
 in England, titanic acid, prepared by decomposing titanic iron ore by fusion 
 with bisulphate of potash, and by subsequent purification, and separation Itg applica . 
 from iron, is precipitated from its hydrochloric solution by ferrocyanid of 
 potassium at a boiling heat. By this means, a beautiful dark green pig- 
 ment is obtained ; which is however inferior in brilliancy to the arsenical 
 copper green. 
 
 In March, 1861, specifications for a patent were deposited in London, 
 by Mr. F. Versmann, for the employment of the compounds of titanium as 
 pigments, or coloring materials. The details of his processes are not known 
 to us. Several finely colored bodies, besides the green ferrocyanid just 
 noticed, have however been obtained from titanium. Thus the action of 
 gaseous ammonia upon titanic acid, heated in a porcelain tube, gives rise 
 to a stable nitrid of titanium of a violet color ; and when fused with 
 verifiable substances, in presence of metallic tin, titanic acid gives rise, 
 according to Karsten, to a beautiful deep blue enamel. This resembles 
 the smalt which is prepared with the oxyd of cobalt, and it may perhaps 
 be made to replace it. The sulphuret of titanium, prepared by the 
 action of sulphuretted hydrogen upon the bichlorid, is a beautiful bronze 
 or gold-yellow substance, which crystallizes in scales, has a metallic 
 lustre, and resembles the sulphuret of tin, known as mosaic gold. From 
 the cheapness and facility with which titanium and its compounds may 
 now be obtained, it may be presumed that before long this substance will 
 find numerous applications in the arts ; in which case the rocks of the 
 Laurentian series in Canada will probably be able to furnish it in inex- 
 haustible quantities. 
 
 XX 
 
754 GEOLOGY OP CANADA. [CHAP. XXI. 
 
 vaudreuii. The various localities of titanium in the province have been noticed on 
 page 501. The presence of small portions of this metal in many of the 
 specular schists of the Eastern Townships, is there noticed ; and also the 
 existence in Vaudreuii of a bed of iron ore, forty-five feet in width, which is 
 a mixture of about two parts of magnetic iron and one part of titanic iron, 
 or ilmenite, containing forty-eight per cent, of titanic acid. Ilmenite, in 
 a very pure form, is still more abundant in the Laurentian series, where it 
 is sometimes mistaken for an ordinary ore of iron. It closely resembles 
 magnetic iron in its external characters, and in giving a black streak and 
 powder. It is however distinguishable by the fact that it is not attracted 
 by the magnet. The most important mass of it known is that which occurs 
 
 Bay st. Paul, in the parish of St. Urbain, at Bay St. Paul. Here is a great bed, which 
 has a thickness of ninety feet, and is exposed for a length of three hun- 
 dred feet. It is however said to have been traced, with perhaps some 
 interruptions, for about a mile. Besides several smaller masses of the ore 
 in the neighborhood, which, like this, are imbedded in an anorthic feldspar 
 rock, a still larger deposit is said to exist in the vicinity, but is perhaps 
 only a continuation of the previous one. The ore, which is generally very 
 free from any earthy admixture, contains 48-6 per cent, of titanic acid. 
 This is also sometimes found in orange-red crystalline grains disseminated 
 through the ore, thus increasing its richness in titanium. 
 
 MOLYBDENUM. 
 
 Molybdenum. This rare metal exists in nature for the most part as a sulphuret, known 
 as molybdenite, or in the form of molybdate of lead. The former ore is 
 the more common, but is very seldom met with in any considerable quantity. 
 Notwithstanding its scarcity, it has however found several applications. 
 The combination of molybdic acid with ammonia is used as a reagent for 
 the detection and determination of phosphoric acid, in chemical analysis. 
 A fine blue pigment has also been prepared from molybdenum ; and a few 
 years since a German chemist proposed the blue of molybdenum as a 
 substitute for indigo in dyeing silk, cotton, and linen. Experiments to 
 
 its uses test the applicability of this substance were made by Kurrer, and are 
 reported in Dingler's Polytechnical Journal for 1853 ; from which it appears 
 that by the use of molybdenum and a salt of tin, blue dyes of every shade, 
 and of remarkable durability, when exposed to sun and air, were readily 
 fixed upon silk. Durable blues, though inferior to those given to silk, 
 are imparted to cotton by the same dye. The molybdates may also be 
 employed in printing, to give what are called topical colors to both silks 
 and cottons. The molybdic acid for this purpose is said to have been 
 manufactured at Prague, from a massive molybdate of lead, which is found 
 in some quantity in Bavaria. It does not appear that these processes 
 
CHAP. XXI.] MOLYBDENUM. 755 
 
 have ever become adopted to any great extent, one cause of which is 
 undoubtedly the rarity and costliness of molybdenum. At the Industrial 
 Exhibition of 1855, Batka, a manufacturing chemist from Prague, pre- 
 sented specimens of an impure molybdate of soda, prepared for dyeing 
 silks, and containing less than one half its weight of molybdic acid. Its 
 price was $1*20 the pound, while that of the native sulphuret of molybde- 
 num, exhibited by him, which may be made to yield about nine tenths its 
 weight of molybdic acid, was $3-45 the pound. The small supply of the 
 material, conjoined with the demand for it for the uses of the laboratory, 
 has probably prevented its more general employment. 
 
 On page 504, several localities of molybdenite have been mentioned ; Manicougan 
 but the only one of them, so far as known, which affords an^- available quan- Bay - 
 tity of the mineral, is that described as occurring in Quetachoo-Manicou- 
 gan Bay, on the north shore of the Gulf of St. Lawrence ; where it occurs 
 disseminated in a bed of quartz six inches thick, in the* form of nodules from 
 one to three inches in diameter ; and in flakes, which are sometimes twelve 
 inches broad, by one fourth of an inch in -thickness. The bed, which is 
 interstratified in a white coarse-grained gneiss, holding garnets and black 
 mica, was traced about fifty yards, with a dip N. 15 E. < 58, and would 
 probably furnish a considerable quantity of molybdenite. This mineral, 
 which has a specific gravity of about 4-5, has a leaden-grey color, and a 
 metallic lustre. It is soft, and unctuous to the touch, and is often mistaken 
 for plumbago ; from which it is distinguished by its much greater weight, 
 by a peculiar greenish hue in the metallic streak which it leaves on white 
 paper, and by the fact that when heated to redness in the open air, it 
 gives off the odor of burning sulphur, and is slowly converted into a yellowish- 
 white substance, which is molybdic acid. 
 
 Since writing the previous chapters, sulphuret of molybdenum has been Harvey HIM. 
 found at Harvey Hill, in Leeds, by Mr. Herbert Williams, the director of 
 the works of the English and Canadian Mining Company at that place. 
 The mineral occurs in some of the short courses or veins of quartz and 
 bitter spar, which intersect the copper-bearing slates of this locality. It 
 forms small masses, generally rounded in their outline, and sometimes an 
 inch or more in diameter. Judging from the specimens sent, the mineral 
 would seem to be abundant. The molybdenite of this locality, instead of 
 being foliated, as is generally the case, is finely granular, with an uneven 
 fracture ; it is very soft, and assumes a polish when rubbed with the nail. 
 It is not improbable that some among the numerous localities in which 
 molybdenite has been met with on Lake Superior, may be found to yield 
 considerable quantities of this material. 
 
756 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 MAGNESIA. 
 
 salts 
 
 Magnesia and its salts are extensively used in pharmacy, and the 
 former has been proposed as an ingredient in certain cements. The con- 
 sumption of magnesia is however limited, and minerals available for its 
 manufacture are found in abundance in most countries. Among these are 
 serpentine, a hydrous silicate, containing about forty per cent, of magnesia, 
 with a portion of iron. In France, this mineral is used for the manu- 
 facture of sulphate of magnesia. It is first calcined at a strong red heat, 
 for forty-eight hours hi a reverberatory furnace. This expels the water, 
 and renders the iron nearly insoluble. The mineral is then ground to 
 powder, and mingled with a proper quantity of sulphuric acid, which 
 rapidly converts the magnesia into a sulphate, forming a crystalline mass, 
 from which it is dissolved by water ; leaving the silica, and most of the iron 
 behind. A little milk of lime is now added to separate any dissolved 
 impurities, and the clear solution being evaporated, deposits pure sulphate 
 MagneMan of magnesia, or Epsom salt. A small establishment at Remiremont in the 
 Vosges, has long been in operation, and a few years since manufactured 
 annually from twenty to twenty-five tons of the salt from the serpentine of 
 the vicinity. One hundred parts of this, containing forty parts of mag- 
 nesia, will require about one hundred parts of sulphuric acid, and yield 
 about two hundred and fifty pounds of Epsom salt. As a great portion of 
 the magnesia is consumed in the form of calcined or carbonated magnesia, 
 it is more economical to make use of a process which dispenses with the 
 use of sulphuric acid, which is necessary to decompose the serpentine. 
 Magnesian limestone, or dolomite, is therefore resorted to. This contains, 
 when pure, a little over twenty per cent, of magnesia, in the form of a 
 carbonate, combined with an equivalent of carbonate of lime. When this 
 magnesian limestone is calcined, there is obtained a mixture of caustic lime 
 and magnesia, which is suspended in water, and treated with a current of 
 carbonic acid gas. By this means a very soluble bicarbonate of magnesia 
 is obtained, which may be separated from the less soluble carbonate of lime. 
 By referring to preceding chapters, it will be seen, that, besides the exten- 
 sive formations of dolomite, which abound in various parts of the country, 
 serpentine is found in great abundance, forming a rock in various localities, 
 both in the Laurentian and the altered palaeozoic strata. The native car- 
 bonate however is much better fitted for the preparation of magnesian 
 salts than serpentine or dolomite ; since, when calcined, there is obtained, 
 at once, caustic magnesia, without admixture of lime. The occurrence of 
 considerable beds of this rock in Bolton and Sutton has been noticed on 
 pages 457 and 615. When this impure carbonate of magnesia is calcined, 
 there is obtained a mixture of caustic magnesia, with oxyd of iron, and the 
 silicious or feldspathic impurities which the rock contains ; and it suffices 
 
 Magnesite. 
 
 Bolton. 
 
CHAP. XXI.] PHOSPHATE OF LIME. 757 
 
 to treat this mixture with a solution of carbonic or sulphuric acid to obtain 
 bicarbonate or sulphate of magnesia. In the latter case, a small amount 
 of oxyd of nickel, which the mineral contains, is taken into solution, but 
 this may be precipitated by a little sulphuret of barium. 
 
 A French engineer, Vicat, has within the last few years proposed the 
 use of magnesia, in place of lime, for hydraulic cements which are to be 
 used hi constructions exposed to the action of sea-water. For this pur- Magnes 
 pose, according to him, pozzuolana, or calcined clay, is to be mixed with mortar - 
 fifteen or twenty per cent, of caustic magnesia, exempt from lime, when a 
 cement will be obtained, which hardens after three or four days, under 
 either fresh or salt water, and soon acquires a great degree of solidity. 
 The cost of obtaining magnesia from its sulphate, prepared from serpentine, 
 or from magnesian limestone, is such as to constitute an objection to its use. 
 By calcining the magnesite of Canada, however, there is obtained a mixture 
 of caustic magnesia, with oxyd of iron and silicious matters. As the latter 
 substances would not probably be in any way prejudicial to the cement, the 
 mixture thus obtained might be used instead of pure magnesia. The mag- 
 nesite of Bolton, which contains about sixty per cent, of carbonate, would, 
 by calcination, afford a mixture containing forty-three per cent, of caustic 
 magnesia. This carbonate of magnesia, of which the Eastern Townships 
 possess large quantities, is a rare rock in most other regions, so that it is 
 not impossible that the magnesite of Lower Canada may one day become 
 an article of export. 
 
 III. MINERALS USED IN AGRICULTURE. 
 
 Under this head are included those substances which may be used as 
 fertilizers for the soil. Of these mineral manures, the only ones found in 
 Canada are phosphate of lime, gypsum, and marl. To these may however 
 be added lime, which is employed as a dressing for certain soils. 
 
 PHOSPHATE OB 1 LIKE. 
 
 Phosphate of lime is used in the arts for the manufacture of phosphoric 
 acid, and of phosphorus, and enters largely into the composition of certain 
 porcelains. It is besides very extensively used as an application to the 
 soil. Phosphates are among the minerals most essential to vegetation, and phosphate oi 
 are removed from the earth in large quantities by growing crops. The Ume - 
 importance of a supply of phosphates to the soil is made very evident by 
 the fact that the mineral part of the bones of animals is, for the greater 
 part, phosphate of lime, and up to a recent period furnished a sufficient 
 supply of this material for the demands of commerce. Carefully dried 
 bones, when calcined to whiteness, lose about one third of their weight, 
 
758 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 x>ones. which consists of organic matter, and leave a white earthy residue. This 
 contains, on an average, about eighty-six per cent, of phosphate of lime, 
 the remainder being carbonate of lime, with fluorid of calcium and a little 
 magnesia. Burned bones enter to the extent of thirty or forty per 
 cent, into the body of what is called English porcelain, which contains 
 besides, clay, ground feldspar, and flints. The phosphoric acid of the 
 bone-ash is the verifiable element of this mixture, and at a high tempera- 
 ture unites the other ingredients into a translucent enamel. The Parian 
 ware is said to be a variety of this same compound, which differs from the 
 true porcelain, into whose composition phosphate of lime does not enter. 
 The bones for this manufacture are in part obtained in Great Britain ; and 
 in part from South America, where those of the wild cattle are burned, 
 and in that state exported to England. 
 
 By far the greatest consumption of phosphate of lime is, however, for 
 agricultural purposes, for which the amount furnished by bones is alto- 
 gether inadequate. Recourse is accordingly had to other sources, among 
 
 Guano. which are the so-called Columbian guano, and other similar deposits, which 
 differ from Peruvian guano in the absence of ammoniacal or nitrogenized 
 compounds, and are little more than phosphate of lime, sometimes with a 
 portion of phosphate of alumina or of iron. In many parts, both of Eng- 
 
 coproiites. land and France, there are also found large quantities of coprolites, 
 which are the exuviae of animals of former times, and consist for the most 
 part of phosphate of lime. A stratum of clay at the base of the chalk 
 formation in Cambridgeshire furnishes great quantities of these coprolites, 
 which are extracted by washing away the earth by water, and are said 
 to contain about sixty per cent, of phosphate of lime. Nodular masses, 
 which are apparently similar to these coprolites, occur in several parts 
 of the Silurian rocks of Eastern Canada, and have been described on 
 page 461. They do not however contain more than forty per cent, of 
 phosphate of lime ; and, being disseminated in hard limestone or sand- 
 stone, instead of clay, they could not probably be extracted with advantage, 
 and are of much less importance than the crystalline phosphate of lime, 
 or apatite of the Laurentian rocks, which will presently be described. 
 
 The phosphate of lime, whether in the form of bones, coprolites, or 
 apatite, is seldom applied to the soil in its insoluble state, as it is then 
 comparatively unavailable for the nutrition of plants. To render it proper 
 for agricultural purposes, it is converted into a soluble salt, which is known 
 as superphosphate of lime. To render this process intelligible, it 
 should be remarked that in the insoluble mineral or bone phosphate, 
 one equivalent or seventy-one parts of phosphoric acid is united with 
 three equivalents, of twenty-eight parts each, of lime, making the equiva- 
 lent weight of the ordinary phosphate of lime, one hundred and fifty-five. 
 In order to reduce this to the soluble superphosphate, which contains one 
 
 Superphos- 
 phate. 
 
CHAP. XXL] PHOSPHATE OF LIME. 759 
 
 equivalent of phosphoric acid and one of lime, it is necessary to remove 
 two thirds of the lime, or two equivalents. This is effected by adding 
 two equivalents, or ninety-eight parts of sulphuric acid (oil of vitriol), 
 which forms with this lime one hundred and thirty-six parts of sulphate. 
 lOO'O parts of ordinary phosphate of lime, therefore, require 63*2 parts of 
 sulphuric acid to convert them into the soluble superphosphate, with 
 one equivalent of base. In this process, however, regard must be had to 
 the foreign matters which accompany the phosphate of lime, and which 
 may also require sulphuric acid for their decomposition. Of these, the 
 principal are fluorid of calcium and carbonate of lime. The former is 
 always present in small quantities in bones, and in still larger amounts in 
 many of the mineral phosphates, and requires, for the decomposition of one 
 hundred parts, one hundred and twenty-five of sulphuric acid. The principal 
 impurity in burned bones is carbonate of lime, which is also mechani- 
 cally intermixed with many of the mineral phosphates, and requires, for 
 the decomposition of one hundred parts, ninety-eight parts of sulphuric 
 acid. In calculating the value of any material as a source of superphos- 
 phate of lime, it is thus necessary to take into account the quantities of 
 fluorid and carbonate present, which take up a portion of sulphuric acid, 
 without giving any valuable product in return. As the greater part of the 
 expense in this process is the cost of the sulphuric acid, the manufacture 
 of the superphosphate of lime is chiefly confined to those districts where 
 sulphuric acid is prepared. In South Lancashire alone, the weekly pro- 
 duction of the superphosphate, in 1861, was stated to be from 500 to 
 600 tons ; besides which very large amounts are manufactured in other 
 parts of Great Britain. 
 
 Of late years, the increasing demand for phosphates as fertilizers has Apatite, 
 drawn attention to the use of the crystalline mineral phosphate of lime, or 
 apatite, of which large quantities have been imported from Norway into 
 England ; and attention has recently been turned to the abundant supplies 
 of this substance existing in Canada. According to a letter received in 
 September, 1862, from one of the largest manufacturers of superphos- 
 phate in England, he, a few years since, imported several thousand tons of 
 apatite from Sweden, and only abandoned its use because the English 
 phosphates of lime could be furnished at lower rates than the Swedish. He 
 writes that the following prices may be expected for phosphate of lime in 
 England : for a mineral containing ninety per cent, of phosphate of lime, 
 about j6 10s. sterling per ton; for one containing eighty per cent., 
 5 10s. ; and for one of seventy per cent., X4 10s. A mineral with a 
 lower per-centage than this would not, it is said, be merchantable. 
 
 The question is sometimes asked, whether the native phosphates of lime 
 may not be directly applied to the soil as a manure, and thus dispense with 
 the costly process of converting them into superphosphate. Ground bones, 
 
760 GEOLOGY OF CANADA. [CHAP. XXL 
 
 Phosphatic which are used with great advantage as a manure, owe a portion of their 
 efficacy to the organic matter which they contain ; and which, by its slow 
 decay in the soil, gives rise to ammonia, an important fertilizer. By this 
 process, the phosphate of lime of the bones is at the same time presented 
 to the roots of the plants in a divided state, and doubtless exerts a bene- 
 ficial action ; which, from the slowness with which the substance is dis- 
 solved, extends over several years, and is more marked after a year or 
 two than at first. The more dense phosphate of the coprolites, and of the 
 crystalline apatite, is however much less soluble than the phosphate of 
 bones, and slower in its action when applied to the soil. It therefore be- 
 comes an object to the agriculturist to apply phosphate in small quantities, 
 and in such a form as will be immediately available to the growing crop. 
 For this purpose, he has recourse to the superphosphate of lime, or to 
 some other soluble phosphate. Peruvian guano owes a great part of its 
 value to the fact that it contains three or four per cent, of phosphoric acid 
 in the form of phosphate of ammonia. When this substance, or the super- 
 Soiubiiity of phosphate of lime, is applied to the soil, it is at first taken into solution by 
 phosphates, the water there present, and is then decomposed by the compounds of lime 
 and other bases present in the soil ; so that it is again converted into an 
 insoluble phosphate, which is produced in a state of very minute division, 
 thus exposing a great amount of surface, and is distributed throughout 
 the soil. To illustrate the extent of subdivision which is attained in this 
 manner, Prof. S. W. Johnson tells us, that, while the particles of ground 
 bones will average perhaps one hundredth of an inch in diameter, those of 
 the phosphate of lime, precipitated from the dissolved superphosphate, are 
 not more than one twenty-thousandth of an inch in diameter ; so that one 
 single particle of bone dust, one hundredth of an inch in diameter, would 
 be equal to eight million particles of the precipitated phosphate. This 
 enormous subdivision, which is thus obtained by the use of a soluble 
 superphosphate, renders intelligible the great efficiency of small portions 
 of this substance, when applied as a fertilizer. According to the 
 analyses by Prof. Way, of several of the best specimens of English 
 superphosphate of lime, it appears that they contain on an average about 
 thirteen per cent, of soluble phosphoric acid, and about three per cent, more 
 in the form of insoluble and undecomposed phosphate of lime. The remain- 
 der consists of the lime of the superphosphate, together with sulphate of 
 lime and water. Besides these, there is sometimes a portion of animal 
 matter derived from bones, when these are employed, or subsequently 
 added for the purpose of converting the superphosphate into various arti- 
 ficial manures. 
 
 Apatite The abundant deposits of apatite in the Laurentian rocks of Canada, 
 
 deposits. h ave already been noticed on pages 461 and 592. The mineral has been 
 
 observed in the Laurentian limestones on the Gatineau, and on the seventh 
 
CHAP. XXL] PHOSPHATE OF LIME. 761 
 
 lot of the first range of Ross, where it is abundant in crystals disseminated BOSS. 
 with purple fluor spar in limestone ; but the most remarkable deposits of it 
 occur in the townships of Burgess and Elmsley. The mineral has been 
 traced for about a mile on the eighth range of North Elmsley, across the Eimsiey. 
 lots twenty-four, twenty-five, and twenty-six, in a direction nearly south- 
 west ; and apparently forms an irregular bed in the Laurentian limestone. 
 On the second of these lots, where it has been somewhat quarried, the 
 breadth of the bed seems to be about ten feet, of which three feet are nearly 
 pure crystalline apatite, sea-green in color, and with a small admixture of 
 black mica. Masses of this gave on an average eighty-eight per cent, of 
 phosphate of lime. 
 
 The deposit of apatite just noticed appears to extend southwestwardly, Burgees. 
 into North Burgess, where it is found in a great many localities. The 
 fourth lot of the eighth range, and the second and seventh lots of the 
 seventh, are localities of the mineral. The first of these has furnished large 
 crystals, thickly disseminated with mica, in a flesh-colored limestone. It 
 has also been found south of Rideau Lake, on the first lot of the fourth 
 range of South Burgess ; but it appears to occur in the greatest abundance 
 in the fifth range of North Burgess, where it has been observed in lots 
 four, seven, eight, nine, and ten. Specimens from the latter two lots 
 are massive, crystalline, and very pure. That from the fourth lot is 
 described as presenting eight or ten parallel beds, interstratified with 
 gneiss, and running northeast and southwest. These beds are said 
 to be from eight to twenty-four inches in thickness, and from ten to 
 twenty feet apart. A large block of this mineral was found to resem- 
 ble closely in aspect that from the two lots mentioned above. It is 
 crystalline, granular, with an uneven fracture, a vitreous lustre, and is 
 translucent, with a greyish hue, which passes into greenish or reddish. It 
 resembles, at first sight, some varieties of quartz rock ; from which how- 
 ever it is readily distinguished by its inferior hardness, its greater weight, 
 and by the action of nitric and muriatic acids, which readily dissolve it 
 when in powder, without effervescence. What was regarded as an average 
 specimen from one of the beds, on the fourth lot, gave by analysis : phos- 
 phate of lime 91-20, fluorid of calcium 7'60, chlorid of calcium 0-78, 
 insoluble 0-90 ; = 100'48. When treated with sulphuric acid, it is readily 
 decomposed, and evolves abundance of hydrofluoric acid. This mineral 
 phosphate contains only traces of oxyd of iron ; and from its purity, it might 
 perhaps be used instead of bone-ash in the manufacture of English por- 
 celain. Mr. Benj. Hutchins, of Montreal, has recently acquired the most 
 important of these deposits of apatite, in Burgess and Elmsley, and is 
 making preparations to work them, with a view of offering the phosphate 
 of lime of Canada to the English market. 
 
762 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 The existence of gypsum in various geological positions in Canada has 
 already been noticed on page 459. It is only in the Onondaga formation 
 
 Gypsum that workable deposits of it are known to occur : and the facts of scientific 
 importance in the history of the gypsum of this formation will be found in 
 the thirteenth chapter, where it has been shown that it is interstratified 
 with peculiar dolomites and dolomitic marls ; some of which are farther 
 described on page 625. The outcrop of this gypsiferous formation extends 
 from the Niagara River to the Saugeen on Lake Huron, a distance of 
 about one hundred and fifty miles ; but the gypsum mines at present known 
 
 Grand are all found within about thirty-five miles, on the Grand River, extending 
 
 Biver. f rom Cayuga to Paris. It is probable however that as the country to the 
 north west of Paris becomes more settled, farther discoveries of gypsum 
 beds will be made in that direction. To the southeast of Cayuga, the 
 overlying drift conceals any beds of gypsum which may be present. All 
 of these deposits seem to be confined to one stratigraphical position, which 
 is probably about the middle of the formation. The gypsum occurs in 
 beds, which thin out in such a manner that they present the form of len- 
 ticular masses. These vary in horizontal diameter, from a few yards to a 
 quarter of a mile, and are from three to seven feet in thickness. The 
 strata above them are arched and broken, while those beneath present an 
 undisturbed level floor, the two coming into contact at the edge of the 
 masses. This peculiar structure gives rise to mounds on the surface, which 
 are regarded by the inhabitants of the region as indications of the pre- 
 sence of beds of gypsum below. The probable origin of this structure has 
 been discussed on page 352. 
 
 Cayuga. A large deposit of gypsum, which h&s been extensively wrought, occurs 
 about three miles below the village of Cayuga, on the left bank of the 
 Grand River, and is supposed to extend over at least sixty acres. The 
 bed, which is five feet in thickness, and very pure, is in some places over- 
 laid by thin beds of dolomite ; but in most parts it is covered only by clay 
 and gravel. About five miles above this, which is known as Mr. Brown's 
 plaster-bed, gypsum is met with in Indiana, on the left bank of the river ; 
 and about four miles farther up, near York, it occurs on both sides. On 
 the right, near Mount Healy, is a very large bed of gypsum, three or four 
 feet in thickness, which has been extensively wrought. About a mile and 
 a half above York, on the left bank of the Grand River, is a mass of gyp- 
 sum seven feet in thickness, but divided by layers of dolomite. Occasional 
 masses of gypsum, imbedded in green shales, are met with for two miles 
 farther up the river to Seneca. Twenty miles above, in the township of 
 Brantford, gypsum is again found, extending over several lots, and on both 
 sides of the river. A bed of three feet in thickness is here wrought ; and 
 
CHAP. XXI.] FRESH-WATER MARL. 763 
 
 above this place, gypsum is quarried at several places along the river as far Brentford, 
 as Paris. Near this town, the mass of gypsum is divided into two portions, 
 of four or five feet in thickness, by a bed of four feet of shale. 
 
 The amount of gypsum annually raised from these various quarries on 
 the Grand River, is about 14,000 tons ; which is, for the most part, em- 
 ployed for agricultural purposes, and is consumed in Western Canada. 
 The price of "the crude gypsum at the mine is about 12-00 the ton ; but 
 when ground for use, at the mills in the vicinity, it is sold at from 83 '50 
 to 84.00. Much of the gypsum is white and pure, and is well fitted for 
 the purposes of cement and stucco. The quality which is used for this 
 purpose sells, when ground, at from 85-50 to 8T'00 the ton; and when 
 calcined, at about 816-00 the ton. 
 
 Large quantities of gypsum are brought to the Lower Canada market 
 from the Magdalen Islands. Nothing certain is known of the geological 
 relations of this deposit ; but it is perhaps, like the extensive beds of 
 gypsum which are wrought in Nova Scotia, of Carboniferous age. 
 
 FRESH-WATER MARL. 
 
 Under this head may be noticed certain deposits of carbonate of lime, Origin of 
 which are found in marshes and shallow lakes ; and which generally con- m 
 tain, in greater or less abundance, the shells of several species of fresh- 
 water mollusca. Although belonging to the present geological period, this 
 marl is not always of very recent formation ; inasmuch as the beds of it are 
 sometimes overlaid by peat, or by a soil supporting a growth of large trees. 
 At other times however the marl covers the bottom of shallow lakes or 
 ponds, and is evidently still in the process of deposition. It appears to be 
 formed by the waters of springs highly charged with lime, which is at first 
 held in solution as bicarbonate, but is deposited when these waters come 
 to the air. It is thua similar in its origin to the deposits of calcareous tufa, 
 which occur in many places where such calcareous springs flow over earth, 
 rocks, and vegetation, instead of falling into lakes or marshes. The pre- 
 sence of carbonate of lime is a necessary condition of the development of 
 shells, and various species of mollusca abound in such waters. These 
 by their remains, which often form a considerable portion of the deposits, 
 give to them the name of shell-marl, which is frequently applied. This 
 substance is white, and earthy hi its aspect, and, unless mingled with 
 clay, is a nearly pure carbonate of lime ; which, from its finely divided 
 state, is well adapted to serve as a dressing for such soils as are deficient 
 in calcareous matter. When calcined, marl yields a nearly pure and very 
 white lime, well adapted for mortar and for other uses. In many parts of 
 Vermont large quantities of lime are thus manufactured. The marl is 
 moulded into shapes like bricks, which are dried and burned in a kiln. 
 
764 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 The analyses of various marls from Vermont show them to contain from 
 one to four hundredths of carbonate of magnesia, with small but variable 
 amounts of clay, water, and organic matters. When pure, marl may be 
 used as a substitute for prepared chalk or whiting, in cleaning metals, and 
 for similar purposes. In many parts of the country, it is commonly 
 employed by the people for white-washing their buildings. It has also 
 been used for the production of carbonic acid gas for the manufacture of 
 soda-water, and other aerated waters, in place of the pulverized chalk or 
 marble-dust which is generally employed. The fossiliferous limestone of 
 Montreal has sometimes been used for this purpose ; but the small amount 
 of bituminous matter which it contains, gives a peculiar odor to the carbonic 
 acid gas obtained from it, which is communicated to the aerated waters. 
 
 Marl is met with in a great many localities throughout Canada, and 
 it will be sufficient to mention some of the most important among them. 
 Deposits of this material are abundant in the counties of Bruce and Grey. 
 
 carrick. One of these, on the twenty-fifth lot of the fifteenth range of Carrick, 
 covers about six acres, and was found to have a depth of twenty-seven 
 inches. It is very pure and white, and is covered with a thin layer of 
 black mould, forming the soil of a meadow. Other deposits, estimated at 
 forty acres in all, occur in the immediate neighborhood. On the sixth lot 
 of the first range of Brant, north of the Durham road, marl occurs in a 
 peaty meadow, beneath a foot of soil. It is two feet in thickness, and 
 extends over seven acres. Another locality in the same township is on the 
 seventieth lot of the first range, south of the same road ; where it is seen 
 in the banks of a little stream, near its junction with the Saugeen, and has 
 in some places a thickness of three feet. On the twenty-sixth lot of the 
 first range of Bentinck, a deposit of marl has been traced over eight or ten 
 acres of low ground, which is covered with heavy timber. The marl is 
 very solid and pure, and where examined was found to be four feet in 
 thickness. 
 
 In the rear of Kingston, an extensive deposit of marl occurs in the 
 fifeenth and sixteenth lots of the second range of Sheffield ; and another on 
 
 Brant. the twelfth lots of the third and fourth ranges of the same township. The 
 former of these has been traced over two hundred acres or more, and has, 
 in the greater part at least, a thickness of ten feet. It is covered by a 
 thin soil, supporting a growth of meadow grass. In the second locality, 
 the marl, whose thickness has not been ascertained, extends over three or 
 four hundred acres of marshy land, which is covered by about four feet of 
 peat. It also forms the bottom of White Lake, in this township. A great 
 portion of the bottom of Loughborough Lake is a thick deposit of marl ; 
 and the bottoms of all the lakes, from this to White Lake in Olden, are in 
 greater or less degree composed of the same material. A bed of marl is 
 found at Belleville, but it does not appear to be extensive. 
 
CHAP. XXL] FRESH-WATER MARL. 765 
 
 In the township of Yonge, on the thirteenth lot of the eighteenth range, Yonge. 
 a bed of marl occurs beneath a marsh, and it is said to extend over twenty 
 or twenty-five acres. Its thickness was found to be seven feet, but it is 
 reported to be fifteen feet in some parts of the deposit. Marl has also been 
 found in the bays on the south shore of a lake in Elmsley, where it has a 
 thickness of three or four feet, and extends beneath the waters of the lake. 
 
 Marl has been observed in many localities along the valley of the 
 Ottawa, and some remarkable deposits of it are found in the lakes near the 
 Bonnechere. In the upper end of Mink Lake, a bed of marl extends out Mink Lake, 
 for a quarter of a mile from the shore, where it has a thickness of nine 
 feet, and is covered by two or three feet of water, while nearer the shore 
 the depth of water is less. Several bays in this lake have in like manner 
 bottoms of marl, and a shoal of it occurs in the middle of the lake. In 
 the lower part of White Lake, in the township of MacNab, about seven MacNab. 
 hundred acres are covered with marl, which was found to have a depth of 
 from five to seven feet, and was covered by not more than two or three 
 feet of water. Both of these lakes might easily be subjected to a partial 
 drainage, by which great quantities of marl would be exposed. Around 
 the shores of Clear Lake, in Sebastopol, there are numerous shallow lakes 
 or ponds, which discharge their waters into this, and contain beds of marl, 
 evidently in the process of deposition. Their waters contain abundance 
 of living fresh-water mollusca, and plants. Marl has also been observed 
 in several small lakes on Calumet Island, and on the twenty-third lot of 
 the first range of Clarendon. 
 
 Near Ottawa, marl occurs at New Edinburgh in Gloucester. Here the Ottawa, 
 deposit is evidently of more ancient date than those just described ; for 
 it is covered with soil, and supports a growth of large forest trees. The 
 bed of marl has a thickness of about five feet, but its extent is not known. 
 Marl occurs on the eighteenth lot of the fourth range of West Hawkes- 
 bury, in a low meadow, which apparently occupies the site of an ancient 
 lake. It is known to cover three or four acres, but is supposed to be much 
 more extensive. At the place which has been excavated, the marl is three 
 and a half feet in thickness, and is covered by four feet of peat. Branches 
 and trunks of trees, in a good state of preservation, are met with in the 
 marl, but not in the overlying peat. This marl has been applied as a 
 manure to the sandy soils of the vicinity, and it is said with very good 
 results. The peat has also been used for a similar purpose. 
 
 On the third lot of the first range of Argenteuil, marl is also met with Argentina, 
 in what appears to be the basin of a former lake, but now filled with 
 peat ; beneath about nine feet of which is found a bed of marl, five or six 
 feet deep, and in one place, it is said, thirteen feet. The area of this 
 deposit of peat is about twenty-two acres. On the same lot is another peat 
 bog, which has a length of about half a mile from east to west, with a 
 
766 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 Montreal. 
 
 breadth of from one hundred to one hundred and fifty yards. Beneath 
 this, marl was met with, at a depth of twelve feet. 
 
 Marl has been observed in Eagle-Nest Lake, on the twenty-second lot of 
 the eighth range of Wentworth ; and also in a pond on the fifth lot of the 
 fourth range of Harrington. The quantity in both cases was considerable. 
 In the seigniory of Vaudreuil, at Point a Cavagnol, is a bed of marl which 
 extends over about twenty acres, with a thickness of from twelve to 
 eighteen inches. It has been largely used as a manure on the lands in 
 the vicinity, and with beneficial results. 
 
 On the island of Montreal, marl is found in several places, underlying 
 the peat along the banks of the river St. Pierre, between Montreal and 
 Lachine. A deposit of very pure white marl also occurs at Thornberry, 
 on the west side of Mount Royal. It is overlaid by peat, and does not 
 appear to be extensive. In the seigniory of St. Hyacinthe, near the foot 
 of Yamaska Mountain, and the junction of the Granby road with that to 
 St. Pie, is a bed of marl about a foot in thickness, extending over about 
 seven acres, and covered by a thin layer of peat. Marl is met with about 
 st. Armand. a mile southeast of Philipsburgh, on lots 156 and 157 of St. Armand. It 
 appears all around the margin of a small lake, and probably covers between 
 thirty and forty acres. Its thickness in some parts is seven feet. This 
 marl, which, like all the others here mentioned, contains fresh-water shells, 
 rests upon a deposit containing marine shells, probably of post-tertiary age. 
 Marl is also found on the fourth and fifth lots of the tenth and eleventh 
 ranges of Stanstead. It appears at the margin of a pond over an area of 
 about twenty acres, and is said to have a depth of from thirty to forty feet. 
 
 In the Bonaventure district, marl is met with a mile or two from 
 the village of New Carlisle. Here, in a valley of about three miles in 
 length, by half a mile in breadth, are four or five small lakes, in the bot- 
 toms and around the margins of which is found a layer of pure white marl, 
 from one to six feet in thickness. Marl has been observed in the upper 
 end of Lower Lake Metis ; and about five miles below the Matanne River, 
 near the bank of the St. Lawrence, a deposit of the same substance, with 
 a thickness of fifteen niches, has been found to underlie in various places 
 a marsh of between sixty and seventy acres. 
 
 In Anticosti, marl exists in most of the small lakes or ponds which have 
 been examined near the coast of the island. One of these at the west end 
 of the island, named Marl Lake, has an area of about ninety acres, and is 
 covered at the bottom with marl, apparently of considerable thickness. 
 The stream which discharges this lake into Indian Cove, carries down a 
 large quantity of the marl to the sea, where it is spread out for a consider- 
 able distance over the rocks of the coast. About three miles from South- 
 west Point, marl was found on the bank of a brook, and was traceable 
 thence for a quarter of a mile, in a bed of a foot in thickness, covered by 
 
 Anticosti. 
 
CHAP. XXL] IRON OCHRES. 767 
 
 peat. About half a mile farther inland, it covers the bottom of a lake of 
 two hundred acres ; and on the east side of South Point it was observed near 
 the shore, resting on rock, and covered by from four to ten feet of peat. 
 
 IV. MINERALS USED AS PIGMENTS. 
 
 Under this head will be considered certain matters which are employed 
 as paints. The marls which have just been described are occasionally used 
 in- this way, for white-washing walls or wood-work, instead of whiting, and 
 may be mingled with cheap colors. Besides these may be noticed iron 
 ochres, and sulphate of barytes, both of which are extensively used as pig- 
 ments. Of late years, various substances have been introduced into the 
 arts under the name of stone paints. These often consist of fine shales, or stone paints, 
 other soft rocks ground to a powder, and, when mingled with oils, consti- 
 tute a cheap and durable covering for wood-work, which is generally how- 
 ever of some dull and earthy color. In Newburyport, Massachusetts, ser- Serpentine, 
 pentine, which gives a nearly white powder, is ground, and subsequently 
 impregnated by a peculiar process with various mineral and vegetable 
 colors. By this means, cheap and durable paints of various hues are manu- 
 factured. Soapstone, or steatite, is also made use of in a similar manner. 
 Two coats of these materials are said to form a good base for a third of 
 common paint. Both steatite and serpentine fit for the purpose are found in steatite, 
 great abundance in many parts of the province. On the thirteenth lot of 
 the ninth range of Stanstead, is a soft and apparently decomposing talcose 
 slate, which exhibits parallel vertical layers of greyish-white and ochre- 
 yellow colors ; the latter being due to hydrated peroxyd of iron. This 
 talcose rock has been employed, mixed with oil, for painting houses. A 
 similar material is met with on the seventeenth lot of the thirteenth range 
 of Leeds. Its color is a light ash-grey, and it has been used as a water- 
 color, but it might probably, like the last, be mixed with oil. 
 
 IBON OCHRES. 
 
 These ochres are similar in composition to the ore of iron which has been 
 already described under the name of limonite and bog ore. They differ 
 from it however, in being soft and pulverulent, instead of forming solid 
 masses ; and consist of peroxyd of iron, combined with water, and often 
 with a large amount of organic matter, as will be seen by referring to the 
 descriptions and analyses given on page 511. The color of these ochres Ochrea. 
 is generally some shade of yellowish or reddish brown ; but purplish and 
 blackish brown hues are met with. By calcination, the water is removed, 
 and the color of the ochre is changed to a dark red. These substances are 
 extensively used, both in the raw and calcined state, as cheap paints, with 
 oil, and with water. 
 
768 GEOLOGY OF CANADA. [CHA?. XXI. 
 
 The most abundant deposits of ochres known in Canada are on the north 
 side of the St. Lawrence, at the foot of the Laurentide hills, where, as haa 
 been seen, the most extensive beds of bog iron ore are also met with. A 
 ste.Anne. remarkable deposit of ochre is found in the parish of Ste. Anne, Mont- 
 morenci, on the land of Mr. E. Caron, about a mile and a half above the 
 mouth of the Ste. Anne River, and covers an area of about four acres, 
 with a depth of from four to seventeen feet. A detailed description of the 
 deposit will be found on page 511. In the superficial portions of the bed 
 are found yellowish and reddish-brown, and brownish-black ochres ; all 
 of which are very pure and free from foreign matters. When raised from 
 the deeper parts of the bed, the ochre is of a pale greenish color, but 
 becomes reddish-yellow when exposed to the action of the air. This deposit 
 occurs upon a somewhat sloping ground, and offers great facilities for exca- 
 vating and draining. No attempt has however as yet made to work 
 it. Iron ochre is said to be found in some abundance on the road to 
 St. Stanislas, at Lake Capabusca, on a tributary of the Batiscan, about 
 seven leagues from Ste. Genevive. 
 
 A great deposit of ochre occurs on the St. Malo range, in the seigniory 
 cap deia of the Cap de la Madeleine, about two miles below the parish church, and 
 Madeleine. fae same distance from the St. Lawrence. It extends over about 600 
 acres, and is interstratified with peat, which underlies it, and is in its turn 
 underlaid by shell marl. From an examination of the locality, it would 
 appear that it was originally a lake, in which marl was at first deposited, 
 and which eventually became filled up with peat. Over a part of this 
 surface, ochre was then deposited, and was followed by a second growth 
 of peat ; which has been in its turn covered by a more recent deposit of 
 ochre. This succession is shown by a series of borings and excavations 
 made along a line through the middle of the deposit, from southeast to 
 northwest. At fifty paces from the margin, there were found six inches 
 of yellow ochre, followed by the same thickness of peat, and a second bed 
 of six inches of ochre, resting on two feet of peat. Three borings in the 
 next one hundred and twenty paces, showed from one to two feet of ochre, 
 resting upon from four to eight feet of peat. A hundred paces beyond, 
 the ochre was wanting, and nine feet of peat were found to rest upon six 
 inches of marl ; while one hundred and sixty paces farther, two feet of ochr*e, 
 at the surface, were followed by two layers of peat, separated by a second 
 layer of ochre, and underlaid, as before, by marl ; the whole section hav- 
 ing a thickness of nine feet. Beyond this, the ochre is wanting, and the 
 bed of peat is in some parts twelve feet in thickness. This locality would 
 furnish very large quantities of ochre ; and in the parts where it is more 
 or less mingled with the peat, blocks of the mixture, dried and kindled, 
 burn slowly away ; the organic matter being destroyed, and leaving the 
 ochre behind, in a calcined state. In the Ste. Marguerite range, ochre is 
 
CHAP. XXI.] IRON OCHRES. 769 
 
 met with along a distance of several miles. It is however in small patches, 
 seldom more than a few yards in diameter or three or four inches in thick- 
 ness, and is more or less mixed with sand. In the vicinity of St. Maurice, 
 about a mile and a half below the iron-works, and on the opposite side of 
 the river, a small deposit of ochre has been observed, extending over about 
 two hundred yards, with a thickness of from three to six inches. 
 
 In the St. Nicholas range of the seigniory of Pointe du Lac, there is an PointeduLac. 
 important ochre bed, which covers about four hundred acres, and has a 
 thickness ranging from six inches to four feet, averaging perhaps eighteen 
 inches. The prevailing colors of the ochre are different shades of red and 
 yellow ; but it has in some parts a fine purple tint. All of these however 
 become dark red by calcination. Besides this, a blackish-brown variety is 
 found, which is rarer than the others. This assumes a lighter brown, 
 instead of a red color, when subjected to heat, and probably contains a little 
 manganese. The impurities of these ochres consist of small quantities of 
 sand, and of the roots of plants, which have grown upon the surface, and 
 penetrate the bed to considerable depths. These vegetable impurities are 
 easily got rid of by calcination ; but when it is required to preserve the 
 colors unchanged, the ochres are dried and sifted. In 1851, an attempt 
 was made to work these ochres, on a considerable scale, by persons from 
 New York, who erected furnaces for the calcination of the ochres ; and 
 are said to have prepared as much as twelve barrels daily, which were 
 sent to New York for sale, and were worth there about five dollars the 
 barrel. Eight different tints were said to have been manufactured from 
 these ochres. The blackish-brown variety, which is rarer than the others, 
 was found to command a considerable price, and was sold by the name of 
 raw sienna ; while the same ochre, calcined, was sold as burnt sienna. 
 The enterprise was however, after a while, abandoned. 
 
 Farther to the northwest, in the same range, patches of ochre are found 
 in considerable abundance for upwards of a mile ; but they are less pure 
 than the deposit just described, and have a thickness of from three to six 
 inches only. Small portions of ochre are in like manner met with on the left 
 bank of the Great Yamachiche River, near the southwest limit of the 
 Augmentation of Caxton. The ranges Ste. Emelie and Ste. Rose, in the 
 seigniory of Lanoraie and Dautraye, in like manner contain small areas of 
 ochre ; and it is probable that this substance is common in many of the 
 localities throughout that region. 
 
 On the south side of the St. Lawrence, ochre has been observed in a Durham, 
 marsh on the fourth lot of the fourth range of Durham, where it was 
 traced one hundred and fifty yards, with a breadth of ten yards, and a 
 depth of from one to four feet. A small deposit of ochre is found resting 
 upon the Potsdam sandstone on Hemmingford Mountain. Upon the 
 Ottawa, ochre occurs in considerable quantity in the Grand Marais, in 
 
 YY 
 
770 GEOLOGY OP CANADA. [CHAP. XXI. 
 
 Mansfield, opposite the northern extremity of Calumet Island. It has also 
 been obtained from Paint Lake, at the Black River Chute. In the seign- 
 
 vaudreuii. . iorj of Vaudreuil, overlying a bed of bog iron ore eight feet in thickness, 
 which has already been described, is a layer of about a foot of ochre. 
 In the immediate vicinity, and along the edge of the ore-bed, which 
 it apparently underlies, is a deposit of earthy phosphate of iron, of a bright 
 blue color. The presence of water rendered it difficult to determine the 
 quantity of this substance ; but it appeared to be considerable, although 
 somewhat mingled with foreign matters. If obtained in sufficient purity, 
 it might be used as a pigment. 
 
 In Western Canada, on the southwest side of the village of Owen 
 
 Owen sound. Sound, a bed of bright yellow ochre, containing an admixture of carbonate 
 of lime, is found at the foot of a hill in which the rocks of the Clinton 
 formation are exposed. The extent of the deposit has not been ascertained ; 
 but it has in some parts a thickness of four feet. On the second lot of the 
 eleventh range of Nottawasaga, on the south side of the river, is a small 
 bed of yellow ochre, which has in some parts a thickness of two or three 
 feet. It is produced by chalybeate springs, which issue from the rocks of 
 the Clinton formation. Small deposits of ochre, from a similar source, are 
 found in various other localities at the outcrop of this formation. A red 
 argillaceous earth, derived from the disintegration of the shales of the 
 same series of rocks, occurs in abundance at McKann's mills in Nassaga- 
 weya ; where it has been used, mingled with oil, as a paint. A similar 
 earth occurs in many other places along the outcrop of these rocks. 
 
 SULPHATE OF BARYTES. 
 
 This mineral, which has been noticed on page 458, is extensively employed 
 in the arts, as a paint, both by itself, and for mixing with other pigments 
 as an adulteration, for which purpose it is fitted by its great weight. It 
 enters into the composition of the cheaper kinds of white-lead paint ; some- 
 times, it is said, to the extent of seventy-five or eighty per cent. For this 
 purpose, the native sulphate of barytes is crushed, and if necessary boiled 
 with dilute muriatic or sulphuric acid to remove any metallic oxyds which 
 may discolor it ; after which, it is ground to a fine powder. An artificial 
 sulphate of barytes is also manufactured by precipitation, and is sold 
 under the name of permanent white, or blancfixe. This is prepared from 
 the native sulphate by igniting it with charcoal, by which a sulphuret of 
 barium is formed. This, by the addition of muriatic acid, is converted 
 into chlorid of barium, from which the sulphate is precipitated by sulphuric 
 acid. The pigment thus obtained is much finer than that prepared by 
 simply grinding the mineral. It is used as a water-color ; and also in the 
 manufacture of paper-hangings, for giving a peculiar glossy surface. In 
 
CHAP. XXL] PEAT. 771 
 
 1861, about two tons a week of the precipitated sulphate of barytes were 
 prepared by this process in South Lancashire. The consumption of the 
 ground sulphate of barytes is very considerable. Many years since, about 
 4,000 tons of the mineral were sold annually in the United States ; of which 
 1,500 tons were imported from England, and the remainder obtained from 
 various parts of the country. 
 
 Available deposits of sulphate of barytes exist in several parts of 
 Canada, and it is found in many of the lead veins in the Laurentian rocks. 
 One of these is on the second lot of the seventh range of Lansdowne ; Lansdowne. 
 where, in an excavation made in search of lead, it was found that the lode, 
 for a length of twenty-eight feet, and a breadth of twenty-seven inches, 
 was filled with pure, crystalline, and almost colorless sulphate of barytes ; of 
 which the vein, in this part, would yield about ten tons to the square fathom. 
 A vein of sulphate of barytes, about a foot in breadth, occurs in gneiss, on the 
 fourth lot of the ninth range of North Burgess. It is opaque white, lamellar, Burgess, 
 and contains no impurity, except small grains of copper pyrites. In the 
 limestone of the Niagara formation, at Port Daniel, a vein of sulphate of 
 barytes, nine inches in breadth, is met with. It contains small portions of 
 copper pyrites, and of green carbonate of copper. Numerous veins of sul- 
 phate of barytes, mixed with calc-spar, and not above three inches in 
 breadth, occur in the Gaspe sandstones on the York River. The most 
 abundant source of barytes in Canada will, however, be found the vein- 
 stones of the large lodes carrying copper ores, on the north side of Lake Lake 
 Superior, between Pigeon River and Fort William, and in Thunder Bay. Su P enor - 
 
 
 V. COMBUSTIBLE AND CARBONACEOUS MINERALS. 
 
 It has already been shown in a previous chapter, that, although met with 
 in small quantities in the Devonian rocks, coal cannot be reckoned among 
 the economic minerals of Canada, so far as yet examined. The province, 
 however, possesses great quantities of peat ; and it is here proposed to 
 consider this substance, together with bituminous shales, and bitumens. 
 
 Great deposits of peat are met with in various parts of Eastern Canada, 
 which seems to present conditions of soil and climate peculiarly favorable 
 to its growth and accumulation. The peat bogs, so far as known, are Peat bogs, 
 chiefly confined to the plains along the St. Lawrence and its tributaries, 
 and appear to have been formed in shallow lakes, which have been gradu- 
 ally filled up by a vegetable growth. The peat often rests upon a layer 
 of shell-marl, which at one time formed the bottom of the lake. The vegeta- 
 tion consists, for the most part, of mosses belonging to the genus Sphagnum. 
 
772 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 Besides these, however, the bogs often support a growth of tamarack 
 (Larix Americana) , and of various ericaceous plants, belonging chiefly 
 to the genera Cassandra, Andromeda, Kalmia, and Ledum. The leaves, 
 roots, and stems of these help, with the moss, to make up the peat. The 
 peat near the surface of the bog, consists of the moss but little altered, 
 and is very soft and porous ; but in the older and deeper portions of the 
 deposit, it is more dense and darker in color ; the vegetable tissue having 
 undergone a partial decay, by which its fibrous structure, to a greater 
 or less degree, disappears, and the peat becomes earthy in its texture. 
 
 Density of These different forms of peat present very great variations in their specific 
 gravity. That from the surface of the Bog of Allen, in Ireland, according 
 to Sir Robert Kane, has a density of 0-335, or only one third that of water ; 
 while the blackish-brown earthy peat, from a lower layer in the same bog, 
 is from 0-639 to 0*672, or double that of the surface. A peat which is 
 dug near Tavistock in Devonshire, has a density of 0.850. Similar differ- 
 ences will be found in the peat bogs of Canada. A specimen of peat from 
 Sherrington, described on page 642, is still more dense than any of these, 
 being so heavy as to sink in water ; while at the same time it only contains 
 3-5 per cent, of ash. One of the great obstacles to the use of peat is the 
 large amount of water which it holds, and the obstinacy with which it 
 retains this water. The average result of a great number of experiments 
 made in the Irish bogs, show that the general mass of the undrained peat, 
 including both the lighter and denser varieties, contains from 92 to 95 
 per cent, of water; while the edges of the bog, and parts more or less drained, 
 in the state in which peat is generally cut, contain from 88 to 91 per 
 
 Amount of cent. The turf, as used in that country, often holds from 20 to 35 per 
 
 water. cent, of water ; while that which has been stacked from six to twelve months, 
 still retains from 18 to 20 per cent., and that which has been kept in a dry 
 house for two years, from 10 to 15 per cent, of water. The above details, 
 and many of those which follow, are taken, in part, from Sir Robert Kane's 
 work on The Industrial Resources of Ireland, and a subsequent report by 
 him on the working of peat; and also in part from a recent paper by 
 Mr. C. Hodgson, read before the Institution of Civil Engineers of Ireland. 
 From this, it will be seen that in cutting out and removing the peat from 
 the bog, it becomes necessary to transport about nine tons of water for 
 each ton of real fuel. So long as a turf-cutter works along the edge of 
 
 cutting the bog, or of one of the main drains, he can spread the material as he cuts 
 it ; but when large quantities are wanted, additional laborers are required 
 to carry the peat, with its great weight of contained water, to a proper 
 place for spreading and drying. From the slowness of this process of air 
 and sun drying, moreover, a given district can only produce a small amount 
 of dried peat annually. The consequence is, that, although peat prepared 
 in the ordinary way is a cheap domestic fuel, and is sold at a moderate 
 
CHAP. XXL] PEAT. 773 
 
 price, it is found that as soon as the consumption increases in a district, 
 the price increases, and that it is impossible to augment the supply beyond 
 a certain limit. The Irish Peat Company, who a few years since constructed 
 works near Athy, for distilling peat, at the rate of fifty tons daily, had 
 counted upon obtaining this supply at from 2s. 6d. to 3s. the ton; but it was its cost, 
 found that before they had secured the quantity necessary for carrying on 
 their works successfully, the price of peat increased to 5s., and ultimately 
 to 6s. 6d., and 7s., sterling the ton. This increase, together, as we are 
 told, with the impossibility of obtaining, at any reasonable price, a much 
 larger supply, were among the causes of the failure of the enterprise. 
 
 It is obvious, then, that in order to extend the use of peat, either as a 
 combustible, or as a material for distillation, it becomes necessary to intro- 
 duce great improvements into its manufacture ; which will make it possible 
 to free it as rapidly and as completely as possible from the water which it 
 contains. It is also desirable to reduce its volume, for the convenience of compressing 
 transportation ; and to give it a solidity and tenacity approaching to coal, pea ' 
 which will allow it to be used in ordinary grates and furnaces, and to bear 
 a strong blast. For this purpose, many plans have been proposed, and 
 numerous patents obtained within the last twenty-five years. One of the 
 most satisfactory processes is said to be that now pursued at Ekman's iron 
 works in Sweden, which is similar to that patented by Linning in 1837. 
 Acccording to his specifications, the peat is first ground to a homogeneous 
 mass in a pug-mill, similar to that used by brick-makers, but with longer 
 and sharper knives, placed obliquely. The pulp thus obtained is moulded 
 into convenient shapes, and consolidated by a hydraulic or other press ; 
 after which the blocks are dried by artificial heat. The use of hydraulic 
 pressure was several years since tried on an extensive scale, by Mr. C. M. 
 Williams, at Cappogue, in Ireland. He, having broken up the peat, placed plan< 
 it in layers between cloths, and subjected it to a powerful hydraulic press. 
 By this means, he succeeded in reducing it to one half its original weight, 
 and to one third its volume. The remaining water was, however, difficult to 
 be expelled from the consolidated peat; and the more fibrous varieties 
 expanded a good deal in drying. This experiment was lately repeated, on 
 a considerable scale, by the Irish Peat Company ; and with similar results. 
 They also built large drying-houses, in which attempts were made to dry 
 ordinary peat by artificial heat ; but the quantity of fuel required to expel 
 the great amount of water from the peat, was found to be so considerable 
 that the process was not economical. 
 
 A different plan was some years since proposed for overcoming certain 
 of the difficulties of the problem ; which was, after drying peat in the 
 ordinary manner, to pulverize it by passing it through rollers, then to drive 
 off the remaining water by heat, and consolidate the dry powder by pow- 
 erful pressure. This process is followed at Rosenheim, in southern Bavaria, 
 
774 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 where the peat is made into small blocks of eight or ten ounces, and 
 weighing from seventy to eighty pounds to a cubic foot. The latter weight 
 corresponds to a specific gravity of 1*25 ; which is nearly that of bitumi- 
 nous coal. (Percy's Metallurgy, vol. i., p. 78.) Several patents, based 
 upon this plan of dry compression, have been within the last few years 
 obtained in England ; but practical difficulties were met with in the machin- 
 Hodgson's ery for compression ; besides which, as Mr. Hodgson has well remarked, 
 the great problem of obtaining a cheap and abundant supply of dried and 
 powdered peat still remained. This however, according to him, is in 
 great measure resolved by a simple expedient. By passing a very light 
 harrow over the surface of the bog, a thin layer is broken up. After a 
 few hours of exposure to the air, for draining and partial drying, it is 
 removed by scraping ; and in this way a powdered peat, far drier than the 
 general mass, may be obtained every day, when it does not rain. The 
 material thus collected costs five-pence the ton, and contains, on an average, 
 forty-five per cent, of solid matter ; while recently cut peat contains only 
 ten per cent. It is heaped in embankments, where it is found not to 
 absorb water, and is dried by being spread out over iron plates warmed by 
 the waste steam from the compressing engine. In this way, according to 
 Mr. Hodgson, the peat standing in the bog in the morning may be har- 
 rowed and scraped, brought in, dried, compressed, and converted into an 
 excellent fuel before night. He employs for its compression, an engine 
 patented by himself; which he describes as a horizontal reciprocating ram, 
 working in a cylinder five feet long, with a uniform bore. The powdered 
 peat falls into this as the ram draws back at each stroke, and, soon filling 
 the whole length, considerable friction takes place against the sides of 
 the tube. This becomes so great that, as each charge falls in, it is com- 
 pletely consolidated between the advancing ram and the column of peat in 
 the tube, before the frictional resistance of the column is overcome, and 
 the whole mass moves on ; so that the blocks formed at the one end are 
 successively discharged at the other, at the rate of sixty a minute ; making 
 in a hour about fifteen hundred-weight of compressed peat, equal in density 
 to coal. This apparatus is now in operation at Derrylea, near Monas- 
 terevan ; and it is said by the inventor to leave no doubt of the practica- 
 bility of producing dry compressed peat on a large scale, and with profit." 
 Peat is not only an economical fuel for domestic use, but is in many 
 countries employed for generating steam, and for the manufacture of iron. 
 For the latter purpose, it is used in Sweden, France, and in many parts of 
 Germany, where the supplies of mineral coal are not abundant. It is par- 
 ticularly well fitted for producing steam, and compressed peat has now for 
 several years been used in locomotive engines in Bavaria ; but we are told 
 that before this application was successful, many difficulties had to be sur- 
 mounted. Several years ago, according to Sir Robert Kane, it was in 
 general use upon the steamers on the river Shannon in Ireland. 
 
CHAP. XXL] PEAT. 775 
 
 In a paper communicated to the Society of Arts in London in November, 
 1862, Dr. B. H. Paul whose experiments on the distillation of peat are 
 described farther on has given some interesting conclusions as to the rela- 
 tive values of peat and coal as fuel. According to him, while the calorific 
 or heat-giving power of carbon is represented as 1000, that of the various 
 mineral coals is equal to -from 903 to 906 ; while that of perfectly dried 
 peat, as deduced from its average composition, will be 660. But as Peatand 
 ordinary air-dried peat contains about one fourth its weight of water, its coal< 
 calorific power is reduced to 495 ; or about one half that of the same weight 
 of coal. The average weight of a cubic foot of solid coal is about eighty 
 pounds, while air-dried peat has a density corresponding to only sixty-four 
 pounds. A cubic foot of broken coal, however, contains about sixty pounds, 
 while the same volume of ordinary peat weighs only about thirty pounds ; 
 " so that with but half the calorific power, it takes twice the space ; and thus 
 to produce a given effect with air-dried peat, it would require twice the 
 weight, and four times the bulk, of the coal necessary to produce the same 
 effect." This calculation as to bulk, of course refers to uncompressed 
 peat : if reduced to the density of coal, as claimed by Mr. Hodgson's pro- 
 cess, its volume is of course diminished one half. From his own experience 
 in Lewes, Dr. Paul found, that, on the moors, where peat was to be had 
 for two shillings the ton, it could be economically used for generating steam, 
 and for burning bricks ; while at Stornaway, near by, where the cost of the 
 peat, delivered, was six or seven shillings, coal, which was eighteen shillings 
 the ton, was found more advantageous. He concludes that peat cannot be 
 economically transported to any considerable distance ; but that wherever 
 a peat having a fuel-value one half that of coal, can be delivered at the place 
 of consumption at a cost of four shillings sterling the ton, it may advan- 
 tageously replace coal, where this, under the same circumstances, costs 
 more than ten shillings ; but if the price of coal is ten shillings or less, 
 there would be a disadvantage in the use of peat. During four years Dr. 
 Paul used it as the only fuel under stationary steam-boilers, and found it 
 to answer admirably ; and he states that Mr. James Napier of Glasgow, 
 having tried it upon a steamer, is of opinion that it might be used in place 
 of coal. This, of course, applies to short voyages, and to conditions where 
 space is not a great consideration. It is a question for Lower Canada 
 whether properly dried peat can be furnished at a price per ton less than 
 two fifths that of coal ; in which case, it might perhaps be advantageously 
 employed hi our inland navigation. 
 
 Large quantities of peat charcoal are manufactured in France, and in p ea t 
 Germany. For this purpose, either ordinary stacks, or cylindrical kilns charcoal - 
 built of brick are employed. A current of steam, heated to 450 or 
 460 F., has likewise been employed for the purpose; and the compressed 
 peat has also been distilled in iron retorts, like those used for making coal 
 
776 GEOLOGY OP CANADA. [CHAP XXI. 
 
 gas ; by which means, volatile oils and combustible gas are obtained besides 
 the charcoal. Good air-dried peat, in stacks or in kilns, yields from 
 thirty to forty per cent, of its bulk, and from twenty-five to thirty-five per 
 cent, of its weight, of charcoal ; much of course depending on the amount 
 of ash which the peat contains. Large quantities of peat, and of peat char- 
 coal, are prepared for the market of Paris ; where the latter fuel is largely 
 used for domestic purposes. About fifty miles from Paris, near Liancourt, 
 on the Northern Railway, is a large bog ; from which, in 1855, 10,000 or 
 12,000 tons of peat were obtained. The peat from the whole thickness 
 of the bog, about ten feet, was transferred to flat-boats, trampled, and 
 turned over with shovels, and finally moulded by pressure into small 
 bricks, which when dried are heavier than water. These were charred 
 on the spot, and yielded about forty per cent, of charcoal, which gave 27-0 
 per cent, of ash; the dried peat itself yielding 10*0 or 11-0 per cent. 
 The wholesale price of this compressed peat in Paris was, at that time, 
 $3-75 the ton of 2200 pounds, while the charcoal made from it was 
 $18-00 the ton ; its retail price being about 124-00. Its combustion is 
 slower than wood charcoal, which was sold at about the same price ; while 
 both mineral coal and fire-wood were retailed at from 17*50 to $9-50 the 
 ton weight. These figures will aid in obtaining a notion of the compar- 
 ative value of the various kinds of fuel. 
 
 Distillation The object proposed by the Irish Peat Company, as already mentioned, 
 was the distillation of peat ; by which it is made to yield a tar, from which 
 are extracted illuminating and lubricating oils, and parafime ; besides 
 ammonia, acetic acid, and pyroxylic spirit, which are dissolved in the watery 
 products of the distillation. A large amount of combustible gas is also 
 disengaged ; which may be employed as a source of heat in various opera- 
 tions, such as distilling, burning bricks, and lime. By distilling the dried 
 peat in retorts, a considerable amount of tar is obtained, besides a residue 
 of coke or charcoal ; which, however, is not sufficient to heat the retorts, so 
 that there would be a farther expenditure for fuel. It was therefore desir- 
 able to devise some more simple and economical way of conducting the 
 distillation, and the works of the Company at Athy were built in accord- 
 Eeece's ance with the system patented by Mr. Rees Reece in 1849. This consists 
 process. m burning the air-dried peat, by means of a blast, in cylindrical furnaces 
 of brick, shaped somewhat like iron blast-furnaces, but closed at the top, 
 and furnished with pipes for carrying off the volatile products to a proper 
 condensing apparatus. The furnaces, being filled with peat, and closed, are 
 lighted from below, and the blast applied. The heat from the combustion 
 of the peat in the lower part of the furnace serves to distil the upper 
 layers ; while the gases from the combustion, together with the volatile 
 products of the distillation, are carried, forward by the blast towards the 
 condensers. 
 
CHAP. XXL] PEAT. 777 
 
 This process was to a certain extent successful ; but it was found that 
 when the force of the blast was augmented, in order to obtain a more rapid 
 combustion of the peat, the amount of tar was greatly diminished. Thus, 
 according to Dr. Paul it was found, by experiments in Antrim, with a fur- 
 nace three feet in diameter and fifteen feet in height, that when one and a 
 half tons of peat were burned in twenty-four hours, 3*1 per cent, of tar were 
 obtained ; with two tons in the same time, 1-8 per cent. ; with three tons, Results, 
 only 0*98 ; and when nine tons were burned in twenty-four hours, only two 
 pounds of tar were obtained to the ton. According to the experiments 
 
 of Sullivan, Irish peat, when distilled in retorts, gave from 1-5 to 3-5 per 
 cent., being an average of 2-5 per cent., of tar ; which furnished from 38-0 
 to 72-0 per cent, of oil, the mean being 52-0 per cent. Of this oil, 5-0 
 per cent, distilled below 212 F. ; 20-0 per cent, between 260 and 320 
 85-0 per cent, between 320 and 550 ; and the residue at a still higher 
 temperature. Hence, as an average, 100 tons of Irish peat would yield 
 682 gallons of tar, and 333 gallons of refined oils. It was found that, 
 under favorable conditions, the amount of tar obtained by Mr. Reece's 
 process was very nearly equal to that produced by distilling the same peat 
 in closed retorts. 
 
 Dr. Paul has lately undertaken a series of experiments on the distilla- 
 tion of peat on a large scale, at Stornaway in the island of Lewes ; the 
 results of which he communicated to the British Association for the 
 Advancement of Science, at Cambridge, in October, 1862. The mountain 
 peat of that region is compact, heavier than water, and is superior for this 
 manufacture to ordinary bog peat. By distillation in a retort, it gave : 
 tar 9-08, coke 31-50, water 37-88, gas (loss) 21-54; = 100-00. The 
 tar thus obtained was a soft solid at 60 F. ; it had a specific gravity of 
 960, an acid reaction, and gave, by rectification, forty-two per cent, of a 
 refined oil, boiling above 300 ; besides from thirty to forty-six per cent, of 
 more volatile liquids. These, as well as the ammonia, acetic acid, and 
 pyroxylic spirit were neglected by Dr. Paul in his experiments. The refined 
 oil contained about one tenth its weight of paraffine (equal to four per 
 cent, of the crude tar). About one half of the oil boiled at a temperature 
 between 330 and 500 F. ; it burned without charring the wick, had but 
 little odor, was not explosive at ordinary temperatures, and compared 
 favorably with' refined petroleum. The remainder, which boiled between 
 500 and 600 F., had a specific gravity of -850, and when mingled with 
 fat oils was an excellent lubricator. 
 
 In his early attempts to work this peat on a large scale, by distillation Paul's 
 in brick furnaces or kilns, Dr. Paul substituted for the blast the draught ex P erimente - 
 of a chimney ; but in this way he was unable to obtain more than three per 
 cent, of tar, instead of the nine per cent, which the same peat furnished 
 when distilled in retorts. It was found, moreover, that, on an average, 
 
T78 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 only about fifty tons a week were distilled in each kiln ; while in order to 
 give a profitable return it was necessary to work about seventy tons weekly, 
 and to obtain five per cent, of tar. His apparatus consisted of cylindrical 
 brick chambers, five feet in diameter and twelve feet high ; furnished at 
 the bottom with a fire-grate having an area of two feet, and at the top 
 with a hopper and lid for feeding. Ten of these kilns were built side by 
 side, in a block ; and from the top of each, a pipe of twelve inches in diam- 
 eter led to a main of three feet, and thence, through a condensing appa- 
 ratus, to a chimney. In order to secure a regular current of air through 
 the apparatus, a draught was finally established by means of a thirty-inch 
 fan, of Schiele's patent, making 1600 revolutions a minute, and driven by 
 an eight-inch steam-engine ; which worked at the same time some pumps, 
 and a winding-drum by which the peat was drawn up an incline to the 
 kilns. This fan was capable of passing 2000 cubic feet of gas per minute, 
 and of maintaining a steady powerful draught through seven inches of 
 water, without raising the combustion at the fire-grate of the kiln to a 
 greater extent than was desirable. By this means the vapor was rapidly 
 drawn from the kilns, and was passed several times through water, and 
 also through four chambers filled with bundles of heather. This contri- 
 vance was found effectual to separate the tarry matter mechanically sus- 
 pended and carried over by the current of gas. This, when discharged from 
 the fan, was highly inflammable, and was led by an underground tunnel to 
 a proper furnace ; where it burned with a flame from six to ten feet high, 
 six feet long and six inches thick, and was available for generating steam, 
 distilling tar, evaporating liquids, or drying peat. It was found that the 
 whole of the charred peat was not required for the distillation ; so that by 
 means of an arched opening fitted with a door, just above the fire-grate, a 
 portion of the charcoal could be removed from time to time. By this 
 means, the amount of peat which could be worked was much increased. 
 The removal of the charcoal in this way was however attended with diffi- 
 culty during the prevalence of high winds. 
 
 Results. With these improved arrangements, it was found that the amount of 
 peat distilled was always above seventy tons, and in favorable weather 
 upwards of one hundred tons, weekly, for each kiln ; while the proportion 
 of tar was raised from 3*9 per cent, to 7*5, and was on average as much 
 as 7*0 per cent. In this way there were obtained in the year 1861-62, 
 from one hundred tons of peat 
 
 749 gallons of oil (with paraffine), at 2s, 74 18 
 
 From which is to be deducted 
 
 For 100 tons of peat, at 2s, 10 
 
 " cost of manufacture, 2814 6 
 
 38 14 6 
 
 Leaving a balance of 36 3 6 
 
CHAP. XXL] PEAT. 779 
 
 These are given by Dr. Paul as his working results within the last year, 
 and contrast most favorably -with those obtained in Ireland, as stated by 
 Mr. Sullivan in his report to the directors of the Irish Peat Company in 
 1855 ; according to which, one hundred tons of peat gave 
 
 150 gallons of oil, at 2s., 15 
 
 300 pounds of paraffine, at Is., 15 
 
 52 gallons of wood-naphtha, 210 
 
 3 cwt. of sulphate of ammonia, 116 
 
 34 6 
 
 From which is to be deducted 
 
 For 100 tons of peat, at 4s., 20 
 
 " cost of manufacture, 14 3 4 
 
 34 3 
 
 Leaving a balance of 2 8 
 
 It will be seen that the cost of the Irish bog peat was, for reasons 
 already mentioned, 4s., instead of 2s., the ton; while its yield was so 
 much less than that of Lewes, that, even at an expense of manufacturing 
 which was only one half the latter, its distillation appears to have been no 
 longer profitable ; although the wood-naphtha, or pyroxylic spirit, and the sul- 
 phate of ammonia, products neglected by Dr. Paul, were preserved. While 
 some of the advantages of the results obtained at Lewes are to be ascribed 
 to the method pursued, the superior quality of the peat is, according to 
 Dr. Paul, a more important element. The light refined oil from the on from 
 Lewes peat was sold in 1862 in Glasgow, under the name of lignole ; peat- 
 and according to the report of Dr. Anderson, it compared favorably with 
 the burning oils from coal, shale, and petroleum ; being pale in color, and 
 with much less unpleasant odor than the coal oils. The statements of 
 Armand that peat may be made to yield as much as fifteen, or even 
 eighteen per cent., of tar, do not appear to be confirmed by other inves- 
 tigators. According to Vohl, who in 1858 published an elaborate inves- 
 tigation into the distillation of lignite, peat, and bituminous schists, the 
 various peats, when distilled in retorts, yield from six to nine per cent, of 
 tar ; and in the case of a light peat, 5'37 per cent. In rectifying the tar, 
 the distillation may be carried to dryness, when it is wished to obtain the 
 greatest amount of liquid products, as in Dr. Paul's operations. By 
 arresting the process at the proper point, a large proportion of the material 
 remains in the retort, as a kind of pitch ; which may be used, like asphalt 
 or solid bitumen, for covering roofs and similar purposes. In this way, 
 according to Vohl, one hundred parts of tar yield forty-two parts of pitch. 
 In order to purify the distilled oil, for burning in lamps, it is first treated 
 with a solution of soda, and afterwards with concentrated sulphuric acid, 
 as in the refining of petroleum. The alkaline solution dissolves a consid- 
 erable amount of creosote and of carbolic acid ; which may be after- 
 
780 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 wards separated by means of an acid, and have a commercial value. 
 The paraffine separates in a crystalline form from the heavier and less vola- 
 tile oils, when these are exposed to cold. With the present demand for 
 oils and paraffine, it is more profitable to distill the tar to dryness, than to 
 manufacture a portion of it into pitch. The value of a ton of crude tar, 
 capable of yielding one hundred gallons of oil and paraffine, may, accord- 
 ing to Dr. Paul, be estimated at 5 sterling ; and he concludes that peat 
 approaching in richness to that of the Highlands of Scotland may be dis- 
 tilled with great profit. It remains to be seen whether some of the exten- 
 sive peat bogs of Canada may not produce a material equally available. 
 The importance of these deposits as a source of fuel to the country should 
 not, however, be lost sight of; and it is to be hoped that before long 
 successful attempts may be made to introduce compressed peat as a combus- 
 tible, for the generation of steam and for domestic purposes. 
 
 The principal deposits of peat which are as yet known in Canada, will 
 now be noticed. It is to be remarked, that, with the exception of a partial 
 trial made of the peat near Chambly, none of these deposits have ever yet 
 been worked ; and that it is only in a few localities that the thickness of the 
 peat has been determined by pits, or by borings. Beginning to the west- 
 ward, a deposit of peat occurs on the twelfth lot of the fourth and fifth ranges 
 
 Sheffield, of Sheffield ; where it overlies a bed of marl already described, and extends 
 over three or four hundred acres. The average thickness of the peat is 
 about four feet, and it is said to be of superior quality. In the level region 
 between the St. Lawrence and Ottawa rivers, described on page 8, several 
 large peat bogs occur ; but from their nature, the vicinity has been avoided 
 by settlers, and they are therefore difficult of access. There is said to be 
 a considerable area of peat in the rear of the seigniories of Vaudreuil and 
 
 Caledonia. Rigaud ; and also in Caledonia, where its thickness does not appear to 
 exceed three or four feet. Peat occurs at the sources of the Pain River 
 in Roxburgh, Osnabruck, and Finch ; and also in Clarence, Cumberland, and 
 
 Gloucester. Gloucester. In the third, fourth, and fifth ranges of the latter township is 
 a tract known as the Mer Bleue, which consists of two long peat bogs, sepa- 
 rated by a narrow ridge of higher land, and occupying each about 2500 
 acres. These deposits were sounded in many places, with a rod, to a depth 
 of twenty-one feet, without finding bottom ; in other parts, the peat was 
 from eight to fifteen feet in thickness. This tract is situated only three 
 miles from the Ottawa, and is about 280 feet above the level of the sea. 
 
 Nepean. Three large areas of peat, of from 1000 to 3000 acres each, occur in Nepean 
 and Goulbourn ; one of them to the east, and two to the west, of the village 
 of Richmond. It is also found on the third and eight ranges of Beckwith, 
 to the east of Mississippi Lake ; and an area of about 3000 acres of peat 
 occurs in Westmeath, in the rear of front A, and from the first to the fifth 
 range behind it. In the ninth and tenth ranges of Huntley, there are about 
 
CHAP. XXL] PEAT. 781 
 
 2500 acres of peat ; which in some parts has a thickness of eight or ten Huntiey. 
 feet, while in other parts no bottom was found at a depth of fifteen feet. 
 It is probable that peat may be met with in many other localities through- 
 out this region. 
 
 On the north side of the Ottawa, three small areas of peat have been 
 observed in Grenville. One of these, on the fourth and fifth lots, covers Grenvme. 
 about thirty-six acres, and has a depth of ten feet. It has been used in 
 the neighborhood, and is pronounced of excellent quality. Another deposit 
 of about the same extent occurs on the first lot of the same range, and is 
 in some parts more than fifteen feet in thickness. A third, of about 
 thirty acres, occurs on the fourth lot of the seventh range. On the 
 fourth and fifth lots of the first range of Harrington, is a bog of about Harrington, 
 forty acres, the peat of which varies in depth from ten to twenty-five 
 feet. Another bog is described as occurring on the first and second lots of 
 the fifth range of the same township. It extends over about sixty acres, 
 and has a thickness, in some parts, of twenty-five feet. All of these areas 
 might be drained without much difficulty. To the eastward of this, a peat 
 bog is met with in the Rang Double of Mille-Iles. It exhibits a breadth, Mine-lies. 
 on the road from St. Janvier to St. Jerome, of about half a mile, and has 
 an area of perhaps five eighths of a square mile. Its depth along the road 
 was found to be in several places from two to eighteen feet, the greater 
 depth being towards the southeast side, and its average may be taken at 
 eight feet. A smaller deposit of peat occurs half a mile nearer to St. Jan- 
 vier ; it has a breadth of about a quarter of a mile, but its superficies and 
 depth have not been ascertained. Upon the same great plain with these, 
 a little to the north of the church of Ste. Anne des Plaines, and on the ste. Anne, 
 northeast side of the road leading to New Glasgow, is a peat bog having an 
 area of about a square mile. Its depth was not determined, but it is sup- 
 posed to average about five feet. The farmers are in the habit of burn- 
 ing the surface of parts of this bog, and employing the ashes as a manure 
 for the underlying portions, until by repeated burnings they reach the 
 subjacent clay ; which, mingled with the last thin layer of peat and a 
 portion of the ash, constitutes a very fruitful soil. 
 
 Near the front of the seigniories of Assumption and St. Sulpice there is St. suipice. 
 a peat bog three and a half miles in length, with an average breadth of 
 half a mile, giving an area of about 1100 acres. Its depth varies from 
 two to fifteen feet ; and the result of ten trials, made in two lines across the 
 bog, gave an average of ten feet. In the seigniories of Lavaltrie and Lavaitrie. 
 Lanoraye, there are two extensive peat bogs, running parallel with each 
 other. Of these, the northern is the larger, and is known as the Grande 
 Savanne. It has a length of about eight miles from northeast to south- 
 west, and a breadth of from half a mile to two miles and a half, covering a 
 superficies of from twelve to fifteen square miles. Two sections were 
 
782 GEOLOGY OP CANADA. [CHAP. XXI. 
 
 made across this bog ; one on the line of the railway between Lanoraye 
 and Industry, which traverses it about three miles from its southwest 
 extremity. It here reaches to within four miles of the St. Lawrence, and 
 has a breadth of two and a half miles. The depth along this line was 
 found to be from four to fourteen feet ; the average of twelve trials giving 
 about eleven feet. The other section, along the Lavaltrie road, about four 
 miles to the northeast, gave a breadth of half a mile, and a depth of from 
 seven to fourteen feet ; averaging, as before, eleven feet. The smaller of 
 these bogs lies between that just described, and the St. Lawrence, at a dis- 
 tance from the last of about two miles. On the line of the railway it has 
 a breadth of over half a mile, and an average thickness of about five feet. 
 It has a length of more than five miles, extending four and a half miles to 
 the southwest of the railway, and a superficies of about three square miles. 
 St. Maurice. In the fief St. Etienne, about a mile and three quarters southwest of the 
 Grs, on the St. Maurice river, the main road crosses a peat bog, which 
 is there half a mile in breadth, with an average depth of about six feet. Its 
 extent to the northeast and southwest has not been ascertained. Another 
 champiain. was met with in the seigniory of Champlain, about three miles from the 
 St. Lawrence, and on the road from the church to the river Champlain. 
 Its breadth on the road is about three quarters of a mile, and its average 
 depth, in this part, five feet. Its length from northeast to southwest 
 appears to be about two miles ; giving to the bog an area of about a mile 
 and three quarters. In the fief D'Auteuil, on the road between Cap Sante* 
 and the village of L'Enfant Jsus, there is a peat bog, with a breadth of 
 about a quarter of a mile, which has not been farther examined. Several 
 other peat bogs are known to exist between this last locality and the 
 vicinity of Quebec. 
 
 On the south side of the St. Lawrence, there is a large area occupied 
 by peat on the west side of the river Richelieu. It covers portions of the 
 Lacolle. seigniories De Lery and Lacolle, and of the townships of Sherrington 
 and Hemmingford, embracing perhaps fifteen or twenty square miles. This 
 area is drained in part by the Lacolle River. It has not been carefully 
 examined as yet ; but it contains in some parts, particularly it is said in Sher- 
 sherrington. rington, a very great thickness of peat. Of two specimens from this 
 township, one, which was dark colored, fine grained, compact, and so heavy 
 as to sink in water, gave only 3-53 per cent, of ash ; while the lighter 
 peat, from near the surface of the bog, yielded 4-66 per cent, of ash 
 (page 642). Both of these are very pure ; and the compact peat, which 
 is remarkable from its great density, and its freedom from earthy matters, 
 is particularly worthy of attention. 
 
 Longueuii. A large peat bog occurs in the seigniory of Longueuil, on the road to 
 Chambly ; and an attempt was made a few years since to raise the peat, 
 and introduce it to the Montreal market. A peat bog of large size is found 
 
CHAP. XXL] PEAT. 783 
 
 in the seigniory of Ste. Marie de Monnoir ; and another in the parish of 
 St. Dominique, including parts of Ste. Rosalie and St. Pie. Its dimen- St. Dominique, 
 sions may be five or six miles in one direction, by three or four in another. 
 This extent is covered by a layer of peat ; which, from two or three feet at 
 the edges, attains a depth of six feet, and in some parts, it is said, is 
 eighteen feet in thickness. The bog has been partially drained, and por- 
 tions of the land reclaimed for agricultural purposes. The drained land, 
 being first cleared of trees, is ploughed, and then, in the dry season, set 
 on fire. In this way, eight or ten inches of peat are burned, leaving an 
 ash which serves as a manure, and enables the surface to yield one or two 
 crops of barley or oats. After two years, the soil becomes exhausted, and 
 it requires to be again burned over to render it productive. When, by 
 several repetitions of the process, the peat has been reduced to a few 
 inches, the remaining portion is mingled, by ploughing, with the underlying 
 clay, and a rich mellow soil is obtained. The peat from this bog yields, 
 when heated in close vessels, about thirty-six per cent, of coke, and 
 contains from six to seven per cent, of ash, whose composition has been 
 given on page 642. 
 
 In the seigniory of Riviere Ouelle, there is a peat bog which covers Km6re Oueiie. 
 about 4000 acres ; and another one occurs in the seigniory of Riviere du 
 Loup, having a superficies of 6000 acres. Its breadth on the Temiscouata 
 road is a mile and a quarter, and its depth in some parts has been ascer- 
 tained to be eighteen feet. Peat is found in abundance on the first and 
 second concessions of the seigniory of lie Verte ; and from a point two n e Verte. 
 miles below the Rimouski, there is a belt of peat bog extending nearly all 
 the way to the Metis River, a length of over twenty miles. Its distance 
 from the St. Lawrence is from a quarter to half a mile, and its breadth 
 from a quarter of a mile to a mile. The depth of the deposit, where 
 observed, was from one to six feet. To the east of the Rimouski River, there 
 is a peat bog, which has a length of three or four miles, in the townships of 
 Duquesne and Macpes; with a breadth of about three quarters of a niile,and Duquesne. 
 a thickness which was found to be from five to twelve feet : it is said to be 
 in one place, thirty feet in depth. Another locality of peat is stated to 
 be in the townships of Matanne and Macnider, between the rivers Blanche 
 and Matanne. A peat bog of about one hundred acres occurs on the left 
 bank of the Madawaska, just above the twelfth mile-post on the road to 
 the Little Falls. 
 
 The most extensive peat deposits in Canada are found on Anticosti. Along Anticosti. 
 the low lands on the south coast of the island, from Heath Point to within 
 eight or nine miles of Southwest Point, a continuous plain covered with 
 peat extends for upwards of eighty miles, with an average breadth of two 
 miles ; thus giving a superficies of more than one hundred and sixty square 
 miles. The thickness of the peat, as observed on the coast, was from three 
 
784 GEOLOGY OF CANADA. [CHAP. XXL 
 
 to ten feet, and it appears to be of an excellent quality. The height of 
 this plain may be, on an average, fifteen feet above high-water mark, and 
 it could be easily drained and worked. Between Southwest Point and the 
 west end of the island, there are many smaller peat bogs, varying in 
 superficies from 100 to 1000 acres. 
 
 BITUMINOUS SHALE. 
 
 Bituminous The bituminous shales or pyroschists of Canada, have been mentioned on 
 shales. p a g e 528 ; and described, with analyses, on pages 622 and 627. It has 
 
 there been shown that these rocks contain little or no bitumen ; but an ad- 
 mixture of a hydrocarbonaceous substance, which, like peat and coal, yields, 
 by distillation, combustible gases and volatile oils. When sufficiently rich 
 in these matters, bituminous . shales are distilled with advantage. The 
 amount of oil furnished by different shales may vary from an insignificant 
 quantity, up to twenty per cent, or more. The bituminous shales of Canada, 
 as already described, belong to two different geological positions ; the one 
 in the Utica formation, whose distribution has been given in the tenth chap- 
 ter, and which may be traced from below Quebec to the shores of Lake 
 Huron ; the other belongs to the Devonian series, and, as described on page 
 387, is only met with in the southwestern portion of Canada, in Bosan- 
 quet and its vicinity. These shales, when exposed to heat, give off a vapor, 
 which takes fire and burns into a bright smoky flame. The shales of the 
 Utica formation, in Eastern Canada, so far as yet examined, are less rich 
 in combustible matter, than those farther west. In Collingwood, on the 
 twenty-third lot of the third range, there is an exposure of this shale, where 
 a layer of about seven feet in thickness has been employed for distillation. 
 This rock, as will be seen by the analysis on page 622, is highly calca- 
 reous, containing more than one half its weight of carbonate of lime. When 
 ignited in a close vessel, it loses 12-4 per cent, of volatile and combustible 
 matters ; of which from three to four per cent, are condensable into an oily 
 liquid. This, when rectified, yields oils fitted for burning and for lubrica- 
 ting purposes, and probably also a portion of paraffine. 
 
 Collingwood. In 1859, works for obtaining these oils were erected on the locality of 
 this shale, near the town of Collingwood. Twenty-four longitudinal cast- 
 iron retorts were set in two ranges, and heated by means of wood ; of which 
 twenty-five cords are said to have been required weekly. The shale, broken 
 into small fragments, was heated for two or three hours ; from eight to ten 
 charges being distilled in twenty-four hours. In this way, it is said from 
 thirty to thirty-six tons of shale were distilled daily, and made to yield 250 
 gallons of crude oil, corresponding to about three per cent, of the rock. 
 By a farther continuance of the heat, a small additional proportion of oil 
 was obtained from the shale ; but it was found more economical to withdraw 
 
CHAP. XXI.] BITUMINOUS SHALE. 735 
 
 the charge after two hours and a half. The bed of shale available for the on from 
 purpose, adjoins the works, and was furnished, ready broken, at twenty 8hale 
 cents the ton. The cost of the crude oil from the shale, was stated by the 
 manufacturers to be fourteen cents the gallon. When rectified and de- 
 odorized, it gave from forty to fifty per cent, of burning oil, and from twenty 
 to twenty-five per cent, of pitch and waste, the remainder being a heavy oil 
 fitted for lubricating purposes. After two or three unsuccessful trials, 
 and the repeated destruction of the works by fire, they were at last, in 1860, 
 got into successful operation, and a ready market was found for the oils. 
 Data are however wanting to show whether the enterprise was remunera- 
 tive ; and it was after some time abandoned, partly, it is probable, on 
 account of the competition of the petroleum of Enniskillen, which was about 
 that time brought into the market in large quantities, and at a very low 
 price. Should it however, at any time, be found advantageous to renew 
 the experiment of distilling the bituminous shales of this formation, those 
 of Collingwood offer very favorable conditions, from their accessible position, 
 and also from the ready means of transport afforded both by the lake and 
 the railway. 
 
 The shales of the Devonian series in Bosanquet, whose analysis is given 
 on page 627, are not less rich in combustible materials than those of Col- 
 lingwood. An experiment made on a small scale, gave 4*2 per cent, of oil, 
 which is equal to about ten gallons to the ton of shale. The specimen was 
 obtained from Cape Ipperwash, where a section of twelve or fourteen feet 
 of the shales is exposed. They here contain so much organic matter, that 
 the broken shale, which forms the shingle of the beach, is said, when set on 
 fire, to continue burning for a considerable time. Large portions have been 
 thus burned, and have assumed a reddish color. These shales are also 
 seen in Warwick, and in Brooke (page 388). 
 
 In describing the rocks near Port Daniel, mention was made on page Gaspe. 
 445, of beds of bituminous shales. These are said to yield considerable 
 quantities of oil by distillation. The specimens procured from this locality 
 some years ago by the Survey, were lost by shipwreck ; and no opportu- 
 nity of replacing them having since occurred, it is impossible to give any 
 farther facts respecting the shales of this deposit. 
 
 BITUMENS. 
 
 Under the head of bitumens are generally included both the liquid 
 form, which is distinguished by the name of petroleum or rock oil, and 
 the solid varieties, known as mineral pitch or asphalt. These have been 
 already noticed, and the principal facts relating to their occurrence in 
 Canada are discussed on pages 378, and 521-524. It is now proposed 
 to give some further details as to their economic relations, together with a 
 
 zz 
 
786 
 
 GEOLOGY OF CANADA. 
 
 . XXI. 
 
 Enniskillen. 
 
 Amount of 
 oil. 
 
 description of the facts recently observed with regard to the petroleum of 
 Gasp^. As a sequel to this, will be noticed a peculiar mineral resin lately 
 discovered in the Devonian rocks of that region. 
 
 It has already been shown that the petroleum of Canada occurs in two 
 distinct horizons ; the one in the limestones of the Trenton group, and the 
 other in those of the Corniferous formation. To this it must now be 
 added, that the petroleum of Gasp6 probably belongs to an intermediate 
 position, and is to be referred to limestones of Upper Silurian age. It is 
 from the Corniferous formation, which affords a much more abundant 
 supply than the Trenton group, that the springs of Western Canada take 
 their source. In some cases, the wells are sunk directly in the Cornif- 
 erous limestone ; but in Enniskillen they are bored in the overlying shales 
 of the Hamilton formation ; which have there a thickness of from two to three 
 hundred feet (page 386), and are overlaid by from forty to sixty feet of 
 clay and gravel. In these latter are sunk what are called the surface 
 wells, from which considerable quantities of oil were at first obtained. 
 The deeper wells have however given by far the greater supply of oil ; 
 and in some of them, when first opened, the petroleum has risen above the 
 surface of the earth, constituting what are called flowing wells. One of 
 these, which was sunk to a depth of about 200 feet, is said to have yielded, 
 when first opened, not less than 2000 barrels in twenty-four hours ; and 
 several others gave very large quantities. In many cases both oil and 
 water flow into these wells, and the water in some of the deeper ones is 
 saline. The recently opened wells have frequently been observed to fur- 
 nish petroleum only, which however after some time is accompanied with 
 a portion of water. These wells are chiefly in an area of about four 
 square miles in the first three ranges of Enniskillen. About six miles 
 to the northward however, on lots thirteen and fourteen of the tenth and 
 eleventh ranges of the same township, numerous wells have also been 
 sunk, and considerable quantities of oil obtained. The total amount of 
 petroleum extracted from these various wells in Enniskillen, since their 
 opening, may be seen from the returns kindly furnished by the freight 
 agent of the Great Western Railway ; over which the produce of this 
 district finds its way to market. A small portion of the petroleum is 
 refined in the vicinity, and this is included with the crude material in the 
 following statement : 
 
 Previous to July 31, 1861 
 
 For the half-year ending January 31, 1862. 
 Do. do. July 31, 1862 . . . , 
 
 Do, do. January 31, 1863, 
 
 For the month of February, 1863 
 
 5,529 barrels. 
 
 6,246 
 25,264 " 
 57,550 " 
 
 8,8 74 " 
 
 Number of barrels of forty gallons each 103,463 
 
 Giving a total yield of 4,138,520 gallons. 
 
CHAP. XXL] PETROLEUM. 787 
 
 The region occupied by the Corniferous formation in Western Canada, 
 may be defined as the whole of that portion of the province lying to the 
 south and west of a curved line running from the outlet of Lake Erie, and 
 passing through Stratford, to a point on Lake Huron near the mouth of the 
 Saugeen River. The shales of the Hamilton formation, and those of the 
 Portage and Chemung group, cover this limestone over a small area, but 
 by far the greater part is only overlaid by the superficial clays and sands. 
 It will be seen from the descriptions already given, that the petroleum of jt s accumu- 
 Enniskillen appears to be accumulated, either in the superficial sand and la 
 gravel, as in the surface wells ; or in the shales which overlie the true oil- 
 bearing rock. In the same way, the oil wells of western Pennsylvania, 
 and many of those in Ohio, are sunk in a thick mass of Devonian sand- 
 stone, which there overlies the Hamilton formation, but which has been 
 removed from southwestern Canada by denudation. . This sandstone 
 appears, like the overlying shales and the gravels of Enniskillen, to have 
 served as a reservoir, in which the oil rising from the limestone has been 
 held, and prevented from flowing away at the surface. Over a great 
 part of Western Canada, on the contrary, the oil-bearing limestone is 
 destitute of any covering except the superficial clays and sands ; and 
 thus, during long ages, the petroleum has been escaping from the surface, 
 and has been lost, instead of being retained, as in the case where higher 
 rocks are present. In Oxford and Mosa, and in Dereham, where only 
 clay and sand overlie the Corniferous limestone, natural springs are 
 found, yielding small quantities of oil ; but neither the wells sunk in the 
 clays of these regions, nor the borings into the limestones beneath, have 
 as yet furnished any large amount of petroleum. Small portions of it 
 are however still escaping at these points ; which are on the lines of anti- 
 clinal fold and fracture, and are thus the natural localities both for the 
 accumulation and the discharge of the petroleum contained in the subjacent 
 upraised strata. These oil-springs are seen along the banks of the Thames, 
 for a distance of about four miles, in the townships of Oxford and Mosa. oxford. 
 The Corniferous limestone is here covered by a considerable depth of clay, 
 through which several wells have been sunk, and the rock beneath in some 
 cases has been drilled. One of these wells, at a depth of seventy feet in 
 the clay, yielded a few hundred gallons of oil ; but the vicinity has not so 
 far furnished any considerable quantity. Near Tilsonburg, in Dereham, 
 two wells were sunk in 1861. In one of these, after passing through thirty 
 feet of clay, a boring of ninety-six feet was made in the Corniferous lime- 
 stone. A fissure yielding petroleum was met with at twenty-five feet in 
 the rock, and another at thirty-eight feet, which discharged small quan- 
 tities of oil, with abundance of water and of gas at intervals. Some oil 
 was also obtained beneath the clay, at the surface of the rock. 
 
 The wells of Enniskillen continued to yield large supplies of petroleum 
 
788 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 during a period of eighteen months ; but about the commencement of 
 1863 it was announced that the discharge from the flowing wells had 
 become intermittent, and finally ceased entirely; although there are 
 many wells which have continued to furnish considerable quantities of 
 oil by pumping. Some of these wells have however, it is said, 
 resumed their flow again at intervals ; and it is not improbable, that, 
 as the rising of the oil to the surface, or above it, is dependant upon 
 hydrostatic pressure, the partial check to the flow of the superficial 
 waters, dependant upon the winter frosts, may be one of the causes 
 of the diminished discharge of petroleum. At the same time, it must 
 be remarked, that the experience of the oil region in Pennsylvania has 
 already shown that the supply from these flowing wells soon dimin- 
 ishes, and eventually fails. It has also been observed, that contiguous 
 wells are frequently connected with the same oil-yielding fissure, so as 
 to affect one another's supply. In some cases, air passes down one shaft 
 when the oil is pumped from an adjoining one. In like manner, it was 
 found in Enniskillen that when one of the most abundant of the wells was 
 allowed to flow for some time, the oil disappeared from several of the 
 Future adjoining wells. It is evident that the exhaustion of these reservoirs of 
 supply. Q ^ - g j^ a q ues ti on O f time ; but while the petroleum springs of some 
 regions have failed, those of Burmah, Persia, and Zante* still continue to 
 flow. The present demand for petroleum has however caused a great 
 number of wells to be sunk in the oil regions of America, which must 
 tend to a proportionally rapid exhaustion of the sources. It is however 
 not improbable that farther supplies of this material may ultimately be 
 found in other portions of the country underlaid by the Corniferous for- 
 mation ; and the possibility of its occurrence in available quantities in 
 some part of the Trenton formation should not be lost sight of, although 
 this has never hitherto furnished any considerable amount of petroleum. 
 
 The presence of petroleum in the rocks of Gaspe* has been mentioned on 
 pages 402 and 521. Subsequent explorations have shown several addi- 
 tional localities in the vicinity of Gaspe* Bay. The limestones of this 
 Gaspe. region, which are regarded as of Upper Silurian age, and referred to the 
 Lower Helderberg group of the New York geologists, are observed in 
 various points on the Dartmouth, York, and Malbay Rivers to be more or 
 less impregnated with petroleum. These limestones are generally dark 
 bluish-grey, with layers and nodules of chert, and are traversed by numer- 
 ous veins of white calc-spar, sometimes including drusy cavities. These 
 often hold petroleum, which impregnates the calc-spar, and is seen to rise 
 to the surface when freshly broken fragments of the rock are thrown into 
 water. Few or no fossils are found in these beds, and no petroleum was 
 obtained at Cape Graspe* in the fossiliferous portions of these limestones. 
 In many places throughout this region the limestone is overlaid by a 
 
CHAP. XXL] PETROLEUM. 789 
 
 sandstone, the lower portion of which is regarded as of the age of the 
 Oriskany formation (page 403). This rock near the mouth of York 
 River, is, like the limestone, impregnated with petroleum ; and on the 
 same river, about twelve miles from the entrance of Gaspe* Basin, small 
 portions of solid bitumen were found in the cavities of a trap dyke cutting 
 the sandstone. A similar dyke at Tar Point has already been described. 
 
 At the oil spring at Silver Brook, a tributary of the York River, the petro- saver 
 leum oozes from a mass of sandstone and arenaceous shale, which dips Brook - 
 southeastwardly at an angle of 13, and is nearly a mile to the south of 
 the crown of the anticlinal. The oil, which here collects in pools along the 
 brook, has a greenish color, and an aromatic odor, which is less disagree- 
 able than that of the petroleum of Western Canada. From a boring 
 which has been sunk in the sandstone to a depth of about 200 feet, there 
 is an abundant flow of water, accompanied with a little gas, and very small 
 quantities of oil. Farther westward, at about twelve miles from the 
 mouth of the river, oil was observed on the surface of the water at the 
 outcrop of the limestone. Petroleum is met with at Adams's oil spring, in 
 the rear of lot B of York, nearly two miles east of south from the entrance 
 of Gasp6 Basin. It is here found in small quantities floating upon the 
 surface of the water ; and near by is a layer of thickened petroleum, mixed 
 with mould, at a depth of a foot beneath the surface of the soil. A mile to 
 the eastward, at Sandy Beach, oil is said to occur ; and again at Haldi- 
 mandtown, where it rises through the mud on the shore. These three 
 localities are upon the sandstone, and on the line of the northern anti- 
 clinal (page 398), which passes a little to the north of the Silver Brook 
 oil spring. Farther to the southeast, on the line of the southern anticlinal, 
 and about two miles west of Tar Point, which takes its name from the 
 petroleum found there (page 402), another oil spring is said to be found, 
 three quarters of a mile south of Seal Cove. On the south side of the 
 Douglastown Lagoon, and about a mile west of the village, oil rises in 
 small quantities from the mud on the beach. A well has here been bored 
 to a depth of 125 feet in the sandstone, which dips to the southwest at an 
 angle of 10 ; but traces only of oil have been obtained. Farther to the 
 westward, oil is said to occur on the second fork of the Douglastown 
 River. Traces of it have also been observed in a brook near St. George's 
 Cove, on the northeast side of Gaspe Bay. In none of these localities do 
 the springs yield any large quantities of oil ; nor have the borings, which 
 have been made in two places, been as yet successful. The above indica- 
 tions are however interesting, inasmuch as they show the existence of 
 petroleum over a considerable area in this region, some part of which 
 may perhaps furnish available quantities of this material. 
 
 The petroleum of Western Canada is, like that of other regions, a mixture 
 of hydrocarbons differing in volatility ; which are partially separated in the 
 
790 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 process of distillation. The less volatile and denser portions, which contain 
 a quantity of paraffine in solution, are employed for the purpose of lubri- 
 cating machinery, either alone or mingled with a fat oil ; while the more 
 volatile and lighter portions, after being properly purified, are employed 
 for burning hi lamps. The offensive, and somewhat alliaceous odor of the 
 unrefined petroleum of Enniskillen, is probably due, in part, to some sul- 
 phuretted compound which the oil contains. When the crude petroleum 
 from this place is rapidly decomposed at a red heat, and converted into 
 gas, this is found to contain a little sulphuretted hydrogen. Some of 
 the petroleums from Pennsylvania yield, by distillation, a considerable quan- 
 tity of very volatile hydrocarbons ; which give off so much vapor, even at 
 ordinary temperatures, as to form explosive mixtures with air. The pro- 
 portion of these more volatile oils in the petroleum of Enniskillen is how- 
 ever much smaller. These oils are now separated by the refiners ; and 
 as a substitute for oil of turpentine, they have become an important article of 
 
 Naphtha, commerce. They are frequently known by the name of benzole ; but they 
 are really a kind of mineral naphtha, and contain no benzole, or only but 
 traces of it. They are consequently sold at a price very much less 
 than true benzole ; which is valuable as the source of aniline, now so 
 much used in the manufacture of fine dyes. Benzole, which differs widely 
 from these naphthas in composition, is a result of the distillation of coal ; 
 and as petroleum and its products were introduced to common use as a sub- 
 stitute for the oils previously obtained from coal, it is easy to understand 
 how the name of benzole became transferred to the naphtha, and that of 
 coal oil to the products which have now so generally replaced it. The 
 
 Refining, purification and de-odorization of the distilled petroleum is effected chiefly 
 by treatment with strong sulphuric acid, which is followed by a solution of 
 caustic soda. The process is now succesfully practiced in several parts 
 of Western Canada. The acid and alkali required for this purpose are 
 imported from Great Britain. 
 
 Asphalt. The solid bitumens, or asphalts, are sometimes distilled for the preparation 
 of oils, and are also extensively employed in ' the manufacture of mastic 
 for paving. The half-dried bitumen of the gum-beds of .Enniskillen 
 (page 524) is well fitted for distillation ; but such a process would not 
 perhaps be profitable at the present price of petroleum. The limestones 
 from Kincardine and Manitoulin Island (page 522), which contains from 
 eight to twelve per cent, of mineral pitch or asphalt, may, if found in 
 sufficient quantities, be employed for the preparation of mastic. The 
 minerals used for this purpose are similar natural mixtures of solid bitu- 
 men with sandstone, or with limestone, the latter being preferred. The 
 proportion of bitumen in these is however seldom sufficient to give to 
 the mastic the cohesion required. A proper mixture for paving is one 
 containing about fifteen per cent, of bitumen ; and for this purpose the 
 
CHAP. XXI.] MINERAL RESIK. 791 
 
 pulverized asphaltic mineral is mixed, by the aid of heat, with a sufficient 
 quantity of solid bitumen obtained by the distillation of asphalt, or with an 
 artificial bituminous mixture capable of replacing it. In this way the 
 asphaltic limestones of Switzerland and of Italy, with the addition of 
 from three to five per cent, of a ductile bitumen, are employed for the 
 pavements of Paris. 
 
 The black mineral which has been described on page 525, as probably 
 a product of the alteration of bitumen, and which is met with in consid- 
 erable quantities among the rocks of the Quebec group, on the island of 
 Orleans, at Quebec and elsewhere, has been found to yield a fine black pig- 
 ment ; and when ground with oil, to serve the same purpose as ivory-black. 
 
 The presence of small portions of mineral coal in the Devonian sandstones 
 of Gaspe* has been mentioned on page 394. Some beds of these rocks contain 
 besides, a peculiar resinous matter, which forms the cementing material. It Fossil resiu. 
 appears on the fractured edges of the beds, as in the form of irregular 
 laminae, rarely an eighth of an inch in thickness, and generally much less. 
 It has a vitreous lustre, a conchoidal fracture, and is tough, with a hard- 
 ness nearly equal to calc-spar. Its color is deep reddish-brown, but it 
 gives a fawn-colored powder ; and when in thin plates or fragments, is 
 translucent, and has an orange-red color. This substance has neither taste 
 nor odor ; it is jnsoluble in alcohol, naphtha, or potash-ley, and is but 
 slightly attacked by nitric acid. It is scarcely fusible ; but at a high tem- 
 perature is decomposed, with a slight softening and swelling up ; giving off 
 abundance of inflammable vapors, and leaving a small quantity of brilliant 
 spongy coke. It has the characters of a fossil resin, somewhat like amber, 
 but in its characters approaches more nearly to what have been named 
 scleretinite, and middletonite. 
 
 The portions of sandstone impregnated with this resin, burn, when kin- 
 dled, with a brilliant flame, and much smoke ; and the residue, which con- 
 sists chiefly of silicious sand, has very little coherence. Partial analyses its analysis, 
 were made of four fragments of this rock, which were supposed together to 
 represent an average of the mass. The amount of volatile matter, of fixed 
 carbon or coke, and of the incombustible residue was as follows : 
 
 I. n. m. iv. 
 
 Volatile matters, 32-4 22-8 42-8 30-4 
 
 Carbon 8-9 8-1 7-4 8-9 
 
 Residue 58-7 69-1 49-8 60-7 
 
 100-0 100*0 100-0 100-0 
 
 The purest specimen is seen to yield the smallest amount of fixed carbon. 
 The excess of this in the others is due, in part, to the small portions of 
 mineral charcoal generally present among the layers of this resinous sand- 
 stone. This material could be made to furnish large quantities of illumi- 
 
792 GEOLOGY OF CANADA. [CHAP. XXI . 
 
 use for gas nating and lubricating oils by a process of distillation similar to that 
 kmg> applied to coal and to bituminous shales. In some experiments made 
 on a small scale to test its power of producing illuminating gas, it was 
 found that a few pounds of this material, which lost, by distillation, 26 '0 
 per cent, of its weight, yielded two and a quarter feet of gas of superior 
 illuminating power, to the pound. As this quantity of volatile matter 
 corresponds to about 33*0 per cent, of resin, it is evident that if obtained 
 in a state of greater purity, this material would become valuable as a 
 substitute for coal in gas-making. 
 
 The specimens which served for the preceding experiments were obtained 
 from a bed of from fourteen to fifteen inches thick, which was found near 
 Shaw's mill, on the north side of Gaspe* Basin, and was traced for a dis- 
 tance of about 200 feet before it became concealed by overlying sandstones. 
 
 York River. In numerous localities along the York River, for a distance of nearly thirty 
 miles, small interrupted beds of a similar nature are met with in the sand- 
 stones. Those observed have a thickness of from four to twelve inches, 
 and are sometimes a hundred feet in length. Some of them are composed 
 in great part of laminae of a brilliant brownish-black matter ; which, when 
 examined in thin fragments, show the same reddish translucency as the 
 resin just described, and are apparently similar to it in composition ; although 
 in some cases mingled with more coaly matter, and containing less ash. 
 A specimen from one of these beds on the York River gave of volatile mat- 
 ters 52-4, carbon 26-3, residue 21.3 ; = 100-00. The greater proportion 
 of volatile hydrocarbons which may be obtained from this would render it 
 still more valuable for distillation than the bed whose analysis has been 
 given above. These curious deposits are evidently worthy of further study 
 from an economic point of view. 
 
 VI. REFRACTORY MATERIALS. 
 
 . Those matters which are used in the construction of furnaces, or of 
 crucibles, or generally for purposes of withstanding heat, are technically 
 designated refractory substances. Under the head of Refractory Minerals 
 are here included plumbago, mica, soapstone or steatite, pyrallolite, pot- 
 stone, sandstone (in so far as it is used for furnaces), fire-clay, and 
 moulding sand. Besides the uses indicated in the present classification, 
 several of these materials have other economic applications, which will 
 also be pointed out. 
 
 PLUMBAGO. 
 
 Plumbago or graphite, which is also commonly known as black-lead, 
 receives several applications in the arts. The finer varieties which have 
 the color, texture, and purity required, are employed for the manufacture 
 
CHAP. XXL] PLUMBAGO. 793 
 
 of pencils, and command a very high price. Inferior qualities of black- Biack-iead. 
 lead, if free from earthy matters, are made use of as an application for pre- 
 venting friction in machinery ; and considerable quantities are employed 
 for imparting a lustre to iron, especially for stoves in domestic use. The 
 most important use of plumbago is, however, for the manufacture of 
 crucibles and for melting pots, which are very refractory, and are much 
 esteemed by metallurgists. Small furnaces for assay ers and chemists 
 are also constructed of plumbago. For these purposes it is ground to a 
 fine powder, and mixed with a portion of clay, which gives plasticity to the 
 mass, and allows it to be moulded. The plumbago for these uses is 
 obtained in Bavaria and other parts of Germany, and in Ceylon ; while the 
 finer varieties for pencils are in great part procured from Russia and from 
 Cumberland. This last owes its value rather to its peculiar state of aggrega- 
 tion than to its purity, since it often contains more foreign matter than 
 some of the crystalline Ceylon plumbago, of much less price. The black- Crucibles, 
 lead of Passau in Bavaria, which is extensively used in the manufacture of 
 crucibles, contains only from 35-0 to 42-0 per cent, of pure plumbago, the 
 residue being of the composition of clay ;. yet this is extensively used for the 
 manufacture of crucibles, which are highly esteemed. They are said to be 
 made by mixing two or three parts of the impure mineral with one part of 
 clay. The value of comparatively pure crystalline plumbago, like that of 
 Ceylon, or of Canada, which contains but a small proportion of earthy mat- 
 ters, is said to be about twenty pounds sterling the ton. Argillaceous 
 matters, although they reduce its value, are, as has been seen, not prejudi- 
 cial; but the presence of carbonate of lime is very objectionable, inasmuch 
 as the lime forms a fusible compound with the intermixed clay when the cru- 
 cibles are exposed to heat. The beautiful process of Brodie, by which 
 plumbago is freed from all impurities, and reduced to a state of minute 
 division, is applied to the finer varieties of this mineral, which are to be 
 fitted for the manufacture of pencils. 
 
 The principal facts connected with the occurrence of plumbago in Canada 
 are given on page 529. The black plumbaginous slates of the Eastern 
 Townships, belong in part to the base of the Quebec group, and in part to 
 the overlying Upper Silurian series. Neither of these has yet been found 
 to contain any available quantities of plumbago ; but it is not impossible 
 that workable deposits of the mineral may be met with in some parts of 
 their distribution. The plumbago of the Laurentian series furnishes the 
 mineral in a comparatively pure form ; sometimes however associated with 
 carbonate of lime. In addition to the facts already mentioned with regard 
 to its occurrence, the principal localities of plumbago may now be noticed. 
 On the north side of the Ottawa, several deposits are known ; all of 
 which probably belong to one of the limestone bands of that region. On 
 the tenth lot of the fifth range of Grenville there is a mine of plumbago, 
 
794 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 Grenviiie. which was many years since worked to a small extent. The rock, which 
 is here somewhat disturbed by an intersecting trap dyke, consists of a 
 white crystalline limestone, which, in the immediate vicinity of the plumbago, 
 contains a bed composed of pyroxene, tabular spar, feldspar, and quartz. 
 Large cleavable masses of sphene, with phlogopite, zircon, garnet, and ido- 
 crase, are also met with in this aggregate. With this the plumbago is 
 more or less mingled ; although the greater part of it occurs in two or three 
 strings or irregular beds, from which a small quantity was at one time taken, 
 and sent to the English market. About half a mile to the northward, a 
 deposit of plumbago, which is perhaps a continuation of the last, is met with. 
 Here also the mineral appeared to be divided into three layers, of which 
 the widest was eleven inches, and it was accompanied by a bed containing 
 pyroxene, tabular-spar, sphene, and zircon. Plumbago is also said to 
 occur on the thirteenth and fourteenth lots of the fourth range of Gren- 
 ville ; where the limestone band just noticed, is repeated on the other side 
 of a synclinal. Farther to the northeastward in the continuation of this 
 same band, good specimens of plumbago are found on the north half of the 
 second lot of the tenth range of Grenviiie ; and beyond this, on the fifth lot 
 of the fourth range of Chatham Gore, masses of it are found on the surface, 
 in the vicinity of the crystalline limestone. To the westward, in the Aug- 
 mentation of Grenviiie, this limestone band re-appears in another synclinal ; 
 and a bed of plumbago has been traced along it, at intervals, for a distance 
 of about three miles, running a little to the east of north. On the third 
 lot of the second range, where an opening was made, a thickness of ten 
 inches of pure foliated plumbago occurred ; but this was found to have a 
 lenticular form, and to be separated from other similar masses by portions 
 in which the plumbago was mingled with limestone. Farther northward 
 on the third lot of the sixth range, the bed of plumbago has a thickness of 
 three feet, but is somewhat impure from earthy matters. Specimens of 
 very pure plumbago, associated with quartz, have lately been found in the 
 seigniory of Petite Nation. A few miles to the westward is the township 
 
 Lochaber. of Lochaber, from the twenty-fourth lot of the seventh range of which, 
 very excellent plumbago has been obtained. The adjacent township of 
 Buckingham is also said to afibrd good specimens of the mineral. 
 
 To the south of the Ottawa, plumbago of a good quality has been dis- 
 
 Burgeee. covered by Dr. Wilson in the township of Burgess. It occurs disseminated 
 very generally through the Laurentian limestones in the rear of Kingston. 
 Near the outlet of Gold Lake, on the sixth lot of the ninth range of Lough- 
 borough, it forms a bed in the limestone, from three to eighteen inches in 
 width. The mineral is intermingled with vitreous translucent quartz, in 
 which portions of pure plumbago are sometimes imbedded. A small vein 
 of this mineral is also found on the west side of Mud Lake in the same 
 township. It is not more than an inch in breadth, and is described as 
 
CHAP. XXL] MICA. 795 
 
 cutting the strata of gneiss. On the eighteenth lot of the ninth range Bedford, 
 of Bedford, specimens of plumbago are met with in the crystalline lime- 
 stone ; and on Bird Lake, in the same township, the mineral is found 
 with quartz in the limestone, both on the north shore of the lake, and on 
 the south side of a small island which occurs near its eastern end. It is 
 probable that these limestones, which are so widely distributed throughout 
 the Laurentian series in Canada, will be found to yield, in many localities, 
 valuable deposits of plumbago. 
 
 On page 494 will be found a description and analyses of the magne- 
 sian mica, or phlogopite, which occurs in various localities associated with 
 the limestones and pyroxenes of the Laurentian series. It is frequently 
 found in large masses, which may be separated into thin transparent plates. 
 Mica in this form, as is well known, receives various applications in the its uses, 
 arts, being employed for the fronts of stoves, for lanterns, and for the 
 chimneys of lamps. As it is not liable to be broken by concussion, it is 
 also used instead of glass in the windows of ships of war ; and it has received 
 several other applications of less importance. That hitherto employed, at 
 least such as is obtained from Russia and from the United States, has been 
 chiefly the mica of granitic rocks, called muscovite ; which differs in chemi- 
 cal composition from the phlogopite. The two species however resemble 
 one another closely in physical characters, and may be used for the same 
 purposes. The value of mica depends upon the size, the transparency, and 
 the perfection of the plates. The ordinary price of cut and dressed sheets its price, 
 of the usual size, in New York, is said to be $1-50 the pound ; while their 
 present value in London is about seven shillings sterling. A quantity of 
 large and carefully selected sheets from the locality in North Burgess, to 
 be mentioned below, was sold last year hi Paris for the use of the French 
 navy, at $ 2-00 the pound. Several hundred-weights of large selected 
 crystals from the same locality, fit for splitting into thin plates, were also 
 sold hi London at two shillings sterling the pound ; while from fourpence 
 to sevenpence were given for inferior qualities. There is also a large 
 demand for smallar sizes of mica, and for the refuse portions from its 
 working. These, among other uses, are employed in making letters for 
 window-signs. Ten shillings a hundred-weight were lately offered in 
 London for fifteen or twenty tons of such material. These figures will 
 serve to give some notion of the values which may be expected for the 
 different qualities of mica. 
 
 Mica in masses sufficiently large for economic purposes, has been 
 observed in several localities in Grenville. One of these is on the ninth Grenviiie. 
 lot of the sixth range, from which small quantities have been extracted 
 and sent to market. A crystal from this place was so large as to furnish 
 
796 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 sheets measuring twenty-four by fourteen inches. Good mica has also 
 been found on the tenth lot of the fifth range, and on the first lot of the 
 tenth range of Grenville ; as well as farther to the westward in the Aug- 
 mentation of this township. On the seventeenth lot of the ninth range 
 Burgess. of North Burgess, large crystals of magnesian mica are found in abun- 
 dance in a bed of soft pyroxenic rock. The mica has been traced for 
 about 300 feet ; and considerable quantities have been extracted and sold, 
 as mentioned above, by Mr. Alex. Cowan. Some of the plates are twenty 
 inches square, or even larger. Mica also occurs on the sixteenth lot of 
 the above, range, and on the twenty-first lot of the fifth, as well as on the 
 first lot of the fourth range of South Burgess. It appears probable that 
 by further exploration in this region, and in Grenville, sufficient quantities 
 of mica could be obtained to supply a large demand. 
 
 SOAPSTONE. 
 
 Soapstone, or steatite, is a more or less pure compact talc, for descrip- 
 tions and analyses of which, the reader is referred to page 469. When 
 pure and compact, soapstone is much used as a refractory material for 
 lining furnaces, especially those destined for anthracite. From its softness, 
 it is readily cut with knives and saws into the required shape, and it is infus- 
 ible in any ordinary furnace heat. Slaty varieties, and such as contain 
 crystals of spar, or other foreign minerals, are however to be rejected ; 
 
 steatite. inasmuch as'they are liable to split and exfoliate by heat. Steatite is also 
 used in the construction of small portable furnaces, and of open stoves, 
 which are made of plates of it held together by iron rods and bands. 
 Culinary vessels are made of it ; and it has also been bored for water- 
 pipes, and used for the lining of cisterns for acid and alkaline liquids. 
 When very strongly heated, steatite loses the small portion of combined 
 water which it contains, and becomes much harder, and susceptible 
 
 its uses. of a polish. It may then be colored by various solutions ; and it has lately 
 been used in this manner for the manufacture of buttons, and of some other 
 small articles. Jets for gas-burners are also made of this hardened stea- 
 tite, and have the advantage of not being liable to rust or corrosion. 
 When reduced to powder, the softness and unctuosity of steatite have 
 caused it to be used, like plumbago, as a lubricator to diminish friction ; 
 and the finely ground mineral is also said to be used to give a surface to 
 some kinds of paper-hangings. Its use as a cheap paint has already been 
 alluded to (page 767) ; and it may here be mentioned, that the Venetian 
 chalk which enters into certain cosmetics, and which is also used for 
 tailors' crayons, is steatite. 
 
 Steatite is rare among the Laurentian rocks, where its place is generally 
 supplied by pyrallolite, presently to be noticed. The only deposit of stea- 
 
CHAP. XXI.] SOAPSTONE. 797 
 
 
 
 tite yet known in this series is in Elzivir, and it is impure from an admixture 
 of carbonates. In the altered rocks of the Quebec group, however, it is 
 characteristic of the magnesian band in the second and third synclinals (page 
 710). A bed of steatite, associated with dolomite, occurs on the twelfth lot of 
 the seventh range of Sutton. It is however mixed with crystals of sutton. 
 bitter-spar, pyrites, and small octahedrons of chromic iron. It is enclosed 
 in micaceous slates ; and has adjoining it on the southeast side, a bed of 
 magnesite, described on page 457. A similar impure soapstone occurs 
 near the dolomite in the vicinity of Knowltonville. In many parts through- 
 out the distribution of this magnesian band of rock, steatite is associated 
 with serpentine, dolomite, magnesite, or chlorite ; one of these rocks often 
 appearing to take the place of the other, as noticed on page 248. Thus 
 on the fourth lot of the fourth range of Bolton, the belt of magnesian Boiton. 
 rocks is represented by a breadth of about twenty-five yards of steatite 
 holding bitter-spar and intermingled with patches of dolomite ; while 
 about 300 yards to the northeastward, on the strike, it passes into a bed 
 of dark green slaty serpentine, containing asbestus, with grains of chromic 
 and magnetic iron. This is bounded on the northwest by a bed of stea- 
 tite ; and beyond this is a bed of actinolite, mingled with asbestus and talc ; 
 the whole occupying a breadth of fifty yards. On the sixth lot of the 
 second range of Bolton, is a band of soapstone, which occupies a breadth 
 of about thirty yards, and is limited on the southeast side by a bed of 
 dark green serpentine a foot in thickness, to which succeed nacreous clay 
 slates. The steatite is more or less mixed with crystals of bitter-spar, 
 which to the northwest side predominate ; so that the rock passes into a 
 dolomite, which is bounded by slates similar to those on the opposite 
 side of the band. 
 
 Along the western side of the Missisquoi valley, the western outcrop of 
 a portion of the second synclinal is traced for 'a distance of about twenty 
 miles, through Potton and Bolton ; and is marked by the band of magne- 
 sian rocks already noticed ; which in many places present beds of soapstone, 
 sometimes, but not always, associated with serpentine. On the twentieth 
 lot of the fifth range of Potton, a workable bed of it, three feet in thick- Potton. 
 ness, is met with ; and a locality which furnishes a steatite of superior 
 quality, is on the twenty-fourth lot of the sixth range of Bolton. Here it 
 is associated with chlorite, and with dolomite. Resting upon a band of the 
 latter, is a layer of about three feet of impure steatite, overlaid by four 
 feet of dolomite. This is followed by a layer of a few feet of chlorite ; to 
 which succeed about five feet of steatite ; the upper two feet of which are 
 very pure and compact, and furnish large blocks free from flaws. The 
 bed of steatite however appears here, as in some other places, to have a 
 lenticular shape, thinning out, and being replaced by the chloritic rock. 
 
 On the eastern side of the Missisquoi River the same band of magnesian 
 
798 GEOLOGY OF CANADA. [CaAp. XXL 
 
 strata appears along the western margin of the third synclinal, whose out- 
 crop has already been described in connection with the copper ores which 
 accompany it. Here, as might be expected, on the opposite' side of the 
 anticlinal, the apparent position of the steatite to the great mass of the 
 dolomite is reversed, and it appears to the east of it. A bed of steatite 
 occurs on the seventeenth lot of the ninth range of Bolton, and forms one 
 limit to the bed of magnesite described on page 458, which is bounded on 
 the other side by serpentine. There is little doubt that workable beds of 
 steatite like that of Potton, will be found in many localities in the magne- 
 sian band along the outcrops of the. various synclinals. Steatite is met 
 with farther to the northeastward, in the valley of the Chaudilre, at the 
 fall of the Bras in Vaudreuil. Here a bed of it occurs, associated with 
 dolomite, in argillite. The steatite of this locality contains imbedded 
 crystals of carbonate of magnesia, and is stained green by nickel, traces 
 of which generally accompany the steatites of this series. 
 
 PYKALLOLITE, 
 
 As already remarked, true steatite is of rare occurrence in the Lauren- 
 tian rocks in Canada, and also in northern New York ; but its place is 
 often supplied by a mineral which is similar to it in chemical composition, 
 softness, and refractory properties, and was by Prof. Emmons of New 
 York called renssellaerite. This, as will be seen on page 470, is regarded 
 as identical with what had previously been named pyrallolite. According 
 to Emmons, this mineral is capable of being turned in a lathe, and wrought 
 like soapstone, and has been made into small vases, inkstands, and similar 
 objects. Some varieties of it are nearly white, and have the translucency 
 of porcelain ; others are greenish, and others nearly black. Much of the 
 figure-stone or pagodite, in which the Chinese carve various ornaments, 
 appears to be pyrallolite. It was also used by the aborigines for their 
 calumets. One of these, found in an Indian tomb on Lake Huron, was 
 found to be carved from a nearly white translucent pyrallolite. 
 
 This mineral appears to form beds, associated with the Laurentian lime- 
 stones, and has been observed in several places. A bed of it, associ- 
 ated with serpentine, occurs between the gneiss and the limestone, on the 
 
 Grenviiie. thirteenth lot of the fifth range of Grenville. It may be traced thence into 
 the sixth range, and appears to be in considerable quantity. , Another bed 
 of it is found between quartz and crystalline limestone, on the east side 
 
 Kamsay. O f the eighth lot of the sixth range of Ramsay, and would furnish con- 
 siderable masses of the material. Other localities of pyrallolite have been 
 mentioned on page 470 ; and it is probable that it will be found in 
 many places accompanying the Laurentian limestones. In the Saguenay 
 region, at the lowest rapid of the Peribonka River, a thin band of a 
 
CHAP. XXI.] SANDSTONE AND SAND. 799 
 
 soft greenish rock, which resembles pyrallolite, is interstratified with a 
 great mass of coarsely crystalline violet-blue labradorite ; which has here 
 a breadth, across the strike, of about six hundred feet. 
 
 POTSTONE. 
 
 Potstone, or compact chlorite, receives its name from the fact that it 
 was formerly used in some parts of Europe for the construction of culinary 
 vessels. From its softness, it may be cut and turned like steatite, with 
 which it is often confounded. Among the chloritic rocks which abound in chlorite. 
 Eastern Canada, beds of pure compact chlorite are sometimes met with. 
 One of these, on the twenty-sixth lot of the second range of Bolton, has Boiton. 
 a breadth of about twenty feet, and affords large blocks, from which plates 
 measuring several square feet have been cut by a common mill-saw. A 
 description and analysis of this rock will be found on page 607. It will 
 probably prove a less refractory material than steatite, and has less of the 
 unctuosity which characterizes this mineral, but may be applied to many 
 of the same uses. A bed of pure compact potstone occurs on the fourth 
 lot of the twelfth range of Broughton. 
 
 In this connection may be mentioned a soft micaceous rock which occurs 
 on the eighteenth lot of the fifth range of Shipton. The description and 
 analysis of this rock are given on page 494. In its softness and texture, 
 it so closely resembles potstone as to have been mistaken for it, and it may 
 probably be employed for similar uses. The portion of the bed exposed 
 has a breadth of five feet, but its whole thickness is probably much greater. 
 
 SANDSTONE AND SAND. 
 
 These materials are much used for the construction of the furnaces used 
 in smelting metals, and in other metallurgical operations. The nearly 
 pure silicious sandstone of the Potsdam formation is in some places well 
 suited for such purposes. That from the Grs Rapids on the St. Maurice was 
 used in the ironworks of that vicinity, and of Batiscan ; and is employed at 
 the Radnor furnaces. The blocks of stone have a thickness of from twelve Fire-stone, 
 to eighteen inches, a breadth of twenty inches, and a length of four feet. 
 They are found to answer an excellent purpose, and do not require renewal 
 oftener than once in two years. The rock here is of a freer texture than in 
 many other parts of its distribution. It is probable that sandstones equally 
 well adapted for this purpose may be found in many other places along 
 the extended outcrop of the Potsdam formation, which has been described 
 in the sixth chapter. On the twentieth lot of the first range of Pittsburg, 
 there is- an exposure of a thickness of twenty feet of this sandstone, which 
 is extremely friable, and readily reduced to powder. In this state it is 
 
800 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 Moulding- 
 sand. 
 
 Laval. 
 
 Fire-brick. 
 
 Glass- 
 making. 
 
 sought for by iron workers, who employ it to protect the sides and bottom 
 of their furnaces. About 1500 tons of it are annually supplied to the 
 two cities of Montreal and Toronto. The material is delivered in Mont- 
 real for about three dollars a ton. 
 
 The moulding sand employed by iron founders is a fine quartzose sand, 
 containing at the same time small quantities of argillaceous and ferrugi- 
 nous matters. Sands of this composition, possessing the required texture, 
 are known to exist in several localities in the country. Thus the moulding 
 sands employed at St. Maurice and at Batiscan are found in the vicinity. 
 At Perth, at Brockville, and at Kingston sands fitted for this purpose are 
 also met with; and in the neighborhoods of Dundas, Durham, and Owen 
 Sound are beds of fine sand, which have been successfully employed by 
 iron founders. It is probable that similar materials may be met with in a 
 great many localities. 
 
 Artificial mixtures for the moulder's use are often made, especially by 
 the German founders, and for fine castings. For this purpose, sandstones 
 and argillaceous rocks are carefully ground to powder and sifted. A good 
 mixture is also said to be obtained with two parts of iron ochre, three parts 
 of clay, and ninety-three parts of fine quartzose sand. A deposit of such 
 sand, twenty feet or more in thickness, occurs at Laval, on the right bank 
 of the Bras, at its junction with the Montmorenci River. This material, 
 from its exceeding fineness, has been employed at Quebec as a polishing 
 powder, and might probably be used for the preparation of a moulding 
 sand. A nearly pure silicious sand is employed in England for the manu- 
 facture of the celebrated Dinas fire-brick. This material, which contains 
 from 96*0 to 98-0 per cent, of silica, constitutes the under-clay of a coal 
 bed, in the vale of Neath in Glamorganshire. It is mixed with about 
 one hundredth of lime, and sufficient water to make the mass coherent. 
 The paste is then compressed in iron moulds, dried, and burned for 
 several days, at a high heat. These bricks are very refractory ; and 
 as they expand by heat, instead of contracting like those of fire-clay j 
 they are greatly preferred in the construction of many parts of furnaces. 
 (Percy's Metallurgy, vol. i, p. 237.) It is probable that some of the 
 silicious sands of this country might be advantageously used for the manu- 
 facture of similar fire-bricks. 
 
 The white silicious sandstone of the Potsdam formation affords in many 
 places a material sufficiently pure for the manufacture of glass. Furnaces' 
 for this purpose were formerly in operation at St. Johns, and at Vaudreuil 
 on the Ottawa ; but have been abandoned from the difficulty of competing 
 successfully with glass of foreign manufacture. Beds of sandstone weE 
 fitted for this purpose are found on Isle Perrot, in Vaudreuil, and at 
 Lachute and Ste. Scholastique. The same formation in many parts of Beau- 
 harnois furnishes a sandstone which from its freedom from iron, would 
 
CSAP. XXI.] BRICK-CLAY. 801 
 
 furnish a good material for the purpose. One of the best localities of the 
 stone in this seigniory is at Williamstown, Large quantities of fine white 
 sand from the disintegration of a sandstone of this formation, are found on 
 an island in Charleston Lake in Escott. 
 
 VII. MATERIALS FOR BRICKS, POTTERY, AND GLASS. 
 
 Under this head may be noticed the clays for the manufacture of com- 
 mon bricks, tiles, and coarse earthenware. No clays fit for the finer 
 kinds of pottery have as yet been found in the country. In Vermont 
 however, at the western base of the Green Mountains, valuable beds of 
 kaolin or porcelain clay, belonging to a tertiary formation, are met with in Kaolin, 
 several localities. It is not improbable that these deposits may be continued 
 into Eastern Canada ; but if such be the case, they are concealed by the 
 superficial clays and sands of the region, and have yet to be sought for along 
 the base of the Notre Dame Mountains. Feldspar, which enters into the 
 composition of porcelain, is found in considerable quantities in granitic veins 
 among the Laurentian rocks, and may in some places occur in sufficient 
 purity to be available for the use of potters. In describing the phosphate 
 of lime of this series of rocks, allusion has been made to the fact that this 
 material, in the form of calcined bones, enters largely into the composition 
 of English porcelain, and that the purity of some of the apatite of Canada 
 is such that it may perhaps be employed for a similar purpose. The 
 fitness of some of the Potsdam sandstone for the manufacture of glass, has 
 been mentioned above. The specimens of this stone from Vaudreuil, at 
 the Exhibition of 1851, attracted the attention of English glass manufac- 
 turers, who import a similar material from the United States, and who 
 afterwards made inquiries as to the price at which the sandstone could be 
 furnished in England. 
 
 BRICK-CLAY. 
 
 Clays suited for the manufacture of bricks are found in a vast number 
 of places throughout the province. In Western Canada, the clays are 
 divided into two classes. The older and underlying deposit is compara- Brick-clay, 
 tively free from oxyd of iron, and yields white bricks, which generally 
 however have a somewhat yellowish tinge. The white-brick clay is uncon- 
 formably overlaid by another deposit, which gives red bricks. The history 
 of these two clays will be given in detail in the succeeding chapter. These 
 white bricks, which are more esteemed than the red, are made in a great White 
 many localities from the shore of Lake Huron as far eastward as Brock- bricks * 
 ville. The average number of bricks made annually in Toronto is from 
 eight to ten millions, of which from three to five millions are white bricks. 
 The ordinary price of these at the kiln is from $5-50 to $6-00 the 
 
802 GEOLOGY OF CANADA. [CHAP. XXK 
 
 thousand ; while that of the red bricks is from $3-00 to $4-00. Besides the 
 superficial clays of Western Canada, the soft argillaceous beds of the Medina 
 formation, and of the Hudson River group, are successfully employed for 
 
 Dundas. the manufacture of bricks. At Dundas there is an argillaceous band 
 about twenty feet in thickness, near the base of the Clinton formation. 
 This rock readily disintegrates, and, being washed down by the rains, is 
 deposited from the water in the form of a clay, which is collected and used 
 in the iron foundries of Dundas and Hamilton. It is said that this is of a 
 
 Fire-clay, refractory nature, and serves as a fire-clay. Many of the best mate- 
 rials of this kind are furnished by the under-clays of the coal formation 
 (page 572); and it is not improbable that beds of a similar kind, which 
 have been mentioned on page 395 as occurring in the Gaspe* series, may 
 be found to yield a fire-clay. 
 
 In Eastern Canada, the two kinds of clay which are distinguished in the 
 west are no longer met with ; but an extensive deposit of marine clay extends 
 throughout the valleys of the Ottawa and St. Lawrence, and furnishes 
 every where -material for bricks. The two principal manufacturers at Mont- 
 real produce each about six millions of bricks annually. The ordinary 
 price of these is about $5'00 the thousand. Some beds of these clays 
 
 Pottery. are employed for the manufacture of coarse earthenware ; which is manu- 
 factured, among other places, at Beauharnois, at Yamachiche, at Yamaska, 
 and near Quebec. Drain tiles for agricultural purposes, are also made 
 at several places, as at Montreal, at Treadwell upon the Ottawa, and at 
 Missisquoi Bay. Pipes for sewerage draining are manufactured on a 
 considerable scale at Quebec, where upwards of 150,000 feet of them 
 have been laid for main sewers and for house-drains. They are covered 
 with a lead glaze ; and have a considerable strength, resisting, it is said, 
 a pressure of fifty pounds to the square inch. 
 
 VIII. MATERIALS FOR CEMENTS AND MORTARS. 
 
 Under this head may be included, first, limestones which yield lime for 
 ordinary mortar, and secondly, limestones fit for water-lime or hydraulic 
 cements. To these may be added gypsum or plaster of Paris, which has 
 Magneeite. already been noticed on page 762, and also magnesite. Magnesia, which 
 may be obtained by the calcination of this mineral, has been recom- 
 mended for the preparation of a hydraulic cement especially adapted for 
 constructions which are to be exposed to the action of sea-water. The 
 localities of magnesite, and some details with regard to the preparation 
 of the cement, have been given on page 756. 
 
CHAP. XXL] LIMESTONES. 803 
 
 LIMESTOKE8. 
 
 The Lower Silurian limestones of the Chazy formation and of the Trenton 
 group, afford throughout their distribution, abundant material for the 
 manufacture of lime, and they are extensively burned in the vicinity of 
 Kingston, Ottawa, St. Hyacinth, Montreal, and Quebec. Analyses of 
 some of these limestones are given on page 621. They sometimes contain 
 an admixture of small quantities of argillaceous matter ; but from their 
 general purity, and from their freedom from iron and magnesia, they yield 
 a white lime well adapted for making fine mortar, for whitening walls, for Lime 
 agricultural purposes, and for the purification of coal-gas. The amount 
 of lime annually burned at Montreal is about 270,000 bushels, and its 
 price is about seventeen cents the bushel. The limestone of the Birdseye 
 division of the Trenton group, which is burned at St. Anne near Montreal, 
 yields a lime which is much esteemed. That from Ste. Rosalie, near St. 
 Hyacinth, whose analysis has been referred to, yields a lime remarkable 
 for its purity and whiteness. The stone cannot be distinguished from that 
 which is burned at Highgate in Vermont, and which belongs to the same 
 formation. The quarries in both localities contain interstratified beds of an 
 inferior magnesian limestone. The Devonian limestones of the Corniferous 
 formation, which underlies a great portion of southwestern Canada, resemble 
 in composition those just mentioned, and yield a similar pure lime. 
 
 The Middle and Upper Silurian limestones of Western Canada, including 
 the Niagara, Guelph, and Onondaga formations, are generally magnesian, 
 and have the composition of dolomite (page 624). When burned, they 
 yield a meagre or magnesian lime, which is for the most part very free :,ra g nesian 
 from impurities. These magnesian limes yield very strong mortar, but are ime- 
 considered to be less proper for agricultural purposes than those which 
 contain no magnesia. The Calciferous formation, which underlies the 
 Chazy in some parts of Canada, yields in like manner a magnesian lime, 
 and the same is true of many of the limestones of the Quebec group. Quebec 
 These often contain a considerable quantity of carbonate of iron, which group> 
 gives a yellowish or ochrey tint to the lime. For analyses of them, see 
 page 613. Pure limestones are however sometimes associated with these 
 dolomites, as at Point Le*vis. Throughout the Quebec group, a band of 
 limestone, for the most part magnesian, is generally the accompaniment of 
 the copper ores, in describing which many of its localities have been indi- 
 cated. The distribution of this limestone band in a district where silicious 
 rocks prevail, assumes a considerable economic importance. To the south- 
 east of the Quebec group, the upper slates (page 709) are associated with 
 good limestones, which are sometimes more or less magnesian, and are 
 quarried and burned on Lake Memphramagog, at Dudswell, and on the 
 Famine River. 
 
804 GEOLOGY OF CANADA. [CHAP. XXL 
 
 Limestones occur among the Upper Copper-bearing rocks of Lake 
 Superior, and also in the Huronian series. The distribution of these latter 
 limestones is given in the fourth chapter, and on the map which accompa- 
 nies it ; and analyses of some of them will be found on page 596. The 
 
 Laurentian luuestones of the Laurentian series are very important, both from their 
 extent, and from the fact that wherever they occur, the Laurentian region 
 presents fertile valleys fit for cultivation ; so that the principal settlements 
 found among these rocks are upon the outcrop of the limestone bands. 
 These limestones, which afford excellent lime, as well as good marbles and 
 building materials, are sometimes pure, and sometimes magnesian. Descrip- 
 tions and analyses of some of these are given on page 592 ; and their 
 distribution is explained in the second chapter, and in the map, which repre- 
 sents their arrangement in a part of the Ottawa district. About three 
 miles below Tadpusac, on the St. Lawrence, and a little to the east of the 
 mouth of the Riviere Baude, the Laurentian gneiss is cut by a perpen- 
 dicular vein of calc-spar, which runs northwestward, and has a breadth of 
 twelve feet. This spar, which is coarsely crystalline, contains only scat- 
 tered grains of copper pyrites ; and if burned, would yield a good lime, 
 which, in this locality, remote from any other known deposit of limestone, 
 is of some importance. Mention has already been made of the fresh-water 
 
 Marl and marls as suitable for the manufacture of lime ; and the considerable deposits 
 of calcareous tufa, which is a nearly pure carbonate of lime, and abounds 
 in many parts of Western Canada, may in some cases be applied to a 
 similar purpose. As this material contains no carbonate of magnesia, it 
 will furnish a lime better fitted for agricultural purposes than the dolo- 
 mites of the region, which yield a magnesian lime, generally regarded as 
 injurious to the soil. Deposits of calcareous tufa occur in many places 
 along the base of the Niagara formation in the counties of Grey and 
 Simcoe. The most considerable known is on the banks of the Beaver 
 River, in Euphrasia and Artemisia, which probably covers 1000 acres. 
 An area of about 300 acres of tufa, with an average thickness of five 
 feet, occurs in a similar geological position at the falls of the Noisy 
 River in Nottawasaga. 
 
 HYDRAULIC CEMEOT8. 
 
 Certain impure limestones yield by calcination, a substance which, 
 instead of slaking with water, like ordinary lime, forms with it a paste, 
 which after a greater or less lapse of time sets or becomes hard even 
 under water. This property is now known to depend upon an admixture 
 of clay or silicate of alumina, containing an alkali; and artificial mixtures 
 are prepared by mingling chalk, or any other carbonate of lime, with 
 a proper quantity of clay, and calcining the mixture. In this way the so- 
 called Portland cement, and many other similar compositions are prepared, 
 
CHAP. XXL] HYDRAULIC CEMENTS. 805 
 
 both in England and in France. The pozzuolana of the Italians, and the 
 trass of the Germans, are argillaceous materials of volcanic origin, which 
 when mingled with pure lime, yield hydraulic cements; and these 
 substances may also be imitated by calcining ordinary clays, and then 
 grinding them to powder. Where however natural admixtures of clay 
 and carbonate of lime can be obtained in abundance, it is more advanta- 
 geous to employ them than to resort to artificial preparations. When a water-lime, 
 limestone contains ten or fifteen per cent, of clay, it yields a lime possess- 
 ing hydraulic properties, which increase with the proportion of clay ; and 
 when this amounts to one third of the lime, the mixture yields a mortar 
 which hardens almost immediately under water. The proportion of clay 
 may even rise to sixty per cent, without destroying this property. Mag- 
 nesian limes yield hydraulic cements equally good with those of pure lime, 
 and, as already noticed, a mixture of magnesia with pozzuolana or with 
 calcined clay forms a valuable water-cement. 
 
 Argillaceous limestones and dolomites yielding good hydraulic cements, 
 are known in many parts of Canada, and have been employed to some 
 extent. In the following descriptions, advantage will be taken of the 
 analyses of some of the cements of Canada, made in 1855, by Mr. Delesse, 
 one of the jurors at the International Exhibition at Paris, and published 
 in the report of the Imperial Commission. In the Quebec group, a black 
 thin bedded dolomite, noticed on page 268, occurs at the Mountain Port- 
 age, about five miles from the mouth of the Magdalen River in Gaspe*. Gasps. 
 By its analyses, given on page 614, it is seen to contain about twenty-five 
 per cent, of clay. When calcined, it becomes of a buff color, and yields a 
 cement which hardens under water after five minutes, and soon acquires a 
 great degree of solidity. Beds of a similar rock occur at the Grande 
 Coude, six miles bejow Great Pond River ; and other beds may probably 
 be found in many parts of this region. 
 
 The black limestone of Quebec, which is employed for the manufacture Quebec, 
 of a hydraulic cement, differs from that just described in the absence of 
 magnesia. This stone, whose hydraulic properties were first noticed by 
 General Baddeley, R.E., contains a large proportion of clay, and is colored 
 by a carbonaceous matter, which disappears by calcination, when the rock 
 becomes of a yellowish color. A specimen of the calcined and ground 
 stone, prepared for use by Mr. Gauvreau of Quebec, gave 11-6 per cent, 
 of water and carbonic acid, and the residue consisted of lime 52-49, mag- 
 nesia traces, silica 27'40, alumina and oxyd of iron 12*16, sulphate of 
 lime 7-95 ; = 100.00. The proportion of sulphate of lime in this cement 
 is remarkable ; but it remains to be determined whether it belongs to the 
 rock, or is added in preparing the cement. It becomes solid, according to 
 Delesse, in twenty-five minutes after mixing with water ; but is of a quality 
 inferior to the Thorold cement. 
 
806 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 In the Chazy formation, a bed of grey argillaceous magnesian limestone 
 occurs a few feet above a Blackish-brown band, which is marked by the 
 shells of Leper ditia (page 128). This magnesian layer, which weathers 
 of a yellowish color, has a conchoidal fracture, and holds small geodes of 
 calc-spar, may be traced by its mineral characters, and by the underlying 
 fossiliferous bed, from Hawkesbury as far westward as Allumette Island. 
 
 Nepean. At Nepean, on the shore of the Ottawa, it has a thickness of six feet, and 
 has for many years been quarried for the manufacture of a hydraulic 
 cement. The analysis of the stone from this place is given on page 619. 
 A specimen of the cement gave to Delesse, lime 39' 70, magnesia 9*58 7 
 soluble alumina and oxyd of iron 19' 74, insoluble argillaceous residue, 
 30-98 ; = 100.00. It is probable that this bed may yield a similar cement 
 in other parts of its distribution. Beds of limestone from the Calciferous 
 formation in Hawkesbury, Argenteuil, and Chatham are said to have been 
 tried on a small scale, and to yield a cement. In the township of Lough- 
 borough, on the first lot of the eighteenth range, are beds which resemble 
 those of the Chazy just described, and have been found to yield a hydrau- 
 lic lime. A similar bed, three feet in thickness, occurs in the ditch around 
 
 Kingston, the fort at Kingston, and has been used as a cement. There is little 
 
 doubt that when a larger demand for such materials exists, many localities 
 
 of water-lime may be found, both in the Calciferous and Chazy formations. 
 
 In the Niagara formation near Thorold, a band of dark grey argillaceous 
 
 Thoroid. limestone, eight feet in thickness, (page 323,) yields an excellent cement. 
 Its color after calcination is yellow. A specimen examined by Delesse 
 contained 3' 37 per cent, of moisture, without any carbonic acid. Its far- 
 ther analysis gave lime 53-55, magnesia 2-20, silica 29-88, alumina and 
 oxyd of iron 12-70, sulphate of lime 1-58 ; = 99-91. This cement was 
 found to set in ten to fifteen minutes, with disengagement of heat. A por- 
 tion placed in water ten minutes after mixing, became as solid as another 
 portion which had set in the air, and was only immersed at the end of two 
 hours. The resistance of this cement to traction, according to Delesse, 
 was represented by 85, while that of Quebec was 49. This cement has 
 been largely used in the construction of many public works, and was em- 
 ployed in building the piers of the Victoria Bridge. Its price at St. 
 Catherines is from twenty to twenty-five cents the bushel. This layer of 
 water-lime does not appear to be continuous throughout the Niagara for- 
 mation. At Limehouse, in Esquesing, there is a band of nine feet, which 
 is wrought to a considerable extent, and yields a good hydraulic lime. At 
 Rockwood also, a band of limestone three and a half feet thick, associated 
 with a layer of chert, is said to yield a water-lime. The last two localities 
 are in the Niagara formation, but are not supposed to be the equivalents 
 of the Thorold stone. 
 In describing the Onondaga formation in the thirteenth chapter, it has 
 
CHAP. XXL] MILLSTONES. 807 
 
 been stated that many of the beds of argillaceous dolomite which are asso- 
 ciated with the gypsum, yield a hydraulic cement ; for which purpose they 
 are largely used in the state of New York. Analyses of this dolomite 
 from Oneida, and from Paris, are given on page 625. The calcined rock Oneida. 
 from the first locality gave to Delesse, lime 36 93, magnesia 26 * 74, clay 
 36 33 ; = 100 00. It heats very slightly when mixed with water, and 
 yields a cement of good quality. The calcined material from Paris con- 
 tained lime 53*82, magnesia 35*93, clay 10*25. A specimen from this 
 formation, on the fourteenth lot of the second range of Brantford, yielded 
 a cement which hardened under water in the course of five minutes. 
 Similar beds are found at Point Douglas on Lake Huron ; and it is prob- 
 able that materials fit for the manufacture of water-cement may be found 
 almost everywhere along the outcrop of the Onondaga formation. 
 
 IX. GRINDING AND POLISHING MATERIALS. 
 
 Under this head will be noticed materials for two very different uses ; 
 first, those employed in the construction of millstones for grinding grain ; 
 and second, those which are used for grinding, sharpening, cutting, and 
 polishing metals and stones. Besides the various grindstones and whet- 
 stones, mention may also be made of garnet-rock, which from its hardness 
 is sometimes used as a substitute for emery. Small beds of granular red Garnet, 
 garnet occur with the quartzites to the west of the crystalline limestone at 
 St. Jerome, forming a band of four or five feet, which is divided by thin 
 layers of quartz and of feldspar. Some of the beds consist of grains of 
 hyacinth-red garnet, with small crystals of yellowish pyroxene ; besides 
 occasional grains of white-weathering greenish feldspar, scales of plum- 
 bago, and more rarely black grains, apparently of tourmaline ; the garnet 
 however greatly predominating. Strata of garnetnrock occur in similar 
 conditions near the crystalline limestone in Rawdon, and also at the north- 
 east side of Bay St. Paul, where beds, which run nearly east and west, are 
 made up of red garnet with a little white quartz, and are interstratified 
 with layers of micaceous schist. The whole band occupies a breadth of 
 about sixty feet, of which the garnet-rock constitutes about one third. 
 
 HILLSTONES. 
 
 The French buhrstone, which is preferred to all other materials for the 
 construction of mills for grinding grain, is a peculiar chert-like silicious 
 rock, having a porous or cellular texture, which renders its surface 
 especially adapted for the purpose. Similar silicious rocks are found to 
 some extent in several other parts of the world, and generally form beds 
 in stratified rocks. In the Laurentian series in Canada however, a cellular 
 
808 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 chert. 
 
 Gneiss. 
 
 Millstones, chert of this kind occurs in large veins, apparently of aqueous origin, 
 cutting the intrusive syenite of Grenville, and has been described on 
 page 41. One of these veins appears on the first lot of the sixth range 
 of Grenville, running east and west. Another vein, parallel to it, has been 
 traced across the southern part of the lot just mentioned, to the front of 
 the second lot of the same range, and to the third of the fifth range. Its 
 breadth is from four to seven feet, and it includes in some parts masses of 
 the wall-rock. It is white, often banded with yellowish or reddish colors, 
 which are parallel with the sides of the vein. The chert, which much 
 resembles the French buhrstone in its characters, has been pronounced to be 
 equally well fitted for the manufacture of millstones. The portions at the 
 surface are however injured by the weather ; and the difficulties of quar- 
 rying the material from a vein in the hard syenite are such, that it would 
 probably prove more expensive than the imported buhrstone. 
 
 In various parts of the country, millstones, inferior to the French stones, 
 but answering a very good purpose, are made from different hard silicious 
 rocks. Along the north shore of the Ottawa, the reddish coarse grained 
 Laurentian gneiss is often had recourse to ; and the large boulders, which 
 are abundant upon the surface, are found more convenient for working 
 than the rock in its original beds ; inasmuch as they require only to be split 
 and dressed. At the Crooked Falls, on the Riviere des Aulnais, in the 
 Saguenay district, a rock made up of red orthoclase and brown mica, has 
 been successfully employed for millstones ; and it appears probable that 
 some of the crystalline lime-feldspar or labradorite rocks, which are so 
 abundant in the Laurentian series, and are found in rolled masses along 
 the valley of the St. Lawrence, might be used with advantage for the 
 same purpose. 
 
 Many of the tough feldspathic rocks, and the quartzose conglomerates of 
 the Eastern Townships, would doubtless make good millstones. A granitoid 
 gneiss, which is found near the serpentine in St. Joseph on the Chaudire, 
 furnishes a material of which millstones are made, that .have been used in 
 the vicinity for years, and pronounced to be of an excellent quality. The 
 Potsdam formation in many places contains conglomerate beds adapted for 
 
 sandstone, millstones. In the parish of St. Cuthbert, a band of about eight feet, in 
 beds of from one to two feet hi thickness, has been used for this purpose, 
 and found to answer well for grinding wheat. Similar conglomerates occur 
 in this formation in the seigniory of Vaudreuil, both at the Cascades and 
 the Pointe du Grand Detroit. From one of the layers at the latter place, 
 millstones have been made ; and it is probable that material suited for the 
 purpose may be found in many other places along the outcrop of the 
 Potsdam formation. Near White Cape at Murray Bay, good millstones 
 have been made from beds of quartzose conglomerate, which there occur in 
 the Trenton formation. The Oriskany sandstone from Oneida and Cayuga, 
 
CHAP. XXL] GRINDSTONES AND WHETSTONES. 809 
 
 described on page 360, is in some parts well fitted for a similar purpose ; 
 and good millstones for grinding oats and barley are manufactured from it 
 at De Cewville in Cayuga. 
 
 GKINDSTONES AND WHETSTONES. 
 
 A sandstone well adapted for grindstones is found at Nottawasaga, in Grindstones, 
 what is called the Grey band of the Clinton formation, and is here twenty 
 feet in thickness. The stones, roughly hewn by hand, are sold in the 
 vicinity at the same price as those imported from Ohio. This band is 
 traceable along the outcrop of the formation for a great distance (page 316), 
 and has been employed in many other places for grindstones. Coarse Whetstones, 
 whetstones for scythes are also made of it ; and a stone for the same pur- 
 pose is obtained in Collingwood from the fine grained sandstones of the 
 Hudson River formation. Sandstone beds belonging to the Chazy forma- 
 tion, which yield stones for sharpening axes and carpenters' tools, occur 
 at several places on the Ottawa. Among these are Whetstone Point on 
 the ChaudiSre Lake, Sheriff's Mills at the Chats, and the Allumette Falls, 
 Common whetstones were also at one time manufactured from the fine 
 grained micaceous schists of the Laurentian series, which are found on the 
 fourth and fifth lots of the sixth range of Madoc (page 32). A finer 
 stone, fitted for giving an edge to razors and delicate instruments, is 
 found in many places among the greenish silicious slates of the lower part 
 of the Huronian series (page 56). A locality of this kind occurs on 
 Ottertail Lake on the Thessalon River. 
 
 In the Eastern Townships, a band of very fine grained micaceous rock 
 has been traced from Whetstone Island in Memphramagog Lake, by Lee's Memphra- 
 Pond to the head of Massawippi Lake in Hatley, a distance of twelve magog * 
 miles ; and yields in many places whetstones which are well fitted for most 
 purposes. From a description published forty years since in the American 
 Journal of Science (vol. v., page 406), it would seem that the material 
 then obtained on Whetstone Island was so highly esteemed that a mill for 
 cutting the stones had been erected on the shore of the lake .; and that 
 large quantities were annually prepared for exportation. Among them 
 it is said were oil-stones equal to those of Turkey. Whetstones are 
 also obtained on the fourth lot of the ninth range of Stanstead, on the 
 twenty-third lot of the sixth range of Bolton, and on the seventh lot of the 
 second range of Kingsey, where they were manufactured a few years since, 
 There is a range of slates, fitted in some parts for this purpose, running 
 on each side of the valley from Melbourne to Danville. A hone-stone of 
 a very fine quality has been obtained from the slates near the serpentine, 
 on the ninth lot of the eighteenth range of Orford (Crown Land Survey), 
 
810 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 X. BUILDING STONES. 
 
 \ 
 
 Although Canada possesses in great abundance every kind of stone 
 required for the purposes both of common and decorative architecture, but 
 little has yet been done to bring these materials into notice. With the 
 exception of the common limestones, the building materials of Canada 
 have until recently been almost altogether neglected. It is proposed to 
 notice in succession the principal materials of this class ; including first, 
 feldspathic rocks, such as granite, syenite, and gneiss ; then sandstones, 
 limestones, marbles, serpentines, flagstones, and roofing-slates. 
 
 GRANITE, SYENITE, AND GNEISS. 
 
 These three rocks may be considered together, inasmuch as they may 
 be said to pass into each other. True granite and syenite are regarded as 
 intrusive rocks ; but there are varieties of stratified gneiss, which have the 
 same mineralogical composition, and can only be distinguished by traces of 
 
 Granite. a stratified structure, (pages 600 and 647). The most characteristic 
 intrusive granites in Canada, are those which have been described on page 
 434 as cutting the upper slates and limestones of Eastern Canada. In the 
 
 stanstead. township of Stanstead, a mass of this granite covers an area of about six 
 square miles ; occupying the first six lots of the fourth, fifth, and sixth 
 ranges, and of a part of the seventh range. It here cuts the limestones, which 
 are also intersected by numerous dykes of the intrusive rock. This granite 
 is a rather fine grained and uniform mixture of white orthoclase and white 
 quartz, with a sparing amount of black mica, giving a light grey color to 
 the mass. The rock is free from iron pyrites, and appears to be but little 
 affected by the weather. It is capable of being easily split by wedges into 
 blocks of almost any required size. This stone appears to compare favor- 
 ably with the best granites of Great Britain and of New England. 
 Although granite is more expensive to quarry and to dress than limestone, 
 its superior beauty and durability cause it to be preferred for structures 
 destined to be of a lasting nature ; and it is only the remoteness of this 
 beautiful granite from any line of transport, which has prevented its use 
 in our cities. With the facilities now offered by railways, it is to be hoped 
 that the granites of this eastern region will soon find their way into the 
 Canadian markets. 
 
 Many other masses of granite similar to that of Stanstead are found in 
 its vicinity. In the townships traversed by the Grand Trunk Railway may 
 be mentioned the granite of Barnston, on the first lot of the ninth range, 
 and also on the lots from seven to fifteen of the tenth and eleventh ranges. 
 
 Barford. In Barford, a beautiful granite occurs on the first and second ranges, from 
 the fifth to the ninth lot. It is also met with in the nineteenth and twen- 
 
CHAP. XXI.] GRANITE, SYENITE, AND GNEISS. 811 
 
 tieth lots of the fourth and fifth ranges of Hereford ; and in many localities 
 around the lakes at the sources of the St. Francis and Megantic Rivers. 
 Great Megantic Mountain is a mass of granite, which covers an area of 
 twelve miles in the townships of Marston, Hampden, and Ditton ; and Little 
 Megantic Mountain, also of granite, occupies six square miles in Winslow. 
 
 In this connection may be mentioned the gneiss of St. Joseph on the Gneiss. 
 Chaudiere, whose application to the construction of millstones has already 
 been noticed. This band of rock, which has a breadth of from fifty to sixty 
 feet, and can scarcely be distinguished from a fine grained, rather quartzose 
 granite, would make a good building material. A similar rock occurs on 
 the fourth lot of the sixth range of Shipton, and consists of white quartz 
 and orthoclase, with a little black mica, the quartz greatly predominating. 
 This stone, which yields large massive blocks, was employed in the con- 
 struction of the Grand Trunk Railway bridge across the Nicolet River. 
 
 Among the intrusive rocks of the Laurentian series, is a reddish syenite, syenite, 
 which is noticed on page 39, and forms an intrusive mass having an area 
 of about thirty-six miles among the Laurentian rocks in the townships of 
 Grenville, Chatham, and Wentworth. It is composed chiefly of a deep 
 flesh-red orthoclase feldspar, and a greenish-black cleavable hornblende. 
 Small portions of a white feldspar, probably oligoclase, and of grey trans- 
 lucent quartz, are scattered through the rock ; which is pretty uniform in 
 its character, and generally reddish from a predominence of the orthoclase. 
 To the eastern side of the mass however, in Chatham, a light colored 
 feldspar prevails. This rock is in some localities traversed by two sets 
 of parallel joints at right angles to each other, which much facilitate the 
 quarrying of small blocks. In other places, these joints are far apart ; but 
 the rock splits with much regularity in any direction, by the aid of wedges. 
 Blocks of a fine red variety of this syenite have been obtained from the 
 second lot of the fifth range of Grenville. The porphyries, which are crenvme. 
 associated with this syenite, will be noticed in the next class. A very 
 fine variety of syenite is obtained from Barrow Island in the St. Lawrence 
 near Gananoque ; and it is said to be common in numerous small islands 
 from this nearly to Brock ville. It differs from the last in containing but a 
 small proportion of greenish hornblende. The quartz, which is more 
 abundant than in the Grenville syenite, is somewhat bluish and opales- 
 cent ; and this, with the rarity of the hornblende, gives to the rock a 
 brighter red color, which is very agreeable to the eye, and resembles that 
 of the red Aberdeen granite. 
 
 The gneiss of the Laurentian series is in many localities well fitted for Gneiss, 
 building purposes ; but, like the syenites, it occurs in districts removed 
 from the towns, and has received but few applications. A greyish horn- 
 blendic gneiss has however been used in the construction of the reser- 
 voir for the Quebec water-works, near Jeune Lorette on the river St. 
 
812 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 Charles. The rock, which occurs near by, splits and dresses well, and is 
 easily obtained in blocks of large size. On the Batiscan River, near the 
 site of the old iron-furnace, is a quarry of gneiss, which appears to have 
 been once wrought, and which would afford an abundance of good blocks 
 for building purposes. At Bay St. Paul, near the bridge across the 
 Riviere des Mares, a fine grained greyish-white gneiss is found, which 
 would make a good building stone. It splits readily into rectangular 
 blocks, and can scarcely be distinguished from a true granite. A similar 
 light grey granitic gneiss occurs on the Ottawa, on the first lot of the first 
 range of Clarendon. Many other beds of a like quality, and others of 
 reddish gneiss, often well fitted for building purposes, may be obtained in 
 a great number of places along the north shore of the Ottawa. The 
 Laurentian rocks in many parts near the line of the Rideau Canal, would 
 probably afford similar materials. A fine red granite has been obtained 
 by Dr. Wilson in Bathurst. The labradorite or anorthosite feldspar rocks, 
 which are abundant in many parts of the Laurentian region, would make a 
 strong and durable building material ; but they are generally dark and 
 sombre in color. A pale yellowish variety of this near Chicoutimi was 
 observed to break with facility into great rectangular blocks. 
 
 The various intrusive rocks of the district of Montreal yield building 
 materials of a coarse description. The mountains of Brome and of Shef- 
 ford have already been described on page 656, as composed of a granitoid 
 
 Trachyte, trachyte. This rock consists of crystalline grains of orthoclase, with small 
 portions of mica and hornblende ; and differs from granite in the absence of 
 quartz ; which not only adds to the hardness of the true granites, but seems 
 to bind together the crystals of the feldspar. From the want of quartz, 
 
 Brome. these trachytes of Brome and Shefford Mountains are more subject than 
 granite to crumble from atmospheric influences ; and their ruins form a 
 coarse gravel, which makes up a large portion of the surface-soil in their 
 yicinity. From the existence of regular joints, these rocks are readily 
 divided into rectangular blocks, which may be found sufficiently durable for 
 
 Shefford. building purposes. They are of an agreeable greyish or yellowish tint, 
 and much resemble granite. The rock from the southern side of Shefford 
 Mountain appears to be finer grained, and firmer than in some other locali- 
 
 Dionte. ties. The granitoid diorites of Yamaska, Beloeil, and Mount Johnson, de- 
 scribed on pages 663-665, would furnish also abundance of a strong coarse 
 material for building purposes ; and being situated in a region of soft shaly 
 rocks, are of some local importance. The dolerites of Rougemont, Montar- 
 
 Doierjte. ville, and Mount Royal, (pages 665-667,) are, for the most part, highly 
 augitic, dark colored, and too subject to decay to furnish a good building 
 material. In the vicinity of Montreal however some of the dykes of finer 
 grained intrusive rocks, in great part trachytes and dolerites, are occa- 
 sionally employed for coarse constructions ; and they are also broken up 
 
CHAP. XXL] SANDSTONES. 813 
 
 for macadamizing roads, for which purpose they are much better fitted 
 than the limestone that is often substituted for them. . 
 
 SANDSTONES, 
 
 In describing the sandstones and the limestones which are capable of 
 being employed for building purposes, it will be convenient to keep in view 
 the geological classification hitherto followed, and to begin with the older 
 formations. Without noticing the rocks of the Huronian series, and the newer 
 strata of Lake Superior, both of which will doubtless, one day, yield abun- 
 dance of sandstones fitted for building purposes, the rocks of the Potsdam Potsdam, 
 formation may be noticed. This, in its distribution to the eastward of 
 Kingston, furnishes in many places a fine white sandstone, which is often 
 free from stains, and capable of yielding blocks of a pure quartzose sand- 
 stone of considerable size. It is a durable stone, which is not only capable 
 of resisting the weather, but, unlike the limestone, is fire-proof, not being 
 liable to crack by the effects of a high heat. The toughness and closeness 
 of its grain, and its hardness, which is much greater than that of many of 
 the sandstones hereafter to be noticed, constitute the objections to its use. 
 
 At Lyn, near Broekville, massive beds of a superior quality are Lyn. 
 
 found, from which sandstone has been procured for the new Parliament 
 
 buildings at Ottawa. The further distribution of this sandstone is given on 
 
 page 91, and the succeeding pages. It is exposed over a wide area in 
 
 the county of Beauharnois. The beds here are generally even, and of Beauhamois. 
 
 very varying thicknesses. As they are readily separable, but little difficulty 
 
 is found in quarrying the stone. The color is generally white or slightly 
 
 yellowish or greyish ; and the stone, although hard, may be smoothly 
 
 dressed, and preserves its sharp edges. There is a quarry in the village of 
 
 Beauharnois ; and another on the one hundred and fifty-first lot of the 
 
 second range of Williamstown, from the stone of which several houses have 
 
 been erected. Very fine blocks of this sandstone have also been procured for 
 
 building purposes on the eightieth lot of the second range of Hemmingford. 
 
 This sandstone formation extends across the river, including Isle Perrot, 
 
 and is found from the Cascades to Rigaud on the south side of the Ottawa, vaudreuii. 
 
 and also on the opposite side ; passing by Lachute to St. Jerome. At Ste. 
 
 Scholastique, the beds are fine grained, white, very even, and of varying 
 
 thickness, some of them as much as two feet. Beds of the rock, suitable 
 
 for building purposes, may be found in a great many localities throughout 
 
 this area. Ascending the Ottawa, good massive sandstone occurs in the 
 
 front of the Augmentation of Grenville, and also at Quin's Point in the 
 
 seigniory of Petite Nation. This stone is also exposed on the twenty-sixth, Nepean. 
 
 twenty-seventh, and twenty-eighth lots of the fifth and sixth ranges of 
 
 Nepean ; where a quarry has been opened, from which stone has been 
 
814 GEOLOGY OF CANADA. [CHAP. XXIi 
 
 taken for the Parliament buildings at Ottawa. Good stone may also be 
 obtained from the beds of this formation in Ramsay and in Pakenham. 
 The distribution of the Potsdam formation on the north side of the St. 
 Lawrence, is described on page 95. It affords in many places good 
 material for building and for paving. The large blocks of sandstone which 
 st. Maurice, are used for lining furnaces, and are obtained from the St. Maurice on its 
 right bank, at the foot of the Gabelle rapid, have been already mentioned, 
 smery. The Sillery division of the Quebec group affords massive beds of a 
 
 greyish-green sandstone, which consists chiefly of grains of translucent quartz 
 in a greenish argillaceous cement. Small portions of feldspar are occasion- 
 ally present, and a little mica between the beds. This stone is obtained in 
 several places between Quebec and Cape Rouge. The beds are there 
 massive, and dip to the south-south-east, at an angle of fifteen degrees. 
 A thickness of about forty feet has been quarried. The upper beds of this 
 are even, and split well, both with the layers and across them ; but the 
 lower portions are inferior in this respect. The stone has been used in 
 the construction of many houses in and around Quebec, and in various 
 parts of the walls of the fortress. It is however apt to exfoliate by the 
 action of the weather, and to wear irregularly. 
 
 chazy A band of sandstone is found in the Chazy formation, below the water- 
 
 formation. ii me? wnose distribution has been indicated on page 806. This sandstone 
 from the vicinity of Hawkesbury, was used in the construction of the locks 
 of the Grenville Canal ; but it is inferior in quality to that which is met with 
 Pembroke, farther west in the same formation y in the township of Pembroke. Here it is 
 exposed on the river about four miles below the village, and farther up, on 
 Allurnette Island, where it is found on the fifth range of the township, from 
 the forty-fourth to the forty-eighth lot. The sandstone here occupies a 
 thickness of three or four feet in beds of from six to eighteen inches. It is 
 of a warm grey tint, sometimes inclined to reddish ; and being soft, is easily 
 wrought and carved. It is however ^ufficiently tough to retain sharp 
 angles ; and it will make a very superior building stone, which may probably 
 be found elsewhere in the distribution of the band. A soft fine grained 
 greenish sandstone, which occurs at the base of the Trenton group, on 
 Matchedash Bay on Lake Huron, has been described on page 192. 
 Grey Band. In Western Canada, a belt of sandstone strata, known as the Grey band , 
 is traced, with some interruptions, from Queenston to Collingwood. Its 
 distribution is described on pages 313-317. The thickness of this band of 
 sandstone varies from ten to twenty feet or more ; the separate beds being 
 from a few inches to two or three feet. It is fine grained, compact, and 
 sometimes nearly white in color, at other times light grey, occasionally with 
 a greenish tinge ; and it furnishes an excellent material for building purposes, 
 for which it is largely used in many towns of Western Canada. Univer- 
 sity College at Toronto, and many other buildings both in that city and in 
 
CHAP. XXI.] LIMESTONES. 815 
 
 Hamilton, are constructed of this sandstone. It is extensively quarried for 
 these purposes at Georgetown, in Esquesing on the Grand Trunk Railway ; 
 and also at Hamilton and in its vicinity, at Dundas and at Waterdown, Hamilton, 
 where the band is ten or twelve feet thick. This sandstone is also quarried 
 to a smaller extent at various localities along its outcrop. At Nottawasaga, 
 the band attains a thickness of twenty feet ; and is employed for the 
 manufacture of grindstones and whetstones, as mentioned on page 809. 
 The Oriskany sandstone of the Devonian series has been noticed on the Onskany 
 same page as furnishuig a material fitted for millstones. This rock fur- 
 nishes in some parts of its distribution, massive beds of a fine grained 
 white sandstone from one to three feet hi thickness, which are well adapted 
 for building, and are quarried for this purpose on the forty-eighth lot of 
 the first range of North Cayuga. 
 
 The Gaspe* sandstones would yield an abundance of good building mate- 
 rial in many parts of their distribution. In Anticosti, on the north side of Anticosti. 
 the island, there is a band of about fifty feet of sandstones, belonging to the 
 summit of the Hudson River group, which is exposed for several miles 
 along the coast near Cape James, and also at Table Head. The sand- 
 stones are greenish-grey, and often in massive beds, which are sometimes 
 five feet in thickness and of a free grain well fitted for working. Immense 
 blocks of this stone, which have fallen from the cliff, are seen on the beach 
 at Cape James. 
 
 LIMHSTONES. 
 
 In describing the materials for the manufacture of lime, the principal 
 facts as to the distribution of limestones have been briefly noticed ; and it 
 now remains to mention such localities as afford stones fit to be quarried for 
 building purposes. It is customary to distinguish by the title of marbles, 
 such limestones as are adapted for decoration ; and under the present head- 
 ing therefore, these will only be incidentally mentioned. The Laurentian 
 limestone would yield in many localities materials adapted for building. 
 The coarser grained varieties of it are often however subject to crumble 
 by the action of the weather ; but the finer and more compact ones are in 
 many cases suitable for marbles, and will be noticed under that head. The 
 crystalline limestone of Macnab, there to be described, has recently been 
 employed by the Board of Works in the construction of a bridge across the 
 Madawaska River. 
 
 The Calciferous formation, whose distribution has been described in the 
 seventh chapter, consists for the most part of a bluish-grey crystalline 
 magnesian limestone or dolomite, in many places marked by small geodes 
 holding calc-spar, and more rarely sulphate of barytes, gypsum, and quartz. 
 This rock is employed in some parts of the province for building purposes, 
 
816 GEOLOGY OP CANADA, [CHAP. XXL 
 
 and is a strong, durable material ; but it soon becomes yellow by the action 
 of the weather. It was extensively used in some of the locks of the Rideau 
 Brockriite. Canal, and is employed for building purposes at Brockville and at Pres- 
 cott. Near the former town, it is quarried on the second lot of the first 
 range of Elizabethtown, and on some adjoining lots. Good quarries of it 
 are also found both above and below the town of Prescott. The numerous 
 exposures of this formation farther down the St. Lawrence, and upon 
 the Ottawa, would furnish abundance of common building stone ; but the 
 limestones next to be noticed, are generally preferred. 
 
 The Lower Silurian limestones, comprising the Chazy formation and the 
 overlying Trenton group with its subdivisions, form a great limestone belt, 
 whose distribution has been already given in detail. The Chazy forma- 
 tion is unknown to the west of Kingston ; but the limestone of the Trenton 
 group forms numerous islands in Lake Huron, and is traced from Notta- 
 wasaga, by Lake Simcoe, to the shore of Lake* Ontario ; where it appears 
 Bowman- near Oshawa, and at Bowmanville has been quarried for the purposes 
 of the Grand Trunk Railway. Thence downward to Kingston, the 
 Trenton limestones underlie the whole of the lake shore and of the peninsula 
 of Prince Edward, extending back for a considerable distance. The lock 
 on the Otonabee Canal is constructed of massive beds of limestone, from 
 the lower part of the Trenton group, which was quarried near Warsaw, in 
 Dummer ; and good beds of similar stone are to be obtained in many other 
 places in this region. The upper beds of this group are usually too thin, 
 shaly, and irregular to be employed with advantage for building purposes : 
 and hence it is that although standing upon limestone, the houses of 
 Cobourg, Trent, and Belleville are in great part of brick. The lime- 
 Kingston, stone of which Kingston is chiefly built, is taken from beds which are sup- 
 posed to belong to the base of the Trenton group. This material, although 
 affording good blocks, is fine grained and compact, with a conchoidal frac- 
 ture, and has the defect of brittleness. In descending the St. Lawrence, 
 these limestones afford excellent building material in the township of 
 Cornwall. Cornwall, where quarries have been opened on the fifth and sixth lots of 
 the second range. Here are exposed two compact beds of black lime- 
 stone, each from three to five feet in thickness, which were used in con- 
 structing the locks of the Cornwall Canal. Near Mille Roches in the 
 same township, is another quarry of similar stone ; and good beds of black 
 limestone are wrought in the townships of Winchester, Finch, Charlotten- 
 burg, and Lancaster. These black beds are overlaid in some places by 
 grey limestones, which furnish good building material in the township of 
 Kenyon, and in Lochiel. 
 
 Beds yielding fine blocks of limestone are found both in West and 
 East Hawkesbury. Stone from the latter was employed in building the 
 Carillon Canal. On the north side of the Ottawa, in Grenville and Carillon, 
 
CHAP. XXI.] LIMESTONES. 817 
 
 a bed of limestone, two or 'three feet in thickness, is quarried in several 
 places for building purposes. This limestone, which, like that of Hawkes- 
 bury, belongs to the Chazy formation, lies below the sandstones of this 
 region, already noticed. Farther to the westward, in the vicinity of 
 Ottawa, the Gloucester quarries, which furnish the stone chiefly used in Ottawa, 
 that city, yield a grey granular stone ; which, like that of Montreal, belongs 
 to the lower part of the Trenton formation. The beds here vary from 
 three to twenty inches, and the price of good blocks of stone at the quar- 
 ries is said to be about twenty cents the cubic foot. At the Hogsback 
 lock, on the Rideau Canal, quarries are opened in a limestone which is 
 somewhat lower in the series, and belongs to the Birdseye and Black 
 River formation. At this place there are said to be two solid beds, one 
 two feet, and the other two feet eight inches in thickness. 
 
 The Chazy formation at Grande Isle in the St. Lawrence, near the Grande isle. 
 head of the Beauharnois Canal, affords a strong bluish-grey limestone in 
 beds of about two feet thick, which were quarried for the locks of the canal. 
 Large quantities of stone for this purpose, and also for the upper locks of 
 the Lachine Canal, were obtained from Caughnawaga, where massive beds caughnawaga. 
 of the same formation, grey in color, with red spots, furnish an excellent 
 building stone. This limestone crosses the west end of the island of 
 Montreal, and is exposed at Ste. Genevive, where it yields very fine 
 blocks ; and on Isle Bizard, where it was quarried for the Carillon Isle Bizard - 
 Canal. The formation is also exposed in a quarry at La Chapelle's 
 bridge, and again near Montreal. 
 
 The stone quarried at Pointe Claire, which is black, compact, and in Pointe ciaire. 
 massive beds, belongs, like the similar stone of Cornwall, to the lower por- 
 tion of the Trenton group. At this quarry there is an exposure of about 
 thirty feet of solid beds, varying from one to three feet in thickness. From 
 these were obtained the stone for the piers of the western half of the 
 Victoria Bridge. The blocks quarried for this purpose weighed from four 
 to seven tons each. The stone for the eastern half of the bridge was 
 brought from Isle la Motte, in Lake Champlain, and from beds which are 
 said to be in the same stratigraphical position as those of Pointe Claire. 
 
 The chief part of the limestone quarried in the immediate vicinity of the Montreal, 
 city of Montreal, is derived from the grey beds which are near the base 
 of the Trenton formation, but overlie the black beds of Pointe Claire. 
 These latter belong to that division of the Trenton group which is known 
 as the Birdseye and Black River formation. This grey band has a thick- 
 ness of from eight to twelve feet, and is made up of beds which vary from 
 three to eighteen inches. In tracing the individual beds from one quarry 
 to another, they are found to vary in thickness ; one of them occasionally 
 dividing into two or more, or several thin layers uniting into one solid bed. 
 The trap dykes which intersect this limestone are noticed on page 143. 
 
 B* 
 
818 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 These grey beds consist in great part of the remains of crinoids and 
 cystideans ; and it is the crystalline texture of these organic remains 
 which gives a granular structure to the rock. The grey limestone is 
 Black beds, overlaid by black nodular beds, which are accompanied by shales of the 
 same color ; and a layer of black limestone is also interstratified with the 
 grey beds. These black portions are used for inferior constructions, or 
 for burning into lime. 
 
 There are four principal quarries in this band near the city ; and from 
 these are derived the stone used in the best buildings in Montreal. The 
 still lower grey beds, belonging to the Chazy formation, which have just 
 been noticed as occurring at the quarries of St. Genevidve and Isle Bizard, 
 are exposed near Montreal, in a range running parallel with the last, and 
 about three quarters of a mile to the westward. This stone has also a 
 granular texture, due to the great quantity of organic remains which it con- 
 tains. It is less uniform in color than the higher strata nearer the city, 
 and is liable to become yellow by the action of the weather ; but the beds 
 yield large and solid blocks, which have been extensively employed for the 
 quays and canal-docks of Montreal. Numerous quarries are opened in 
 this stone near the Mile-End toll-bar, and thence along the road to 
 Sault au Recollet ; where they show in many places beds of from one to 
 two feet thick of good grey stone. 
 
 The quantity of limestone annually taken from these quarries in the 
 immediate vicinity of Montreal is very considerable. For the year 1861, 
 it was as follows : 
 
 313,200 cubic feet of cut stone. . . . ; 28,600 tons. 
 
 5,252 toises of rubble 63,024 " 
 
 91,624 " 
 
 A French toise of stone is equal to 9'68 cubic yards English. The 
 average price in Montreal of good stone from these quarries, was in 1861 
 as follows : 
 
 Undressed ashler $0-13^ per square foot. 
 
 Dressed " 0-30 " " " 
 
 Heavy rough blocks (from six to thirty cubic feet).. 0-60 " cubic " 
 
 (of sixty cubic feet) 1-00 " " 
 
 Mouldings ; average 0'45 " square " 
 
 Fluted columns of 18 inches diameter ; for the stone, 1*00 " rising " 
 
 " " " for cutting,. 2-50 " " " 
 
 The Chazy formation yields excellent grey granular stone on Isle Jesus, 
 
 a mile and a half south of Terrebonne ; where two beds, each of five feet 
 
 thick, were wrought for the construction of the lower locks of the Lachine 
 
 Canal at Montreal. Massive beds of the same formation are quarried in 
 
 st. Lin. Lachenaye, near St. Lin; where some portions of it are of a red color, and 
 
CHAP. XXI.] LIMESTONES. 819 
 
 yield a good marble. At Industry, near the upper bridge, it presents industry, 
 good grey limestone, in beds of two or three feet thick. Near this, the 
 higher grey beds of the Trenton formation are quarried, and were em- 
 ployed for the railway bridge at this place. Similar beds, near the Dalles 
 on the Naquareau River, give a good building stone. 
 
 Farther down the St. Lawrence, the limestones, which form a broad belt 
 along the north shore, are generally covered by the superficial deposits as 
 far as the Grondines. Here a large amount of stone fitted for lime-burning, 
 and for ordinary building purposes, is exposed. In the fourth range of the 
 seigniory of La Chevrotiejre, and three or four miles from the St. Lav,-- 
 rence, grey beds of the Trenton formation yield an excellent building 
 material, which is much used at Quebec, where it is known as the Des- 
 chambault stone. The beds which are here wrought are nearly horizontal, 
 and are three in number. The upper and lower ones have each a thickness 
 of eighteen inches, while the middle one is three, feet, and the bed under- 
 lying these is said to be four feet in thickness. This stone has a yellower 
 tint than that of Montreal, and does not become discolored by the weather ; 
 it is also more granular, softer, and more easily wrought ; but does not pre- 
 serve such sharp angles as the Montreal stone, nor receive as good a sur- 
 face by what is called picking. In the rear of the same seigniory, a some- 
 what similar stone, in thinner beds, occurs at the St. Olivier bridge on the 
 Ste. Anne. In the first range, stone was obtained for the constructions 
 on the Quebec and Richmond Railway : the blocks are massive, but are 
 penetrated by thin shaly layers and patches, which injure the aspect of the 
 stone after exposure to the weather. At Pointe aux Trembles^near Que- 
 bec, are massive beds, which furnish large blocks of a harder and less granu- 
 lar grey limestone, more resembling the Trenton beds at Montreal. This 
 stone is quarried for the Quebec market. In the continuation of the lime- 
 stone band thence to Beauport and Montmorenci, great quantities of stone Beauport. 
 fit for lime-burning, and for common building purposes, are met with. At 
 Chateau Richer also there are several quarries, from which large quantities 
 of limestone are obtained for building in Quebec ; but the best stone for the 
 use of this city is brought from La Chevrotiere and Pointe aux Trembles. 
 
 The dark grey limestones of this formation at Bay St. Paul and Murray Murray 
 Bay afford a serviceable building material. At the latter place, the Bay - 
 arenaceous limestones noticed on page 162, furnish beds from eight to 
 sixteen inches in thickness, of a light grey stone, which becomes yellowish 
 when exposed to the air. The strata dip to the northeast at an angle of 
 about fourteen degrees. They are easily wrought and dressed, and have 
 been used in the construction of the church and several other buildings at 
 Murray Bay. The Lower Silurian limestones about Lake St. John afford, Saguenay. 
 near the mouth of the Metabechouan River, massive granular beds, fit 
 for building purposes. The thick beds of yellowish-white granular lime- 
 
820 GEOLOGY OP CANADA. [CsAP. XXL 
 
 stone at the Mingan Islands, noticed on page 134, would afford a superior 
 Anticoeti. building material. At Southwest Point in Anticosti, the yellowish-white 
 limestone, mentioned on page 304, yields large blocks, which are easily 
 dressed, and have been employed in the construction of lighthouses there 
 and at Heath Point. 
 
 It has been shown on pages 205 and 273, that what is called the 
 Deschambault anticlinal brings to the surface, a little to the east of the 
 Yamaska River, a narrow band of the Lower Silurian limestones. Along 
 st. Domi- this line, at the St. Dominique quarries, a thickness of thirty or forty feet, 
 nique. exhibiting many massive beds, is quarried. Like the limestones of Ste. 
 Genevieve and Caughnawaga, it belongs to the Chazy formation, but it is 
 darker colored and more compact. It is used for building at St. Hya- 
 cinth, and was employed in the constructions of the St. Lawrence and 
 Atlantic Railway. The superior lime obtained from this band at Ste. 
 Rosalie has already been noticed. To the southward, what appears to be 
 a continuation of this anticlinal exposes the limestones at Highgate Springs, 
 in Vermont ; and a dislocation a little to the eastward brings up those of 
 Phillips- Phillipsburg. At the latter place the band is nearly two miles wide, 
 and dips with a gentle angle to the southeastward. The rock here, unlike 
 that near St. Hyacinth, is somewhat crystalline, apparently from a com- 
 mencement of metamorphism, and near the base is mixed with small 
 veins and patches of white quartz. Higher in the series, massive beds 
 occur, some of which would furnish a good building material. Its color 
 varies from nearly white or light grey, to dark grey or black ; some of 
 the beds being banded or mottled with different colors. 
 
 In Western Canada, a band of limestones not less extensive than that 
 whose distribution through the eastern part of the province has just been 
 described, is traced from the Niagara River northwestward to Lake 
 Huron. It includes the Niagara and Guelph formations, already described 
 in the twelfth chapter, and yields excellent building stone in many parts 
 of its distribution. Unlike most of the Lower Silurian limestones, this 
 band is almost everwhere magnesian, and generally has the composition of 
 a true dolomite. Great quantities of excellent building material are 
 obtained from this series in various parts along its outcrop. Near Niagara 
 Niagara Falls it has been quarried for the construction of the piers of the Suspen- 
 Faiia. s i on bridge, and large quantities of good stone are obtained at Thorold, 
 (page 328). Quarries are also opened in it at Gait, Hespeler, Puslinch, 
 Gueiph. and many other places. The quarries at Guelph are in the Guelph for- 
 mation, and show a thickness of about fifteen feet of workable beds, which 
 range from a few inches to three feet. The stone, which is easily worked, 
 and is of a superior kind for building purposes, has been extensively used 
 in the town of Guelph. These dolomites are frequently somewhat cellular, 
 but are strongly coherent. They have been described on page 624. 
 
CHAP. XXI.] LIMESTONES. 821 
 
 At Kockwood in Eramosa, there is an exposure of more than 100 feet Rockwood. 
 of crystalline dolomite belonging to the Niagara formation, in beds vary- 
 ing from a few inches to ten feet in thickness. Of these, about thirty feet 
 are nearly white, the remainder being of a light grey. This stone, which 
 does not become discolored by exposure, has been used for the piers of 
 the railway viaduct over the Eramosa River. JA Owen Sound, a similar Owen 
 exposure of this formation occurs, and is capable of furnishing a great S( 
 supply of blocks of any required size of a light yellowish-grey stone, which 
 resists the action of the weather, and does not become discolored. The 
 quarries are about half a mile from the harbor ; and the stone has been used 
 for building purposes in the town of Owen Sound, and for the construc- 
 tion of several lighthouses along the shore of Lake Huron. 
 
 The Onondaga or gypsiferous formation, which overlies the preceding 
 rocks, consists chiefly of a dolomite, which is generally toe thin-bedded 
 for building purposes. On the fourth lot of the second range of Brant Brant . 
 however, at the Oxbow on the Saugeen River, it presents several thick beds 
 of a very fine-grained yellowish-grey dolomite, which appears to be well 
 fitted for architectural purposes. It is free from stains, may be split with 
 regularity, and works with facility ; when fresh from the quarry, it may 
 be cut with a saw, but soon hardens on exposure. Two bands of this stone, 
 each of about ten feet in thickness, occur in this formation. The higher 
 one, which is at its summit, is here exposed at the surface, and offers facili- 
 ties for quarrying. It is made up of massive beds, some of them two feet 
 in thickness ; and a bed of three feet occurs in the lower band. Beneath 
 the upper band is a bed of light grey oolitic rock, seventeen inches in 
 thickness, which has been used with advantage in the neighborhood for 
 supporting the axles of mill-wheels. 
 
 The pure limestones of the Corniferous formation, in various parts of their 
 distribution, yield a stone which is well fitted for building purposes, and is 
 quarried in many places along its outcrop, as at St. Marys and at Goderich. Maiden. 
 At Maiden, near Amherstburg, the limestone is more granular than to the 
 eastward, and is of a whitish or a buff color. The beds, which are here 
 from one to two feet in thickness, are extensively quarried for building, 
 and the stone is carried to considerable distances. In some p^rts of this 
 formation, the limestone becomes so much mingled with chert as to be 
 unsuited for building, and the cherty portions are then employed with 
 advantage for macadamizing roads. 
 
 MARBI/ES AND SERPENTINES. 
 
 The name of marble is applied to those varieties of limestone which, 
 from their fineness of texture and color, and from their susceptibility of 
 polish, are proper for decorative architecture, or for sculpture. .Marbles 
 may consist either of pure or of magnesian carbonate of lime. The presence 
 
822 GEOLOGY OF CANADA. [CHAP. XXI. 
 
 of foreign minerals generally renders a limestone unfit for use as a marble ; 
 but serpentine, which does not differ much from carbonate of lime in hard- 
 ness, is often intermingled with it, and gives rise to some fine varieties o 
 marble. This mineral may greatly predominate over the limestone, or 
 even exclude it altogether ; thus giving rise to serpentine rock, or ophio- 
 serpentine. lite, which through theai admixtures passes into the marbles proper. As 
 all of these have about the same hardness, and are employed for similar 
 uses, they are not unfrequently confounded under the technical name of 
 marble. For convenience therefore, the serpentine-marbles and serpen- 
 tines will be noticed in connection with the true marbles of the province. 
 But little use has yet been made of these various materials in Canada ; 
 and witli the exception of three or four cases which will be mentioned, the 
 only trials as yet made of the marbles and serpentines of the province ? 
 have been by the Geological Survey ; who have selected from various 
 localities, blocks which have been cut and polished. These being from the 
 surface of the rocks, are frequently more or less affected by the weather, 
 and give but imperfect representations of the capabilities of the material. 
 In this way however have been obtained the collection of marbles in the 
 Geological Museum, and those which were sent to the Great Exhibitions 
 of 1851, 1855, and 1862. The great variety of these, and the beauty of 
 many of them, attracted particular attention on these occasions ; and the 
 collection of Canadian marbles was especially commended in the Report 
 of the Paris Exhibition. It is proposed to notice first the marbles and 
 serpentines of the Laurentian series, then those of the Quebec group, and 
 finally the marbles of the more recent Silurian strata. 
 
 Laurentian The crystalline limestones of the Laurentian series yield in many cases 
 eerier. a s t r ong white marble, which, although not generally fine enough for 
 statuary, is well fitted for purposes of decoration. Among the localities 
 on the Ottawa may be mentioned the Calumet Falls, Portage du Fort, 
 and Fitzroy Harbor ; which last has been employed for the Parliament 
 Portage du buildings at Ottawa. Portions of the Portage du Fort marble are of 
 Fort a tolerably fine grain, pure white in color, and of a quality well fitted for all 
 purposes but that of statuary. Near Beverley, in the township of Bastard, 
 Bastard. beds of thjs limestone are wrought as a marble for tombstones. It is 
 strongly coherent, but greyish-white in color, and contains small span- 
 gles of mica and of graphite. Similar marbles may be found among the 
 limestones on the north side of Charleston Lake, and in many other parts 
 of this region ; but where they have the requisite strength and fineness 
 of grain, they are often mixed with small portions of foreign minerals, 
 generally quartz, pyroxene, hornblende, or mica. In the township of 
 Madoc, on the thirteenth lot, and near the road between the seventh 
 and eighth ranges, is a band of a fine-grained yellowish-white magne- 
 sian limestone, which would apparently yield a marble. Large blocks of 
 
CHAP. XXL] MARBLES. 823 
 
 a very good white marble have also been obtained from the adjoining Marmora, 
 townships of Elzivir and Marmora : that from the latter place is extremely 
 pure, white, and compact. 
 
 A fine white marble is found in the township of Barrie, where th'e Lau- Bame. 
 rentian limestones are said to be extensively developed on the twenty- 
 seventh, twenty-eighth, and twenty-ninth lots of the ninth and tenth ranges. 
 Blocks of considerable size have been brought from this locality, and show 
 a fineness of grain and a strength equal to the best foreign statuary 
 marbles. Grains and spots of tremolite, and more rarely of quartz, are 
 however disseminated through thia marble, and detract from its value. 
 Specimens of an equally fine grained marble from the same locality, have 
 a uniform pink or rose tint, and others are of a dove-grey color. Besides 
 these, variegated marbles of blue and white, and of purple and brown colors 
 are said to be found here, which appear to be more free from foreign 
 minerals, and may probably yield abundance of colored marbles for the 
 purposes of interior decoration. 
 
 At the mouth of the Madawaska in MacNab, on the Ottawa, there is a 
 great extent of crystalline limestone, which is colored of a bluish-grey, 
 apparently from an admixture of plumbago. This color is irregularly dis- 
 tributed, some portions being nearly black, and others almost white, so that 
 the rock often presents a striped or barred appearance. In many cases 
 however the beds are very much corrugated, and sections of it exhibit 
 curious complicated patterns like the grain of certain woods ; the white, 
 bluish-grey, and black colors being so arranged as to give very pleasing 
 effects. Different portions of the marble vary in the size and arrangement of 
 the colored bands ; and their aspect changes as it is cut with or across the 
 beds. The stone is somewhat coarse grained, and contains a little tremo- 
 lite ; but it takes a good polish, and is obtained in large blocks, which are 
 easily wrought. A mill has been erected in the vicinity, at Arnprior, for 
 the purpose of sawing and polishing this stone, which is known as the Amprior. 
 Arnprior marble, and has begun to be employed both for interior decora- 
 tion, and for funeral monuments ; for which last, by its color, it is well 
 adapted. The price of the marble delivered in Ottawa, is stated to be 
 $1-50 the cubic foot ; or sawn into slabs, $0-45 the square foot. 
 
 The serpentine which is mingled with .the crystalline limestones of the 
 Laurentian series in many parts of their distribution, gives rise to varieties serpentin 
 of marble in which grains or small masses of the serpentine are dissemin- marbles> 
 ated through a white crystalline base, with a banded arrangement which 
 marks the stratification of the rock. The serpentine is generally of some 
 shade of olive-green or oil-green, but is occasionally of a sulphur-yellow 
 color. Specimens of these marbles may be obtained in many parts of Gren- 
 ville, and of its Augmentation. On the sixteenth lot of the third range of 
 Grenville, a mill was some years since erected at the fall of the Calumet 
 
824 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 River, for the purpose of sawing a marble of this kind. The limestone 
 strata here dip to the northwest at a high angle, and are overlaid by a 
 micaceous gneiss, which holds garnets. A dyke of dolerite, several feet in 
 thickness, cuts the strata ; and a thin layer of greenish translucent serpen- 
 tine, half an inch or more 'in thickness, sometimes with a fibrous coating, 
 occurs bounding the trap on each side of the dyke, as if filling up a space 
 left between the intrusive rock and the limestone. A description and an 
 analysis of this serpentine, to which the name of retinalite was given by 
 Dr. Thompson, will be found on page 471. On the eighteenth lot of the 
 wentworth. first range of Wentworth, a similar limestone, mixed with smaller grains of 
 serpentine than the last, is met with, and would yield a more pleasing 
 variety of marble. 
 
 On the thirteenth lot of the fifth range of Grenville, a massive serpen- 
 Serpentine. tine is associated with the pyrallolite already described on page 789. 
 This serpentine, from which slabs of considerable size have been cut, is of 
 a pale green color, marked with spots and clouds of a rich red-brown color, 
 due to disseminated peroxyd of iron, and forms a fine ornamental stone. 
 A similar pale green serpentine, marked with red, has been found by 
 Dr. Wilson, in Burgess. An analysis of this, and of some others of these 
 ophiolitic rocks, will be found on page 591. 
 
 Serpentines are still more abundant among the crystalline portions of 
 the Quebec group, where they constitute great rock masses ; which have 
 already been described, with numerous analyses, under the name of ophio- 
 lites, on pages 608-612. They are generally darker colored, tougher, 
 and better fitted for ornamental purposes than those of the Laurentian 
 series. The distribution of these rocks in Eastern Canada has been given 
 in detail in the eleventh chapter. It may be said that they are almost 
 everywhere found as a part of the magnesian band in the second and third 
 synclinals of the Quebec group (page 710). Among these ophiolites are 
 many which are well fitted for ornamental purposes. These are chiefly 
 mixtures of limestone or of dolomite with serpentine ; the latter mineral 
 generally predominating. No attempt has as yet been made to work 
 these serpentine-marbles ; and it will for the present be sufficient to 
 mention those localities from which blocks available for ornamental pur- 
 poses have been obtained by the Geological Survey. 
 
 In the township of Melbourne, a band of serpentine has been traced 
 for about four miles on the fifth and sixth ranges, and it attains in one place 
 a breadth of a mile. In this part, on the twenty-second lot of the sixth 
 range, some beds of the rock assume the character of a very calcareous 
 conglomerate, the pebbles of which are arranged in such a way as to mark 
 the stratification of the rock. Other portions are apparently homogenous 
 in texture, and are dark green, banded or chequered with lighter green 
 lines. A very beautiful variety which is found here has a dark or 
 
 Quebec 
 group. 
 
 Melbourne. 
 
CHAP. XXL] SERPENTINES. 825 
 
 blackish-green ground, through which small and more or less angular 
 spots of a much lighter green are equally distributed, giving to the rock 
 the aspect of a porphyry. Blocks of this a foot or more in diameter 
 have been obtained entirely free from flaws, and receiving a fine polish. 
 A paler green serpentine occurs on the twentieth lot of the fifth range ; 
 and near the middle of the band is a dark green variety veined with red, 
 which resembles somewhat the Cornish serpentines. 
 
 In the township of Orford, fine blocks of serpentine have been obtained orford. 
 from the twelfth lot of the eighteenth range. Some portions of this have 
 the aspect of a breccia of dark green serpentine in a lighter green paste of 
 magnesian carbonate of lime ; while others, which are more homogenous, 
 and resemble one of the varieties from Melbourne, have a dark green base, 
 with veins of paler green. Large slabs have been obtained from this 
 quarry, and columns of three feet in length and a foot in diameter. 
 The rock is solid, free from flaws, and susceptible of a fine polish. 
 
 The serpentine of St. Joseph on the Chaudire, has also furnished fine st. Joseph, 
 masses of a brecciated or conglomerate green serpentine veined with 
 white. At Mount Albert in Gaspe*, the serpentines, which are there Mount 
 associated with chloritic, epidotic, and hornblendic slates, and which have Albert> 
 been described on page 266, cover an area of no less than ten square 
 miles. Much of the serpentine is distinctly stratified, and is often striped 
 with red and brown colors. There is little doubt that both here and in 
 many other localities throughout this region, fine varieties, well fitted for 
 ornamental purposes, may be obtained in any quantity required. The 
 serpentines of Roxbury and Cavendish in Vermont, which are found in 
 a continuation of the formation of Eastern Canada, have been extensively 
 wrought and sold under the name of verd-antique marble. They resemble Verd 
 the verd-antique found in ancient Roman ruins, the original locality of an que ' 
 which is unknown. It is a mixture of serpentine with limestone or dolo- 
 mite, similar in composition and in aspect to many of the serpentine rocks 
 of Vermont and of Eastern Canada. Much difficulty was at first met with 
 in giving a fine polish to the Vermont serpentines ; but a substance for Polishing 
 the purpose was at length discovered in the actinolite which often accom- serpen 
 panics them. This mineral is reduced to aji impalpable powder by grind- 
 ing and mixing with water. In this way the coarser material is separated 
 rom the finer portions, which remain for a long time suspended, but are 
 at length deposited as a fine paste of actinolite, which is found to be 
 much superior to any other substance for polishing serpentine. A bed 
 of actinolite rock which occurs in Bolton, and has been noticed on 
 page 797, would probably furnish an ample supply for this purpose. 
 
 Serpentines similar to those of the Eastern Townships are extensively 
 wrought in Italy, France, and England, and are employed for tables, 
 chimney-pieces, columns, and the decoration of churches. The price of 
 
826 GEOLOGY OP CANADA. [CHAP. XXI. 
 
 blocks of the fine varieties of French and Italian serpentine in Paris 
 was in 1855 from $3-00 to $5-50 the cubic foot, and that of polished 
 
 Cornish slabs from $0-60 to $0*70 the square foot. The serpentine of the Lizards 
 in Cornwall is still more esteemed, and is now extensively wrought at Pen- 
 zance ; where it is not only made into tables and chimney-pieces, but is 
 turned into vases, candlesticks, and many other articles of use and elegance. 
 In this serpentine the green color is beautifully blended with red, which is 
 often very brilliant. This material is very durable when not exposed to 
 the weather, as may be seen in tombs made of serpentine from Corn- 
 wall, more than 150 years old, in Westminster Abbey. Rain and frost 
 however slowly destroy its polish. The price of blocks of undressed 
 Cornish serpentine was stated in 1855 to be from five pounds to ten 
 pounds sterling the ton, according to its quality ; and that of polished 
 slabs an inch in thickness, from eight to twelve shillings the square foot. 
 
 Bed The Quebec group presents a red limestone associated with red shales, 
 
 near the river Guillaume, at St. Joseph on the Chaudiere. Polished slabs 
 
 st. Joseph. O f ^ig ii mes tone have a color approaching to brick-red, with dark brown 
 and black spots, apparently from imbedded pebbles, the whole traversed 
 by numerous small veins of white calc-spar. The rock is somewhat argil- 
 laceous, and does not receive a fine polish. The limestones near Phillips- 
 
 stArmand. burg in St. Armand, already mentioned (page 820), afford several 
 varieties of fine-grained marble, some of which is white, and takes a 
 good polish, although seldom very pure in tint. It is not unfrequently 
 clouded with pale greyish-green : a dove-grey variety with white spots, 
 is also mejt with here. Not far from this locality, and about a mile and a 
 half to the southeast of Phillipsburg, a very good black marble was at one 
 time quarried. The beds dip to the eastward at an angle of about twelve 
 degrees, and some of them are of considerable thickness. 
 
 The Chazy and Trenton limestones afford in many places beds of a fine 
 texture, which receive a good polish, and are capable of being employed as 
 
 caughna- marbles. At Caughnawaga some of the beds are grey, with an abundance 
 
 waga. O f sma ]i shells which are dark brown in color, and of other shells and corals 
 of a bright pink or rose-red. The stone takes a fair polish, and yields a 
 pleasing marble. The quarries in the same formation at Ste. Genevi^ve, 
 Isle Bizard, and Montreal, afford a similar stone, with red spots ; and at 
 
 st. Lin. St. Lin the whole rock becomes of a dull red color, in which the fossils 
 appear of a brighter red tint. The limestone of the same formation at 
 
 st. Domi- St. Dominique is of a dove-grey, with spots or clouds of white. It is solid, 
 easily wrought, and takes an extremely fine polish. Similar beds belong- 
 ing to this formation on Esquimaux Island, in the Mingan group, would 
 yield abundance of fine-grained drab colored marble. 
 
 The black strata of the lower part of the Trenton group, already men- 
 tioned, afford in many 'places a good black marble. Two beds, each of 
 
CHAP. XXL] MARBLES. 827 
 
 about two feet in thickness, are found at Cornwall and at Pointe Claire, the Cornwall, 
 lower one of which is the better fitted for cutting and polishing. The black 
 marble of Pointe Claire has often a brownish or greenish hue when polished. 
 Near the same geological horizon, in the township of Pakenham, a choco- Pakenham. 
 late-brown or wood-brown limestone occurs, which is fine grained, and takes 
 a good polish. It occasionally contains fragments of chert, which renders 
 it necessary to employ care in the selection of the stone. A mill was at 
 one time established in the vicinity, for the purpose of working this brown 
 marble. Grey beds of the Chazy formation, thickly marked by small 
 bivalve shells filled with white calc-spar, have been wrought to a small 
 extent near L'Orignal ; but the stone is not well fitted for a marble, inas- 
 much as the shells are readily detached from the rock. The parti- 
 colored limestone beds found in Seymour (page 187), and at the base of 
 the Trenton outliers in Marmora, and in Madoc, yield a fine-grained grey 
 marble thickly mottled with red and yellow colors. 
 
 The grey limestones, both of the Chazy and Trenton formations, from Montreal, 
 the vicinity of Montreal, are sometimes cut and polished as marbles. They 
 are however of a dull grey color, and take but an indifferent polish. 
 Similar material has also been obtained from Terrebonne and from Glou- 
 cester. The marbles of Caughnawaga, St. Lin, St. Dominique, and St. 
 Armand are much better fitted for the ordinary purposes of decoration ; 
 and as they are abundant and easily wrought, they might be furnished 
 at prices which would lead to their general adoption. 
 
 In Dudswell, on the twenty-second lot of the seventh range, the beds Dudsweii. 
 of the somewhat altered limestones, probably of Devonian age, afford a 
 great variety of marbles. Some of these are cream colored, with ochre- 
 yellow veins ; others present a kind of breccia of dark grey and yellow 
 colors ; and others still are black. In some specimens obtained from this 
 locality, a nearly black ground is traversed by veins of an ochre-yellow, 
 giving rise to a variety strongly resembling the Portor marble from 
 northern Italy, which is commonly known as black and gold. -A more 
 detailed description, with analyses of these limestones, is given on page 
 617. They have never yet been wrought; but it appears probable, from 
 the trials which have been made by the Survey upon a few blocks from 
 this locality, that it may furnish several fine varieties of colored marble. 
 
 FLAGSTONES. 
 
 Many of the stratified rocks already mentioned under the head of build- 
 ing stones and marbles afford thin beds which are well fitted for floors, 
 hearths, sidewalks, and street-crossings. As yet however but little atten- 
 tion has been given to these materials in Canada. Brick and wood are 
 very generally used in our towns ; and in some cases flagging-stones have 
 been imported from the state of New York, and even from Great Britain, 
 
828 GEOLOGY OF CANADA. [CHAP. XXL 
 
 Flagstones, although abundance of good material of the kind may be found in various 
 Laurentian P ar ^ s f ^ ne province. The more micaceous parts of the Laurentian gneiss 
 gneiss. afford in various localities thin beds adapted for paving. Such may be 
 found in Horton and Clarendon on the Ottawa, and in Bagot at Calabogie 
 Falls on the Madawaska. In ascending Lake Temiscaming, about seven 
 miles above the Galere, the cliffs, which extend for about five miles on the 
 right-hand side, present great quantities of thin even-bedded micaceous 
 gneiss, which would yield good flagstones of large sizes. Jn many places 
 along the north side of the Ottawa, and of the St. Lawrence, similar stones, 
 two or three inches in thickness, and of large size, may be obtained. 
 Among other localities may be mentioned the flank of the hills between 
 the Batiscan and Charest Rivers, and a similar rock at the St. Joachim 
 Falls on the Ste. Anne (Montmorenci). 
 
 Among the crystalline rocks of the Eastern Townships, the mica slates 
 sutton. of Sutton Mountain will doubtless afford, in some parts, good flagstones. They 
 are seen in several places along the south road across the mountain, espe- 
 cially on the nineteenth lot of the second range of Sutton. It is probable 
 that farther research in this region will discover other localities. On the 
 fifth lot of the second range of Inverness, is a band of greyish-green tal- 
 coid silicious slate, which has been quarried to a small extent. It splits 
 with facility into very even slabs of three inches in thickness, which may 
 be obtained as large as seven by four feet. The higher rocks on the west 
 Memphra- side of Memphramagog Lake, at Potton Ferry, and on the east side for 
 magog ' some miles above the Outlet, afford beds of a greyish-brown somewhat cal- 
 careous sandstone, which splits readily into slabs, some of them as thin as 
 two inches. These may be obtained of almost any required size, up to six 
 feet by three, and often ten feet by five. The slabs are very regular in 
 thickness, but their surfaces are somewhat rough, and would require a 
 little dressing. Great quantities of these stones might be easily obtained 
 Dudsweii. along the lake shore. In the township of Dudswell, on the sixth range, 
 to the east of the Quebec road, is a series of thin grey limestone beds, 
 which might be employed for flagging. The rock, which is crystalline, 
 separates readily into plates of two or three inches thick, which receive a 
 polish, and are used in the vicinity for tombstones. Similar beds may be 
 looked for in other parts of the distribution of these limestones. 
 
 On both sides of the Riviere du Loup for some miles above its junction 
 with the Chaudiere, beds of fine-grained dark bluish-grey sandstones are 
 met with, some of which divide with the bedding into layers sufficiently 
 thin for roofing slates ; while others would yield excellent flagstones, which 
 may be obtained five or six feet long, by two or three feet wide, and not 
 more than an inch in thickness. Similar flagstones and slates are met 
 with on the eighteenth lot of the third range of Tring, and the twenty- 
 ninth lot of the fifth range of Brompton. The rocks of the Gaspe* series 
 furnish in many places thin-bedded sandstones fitted for flagging. 
 
CHAP. XXI.] FLAGSTONES. 829 
 
 The Potsdam formation in many parts of its outcrop yields thin-bedded Potsdam 
 sandstones, which are generally very hard and strong, and well fitted for sa 
 flagging. On the twelfth lot of the ninth range of Storrington, the beds stoning- 
 in a bank by the roadside are very regular, and some of them would 
 furnish slabs of a large size, and from one to two inches in thickness. Simi- 
 lar thin beds of this sandstone are found at Grindstone Point at the north 
 end of Knowlton Lake, and also on Eel Lake in an outlying portion of 
 the formation on the eleventh lot of the ninth range of Loughborough. In 
 Hemmingford, on the eighteenth lot of the second range, to the east of Hemming- 
 Covey Hill, the same sandstone presents beds of from two to four inches, or ' 
 which are fit for nagging. To the west of the same hill, on the Outarde 
 River, are also thin layers of sandstone ; interstratified however with thick 
 massive beds. Flagstones of from one to three inches in thickness may 
 be obtained here ; but the stone is brittle, and apt to break into irregular 
 shapes. It is inferior to that from Malone in New York, which is much 
 esteemed for flagging purposes, and is imported into Canada. It may be 
 expected that beds of sandstone equal to those of Malone may yet be 
 found in that vicinity. 
 
 On the Naquareau River, just below Mr. Dorwin's saw-mill, and near Kawdon. 
 the southeast limit of Rawdon, about four feet of white sandstone belong- 
 ing to the Potsdam formation appear well fitted for flagging. The stone 
 divides into layers of two or three inches, and slabs of large size could 
 probably be obtained. In the same formation, on Cote Ste. Catherine, in 
 the parish of St. Cuthbert, about four and a half feet of similar sandstones St. cutn- 
 are met with. They are quarried for use in the vicinity, and slabs two or bert ' 
 three niches in thickness may be obtained seven feet in length by three or 
 four in breadth. The sandstone at the Gres, on the St. Maurice, already 
 mentioned as furnishing materials for furnace linings, and for building pur- 
 poses, (page 799,) presents a thickness of about eleven feet of thin white 
 beds fit for flagging. 
 
 The limestone of the Trenton group furnishes in a great many places Trenton 
 thin beds, which are extensively used for flagging and paving in many of Iune8tone - 
 the towns along the line of its distribution. At Cap Santd, regular calca- cap sante. 
 reous beds, two or three inches in thickness, are interstratified with the 
 black shales of the Utica formation, and are used in the vicinity for hearths, 
 window-sills, and similar purposes, but are traversed by joints which ren- 
 der them liable to break. These beds are well exposed at Pointe a 1'Abri. 
 The thinner beds of the calcareous sandstone of Murray Bay (page 819) 
 would probably furnish a good material for flagstones. 
 
 In Western Canada the Hudson River group furnishes thin-bedded 
 sandstones fitted for flagging, which are exposed on the banks of the 
 rivers falling into Lake Ontario in the vicinity of Toronto, and in other Toronto, 
 parts of its distribution farther west. The grey band of the Clinton for- 
 
830 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 mation (page 316) affords along its outcrop thin beds of sandstone, which 
 are well fitted for flagging, and are extensively used for that purpose in 
 Toronto and in Hamilton. 
 
 ROOFING SLATES. 
 
 Argillite. 
 
 The complete absence from the rocks of the Laurentian series of any- 
 thing like argillite or clay slate, has already been mentioned. The Huron- 
 ian rocks however occasionally present strata approaching to argillite in 
 character, but seldom fitted for the purpose of roofing slates. Specimens, 
 said to be found about five miles up the Montreal River, a tributary of 
 Lake Temiscaming, are firm and strong, but are more than a quarter of an 
 inch in thickness, and do not seem capable of being split thinner. Among 
 the Upper Copper-bearing rocks of Lake Superior are argillites, which 
 may in some cases be fit for roofing slates. Examples of these are seen 
 on the Kamanistiquia ; and the Slate Islands and Ance a la Bouteille are 
 said to afford roofing slates. 
 
 Among the rocks of the Quebec group in Eastern Canada, argillites fit 
 for this purpose are met with in a great many places, and have been suc- 
 cessfully wrought. The Walton slate quarry, on the twenty-second lot of 
 Melbourne, the sixth range of Melbourne, has been opened within the last three years. 
 The band of slate, which is here in contact with a bed of serpentine, has 
 a breadth of about one third of a mile, and dips to the southeast at an 
 angle of 80. It is so exposed as to offer facilities for extensive working; 
 and within the last two years considerable quantities of these slates have 
 been brought into the Canadian market, where they are likely to replace 
 to a great extent the metal roofing hitherto so commonly employed. The 
 slate of Melbourne is bluish-purple in color, fine grained, and splits with 
 facility into thin plates, which have the smoothness and strength required 
 for good roofing slates, and will compare favorably with the best from 
 other countries. This slate is entirely free from carbonate of lime, and 
 does not appear to be affected by the action of the weather. In the sub- 
 joined table may be seen some of the sizes of slates obtained from this* 
 place, the number of these in a square, and the price per square deliv- 
 ered at the Richmond railway station, a mile and a half from the quarry. 
 
 Walton 
 quarry. 
 
 Inches. 
 
 Number. 
 
 Price. 
 
 Inches. 
 
 Number. 
 
 Price. 
 
 24 X 14 
 
 98 
 
 $4-25 
 
 16 X 9 
 
 246 
 
 $3-75 
 
 22 X 12 
 
 126 
 
 4-25 
 
 14 X 8 
 
 327 
 
 3.00 
 
 20 X 10 
 
 169 
 
 4-25 
 
 12 X 8 
 
 400 
 
 2.50 
 
 18 X 10 
 
 192 
 
 4-00 
 
 12 X 6 
 
 533 
 
 2.00 
 
 Cleveland. 
 
 On the sixth lot of the ninth range of Cleveland is a continuation of the' 
 slate band of Melbourne. A quarry was opened here in 1854, but was 
 afterwards abandoned ; although there seems no reason to doubt that with 
 
CHAP. XXL] ROOFING SLATES. 831 
 
 a judicious expenditure, it might be made to furnish as good slates as the 
 Walton quarry. On the fourth lot of the first range of Kingsey, roofing 
 slates occur in a band of argillite, which is associated with dolomite. 
 This locality was at one time wrought, and good slates were obtained. 
 Their color inclines to a reddish-purple, and they are not quite so hard as 
 those just mentioned. Roofing slates, resembling those of Melbourne, are 
 found on the fourteenth lot of the first range of Halifax ; and farther to 
 the northeast, in the township of Frampton. It is probable that the 
 argillites which belong to the Quebec group will furnish good roofing 
 slates in many other parts of their distribution. 
 
 On the second lot of the fifth range of Orford, there are slates which Orford. 
 are of a dark bluish color, and not unlike those of Melbourne, although less 
 smooth in their cleavage. What appears to be a continuation of these is 
 found on the twenty-ninth lot of the fifth range of Brompton. The 
 argillites from these two localities belong to the Upper Silurian series, 
 in which similar roofing slates are found in Westbury on the St. Francis 
 River. These upper rocks will probably yield slates in many other parts 
 of their distribution. Those which are associated with the flagstones in 
 Tring, and on the Riviere du Loup, have already been noticed. 
 
 X. MATERIALS FOR ORNAMENTAL PURPOSES. 
 
 Under this title may be considered certain porphyries, and other feld- 
 spathic and silicious rocks, which are capable of being employed for vases, 
 tables, inlaid work, and for various articles of ornament. The hardness of 
 these materials, and the consequent cost of cutting and polishing them, 
 prevents their employment to any great extent, and causes the preference 
 to be given in many cases to marbles and to serpentine. The latter, from 
 its softness, and from the ease with which it is cut and turned in a lathe 
 with the aid of ordinary tools, is much employed in various countries for 
 ornamental purposes. Some of the varieties of serpentine which are found 
 at Melbourne, and elsewhere in the Eastern Townships, are apparently well 
 fitted for such uses. The recent application of a variety of diamond 
 to the turning of stones in a lathe has however greatly facilitated the 
 working of these harder materials, which are now fashioned into shape at 
 a much less expense than formerly. Few countries afford more beautiful 
 or more numerous varieties of hard rocks of this kind than Canada : among 
 these are the porphyries, the labradorite, and the other opalescent feld- 
 spars about to be noticed. 
 
 The agates which are common in the amygdaloidal rocks of Lake Agates. 
 Superior, and are abundant in the form of pebbles along the shores of 
 Thunder Bay, and of Michipicoten and St. Ignace Islands, admit of being 
 
832 GEOLOGY OP CANADA. [CHAP. XXL 
 
 cut for ornaments. They are often of considerable size, and exhibit a fine 
 variety of colors. The agates which are found in the conglomerates of 
 the Bonaventure formation (page 404) are scattered abundantly along the 
 coast where this rock prevails, and are known by the name of Gaspe' peb- 
 bles. They are of small size, but are often of fine colors, and admit of a 
 good polish. Agates however are very common in many countries, and, 
 unless of considerable size and perfection, they have but little value. 
 Gems. Canada has as yet afforded but few gems. The zircons or hyacinths 
 
 in the Laurentian limestones at Grenville are occasionally transparent, 
 and have a fine color ; and the presence of small portions of red and blue 
 varieties of corundum in these same limestones in Burgess may also be 
 noticed. This mineral constitutes the gems known as sapphire and ruby ; 
 and it is worthy of remark, that the sapphire of Ceylon is found, with 
 chondrodite, in similar crystalline limestones. The transparent green 
 garnet of Orford, which owes its color to oxyd of chrome, has hitherto 
 been met with only in small crystals ; but if found of large size, it would 
 constitute a gem as beautiful as the emerald. Amethysts abound in 
 some parts on the coast of Lake Superior ; but the specimens hitherto 
 brought from that region haye seldom been sufficiently fine in color for 
 the jeweller's use. The so-called Quebec diamonds, which are sometimes 
 cut and polished for ornaments, are nothing more than rock crystal. 
 
 PORPHYRIES AND FELDSPARS. 
 
 The dykes of quartziferous porphyry which cut the intrusive syenite of 
 Grenville, have been described on page 39, and again on page 654. This 
 rock consists of an extremely hard fine-grained base, which in different 
 specimens varies from dark green to red, purple, dark grey, and various 
 shades of black. In this base are imbedded grains or crystals of rose- 
 Porphyry, red or flesh-red feldspar, sometimes accompanied by grains of quartz. A 
 fine example of a brownish-black porphyry, with well defined crystals of 
 red feldspar, occurs on the south side of the road between the seventh and 
 eighth ranges on the eighth lot of Chatham. The dyke has a breadth of 
 about twenty feet, and runs nearly east and west. On the fourth lot of 
 Grenville. the sixth range of Grenville, there is a great mass of this porphyry, which 
 varies in color from leek-green to blackish-green, and is marked with small 
 red, brown, and black spots. It is very compact, and has a conchoidal 
 fracture. This green porphyry is here about fifty feet in breadth ; and to 
 the northward it passes into a chocolate-brown variety, which is still more 
 abundant. Small specimens of several varieties of these porphyries have 
 been cut, all of which receive a fine polish, and are very beautiful. They 
 may be obtained in large blocks, and do not appear to be much harder than 
 the granites of Aberdeen, and of other regions, which are now cut and 
 polished on a great scale ; while they would far surpass these rocks in beauty. 
 
CHAP. XXI.] ORNAMENTAL STONES. 833 
 
 A beautiful variety of albite, which is described on page 477, occurs on 
 the nineteenth lot of the ninth range of Bathurst, where it is found in 
 veins cutting the Laurentian strata, and has been called peristerite. It is reristento. 
 white or pearl-grey in color, and shows a beautiful blue opalescence, min- 
 gled with pale green and with yellow. Large masses of this feldspar 
 are without any admixture ; but in other portions of the vein, it is 
 mingled with a little quartz, forming a kind of graphic granite. Specimens 
 of this rock, when cut and polished, are very ornamental. A locality of 
 a similar feldspar in Dummer has been described on page 36. 
 
 The name of perthite was given to a reddish variety of orthoclase, Fertute. 
 described on page 474, which forms with quartz a coarse grained granite on 
 the third lot of the sixth range of Burgess. This feldspar is barred with 
 flesh-red and brownish-red colors, and shines with golden or copper-red 
 reflections, like the sun-stone or aventurine. Cut surfaces of it several 
 inches square have been obtained, which when polished are very beauti- 
 ful. This mineral, like the peristerite, was brought into notice by Dr. 
 James Wilson of Perth. 
 
 The labradorite or labrador-feldspar, so called from the region from Labradorite. 
 which it was first brought, is sometimes beautifully opalescent, and exhibits, 
 especially when polished, reflections of blue, green, gold, and purple colors. 
 The geological distribution and the composition of a class of rocks made 
 up chiefly of this, and of similar anorthic feldspars, have been given on 
 pages 33, 480, and 588. Besides the locality mentioned by Dr. Bigsby on 
 Lake Huron, the only spot in which the opalescent labradorite has been 
 seen in place, in Canada, is at Cap Mahue in the tenth range of Aber- 
 crombie. Here, in a fine grained lavender-blue labradorite rock are imbed- 
 ded cleavable masses of the feldspar, sometimes several inches in diameter, 
 and exhibiting blue, golden-green, and bronze-green reflections. The 
 rolled masses of anorthosite or labradorite rocks which are common along 
 the shores of the Ottawa, especially in the vicinity of Grenville, often con- 
 tain small portions of the opalescent feldspar. The mass of the rock 
 receives a high polish, and presents a clouded dark greyish-green ground, 
 with spots of an opalescent blue, forming an ornamental stone which may 
 be applied to the same uses as the polished porphyries and granites. It 
 is somewhat inferior to these in hardness, and would therefore present 
 less difficulty in the working. Large blocks of this material may readily 
 be procured. The syenites and many of the varieties of granitoid gneiss 
 from the Laurentian series are well adapted for cutting and polishing. A 
 peculiar fine grained reddish gneiss, which is traversed by veins of a pea- 
 green epidote, and is very ornamental when polished, occurs near Carleton 
 Place in Ramsay, and at the Falls of the Mingan River, as described on 
 page 37. In this connection may be mentioned a fine grained mixture of 
 pale green epidote with quartz, which is found on the Matanne River, Epidote. 
 
834 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXI. 
 
 and is described on page 497. This rock, which forms great masses in 
 the Shickshock Mountains, is very hard ; and as it receives a fine polish and 
 has a bright yellowish-green color, it might be used as an ornamental stone. 
 
 Sherbrooke. 
 
 Riviere 
 Ouolle. 
 
 Lake 
 Huron. 
 
 A bed of jasper occurs in the town of Sherbrooke, and is traced for a 
 considerable distance, having in some parts a breadth of six feet. Its color 
 is blood-red, and it includes small grains of red hematite, and occasionally 
 passes into a jaspery iron ore. In the parts exposed, this jasper does not 
 appear to be sufficiently compact to be wrought for ornamental purposes. 
 A small bed of jasper occurs imbedded in the red shales at Riviere Ouelle. 
 Its colors are dark green and reddish-brown, and it is penetrated by small 
 veins of white chalcedony. This jasper is compact and uniform in its 
 texture, and receives a good polish. In some parts, the reddish-brown base 
 is marked by clouds of a brilliant red. The jasper conglomerate of the 
 Huronian series, which has been described on page 57, consists of pebbles, 
 chiefly of red jasper, imbedded in a base of white or greenish-white quartz- 
 ite. The jasper is fine in texture, and often brilliant in color, and the 
 whole rock is extremely solid, and receives a polish which makes it well 
 fitted for ornamental purposes. Great beds of this jasper conglomerate 
 are met with on the north shore of Lake Huron ; where rounded masses of it, 
 often of large size, are also found. These are abundant at the Bruce Mines. 
 
 XII. LITHOGRAPHIC STONE. 
 
 Lithographic 
 stone. 
 
 Marmora. 
 
 A very fine grained and compact limestone is required for the purposes 
 of lithography, and beds having these characters are found in the Birdseye 
 and Black River formation at the base of the Trenton group throughout 
 a considerable part of its distribution, from Hungerford to Kama on Lake 
 Couchiching. In the township of Marmora, as described on page 182, 
 there is a section of about twenty feet of light grey limestone, which is 
 compact, with a conchoidal fracture, and holds no organic remains. Some 
 of the beds contain numerous small lenticular crystals of calc-spar, and are 
 marked by crystallites like those described on page 632. There is how- 
 ever a bed of two feet in thickness, which is extremely fine in its grain, 
 and yields a lithographic stone of excellent quality. It has been repeat- 
 edly tried by lithographers, both in Canada and England, with most satis- 
 factory results ; but owing to the remoteness of the locality, no attempt has 
 hitherto been made to work the stone. It is probable that equally good 
 material for the purpose may be found in other parts of this band, which, 
 as already mentioned, may be traced for about a hundred miles. 
 
CHAP. XXL] LITHOGRAPHIC STONE. 835 
 
 Beds of a fine grained yellowish-grey stone, well fitted for lithographic 
 purposes, have lately been found among the dolomites of the Onondaga for- 
 mation in the township of Brant. They occur in the bed of a small stream Brant, 
 about half a mile south of Walkerton, where several strata of the stone from 
 two to eleven inches in thickness occur in a section of fifteen feet. The 
 beds at this place are traversed by natural joints, which cause the rock 
 to divide into somewhat narrow portions ; but the stone is found to be well 
 adapted for lithography, and larger slabs may probably be found elsewhere 
 in the same formation. Equally good specimens of it were obtained from 
 the Oxbow on the Saugeen River, on the third lot of the seventh range of 
 Brant. The stone from this formation, being magnesian, is attacked by 
 acids more gently and with less effervescence than ordinary limestone. 
 This peculiarity in the action of acids, which are employed in the lithographic 
 process, is said to be an advantage. 
 
836 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 CHAPTER XXII. 
 
 SUPPLEMENTARY. 
 
 SERIES;' DISTRIBUTION OF LIMESTONES; ANORTHOSITES; THEIR APPARENT 
 FORMABILITY ; DOLERITE DYKES. HURONI AN SERIES; ITS FARTHER DISTRIBUTION. 
 QUEBEC GROUP ; ITS DISTRIBUTION NEAR PHILLIPSBURGH ; ROCKS OF STANBRIDGE ; or 
 SWANTON ; POTSDAM GROUP ; ST. ALBAN'S. CONGLOMERATES OF POINT LEVIS ; THEIR 
 ARRANGEMENT AND THEIR ORGANIC REMAINS. ROCKS OF THE STRAITS OF BELLE IgLE AND 
 OF NEWFOUNDLAND. GASPE SERIES. SUPERFICIAL GEOLOGY; ROUNDED ROCKS AND ICE 
 GROOVES; BOULDER FORMATION AND ERRATIC BLOCKS; ERIE AND SAUGEEN CLAYS; 
 ALGOMA SAND; ARTEMISIA GRAVEL; ANCIENT BEACHES, TERRACES, AND RIDGES; LOCAL 
 DEPOSITS OF FRESH-WATER SANDS; STRATIFIED CLAYS AND SANDS OF EASTERN CANADA ; 
 SUPERFICIAL GEOLOGY OF MONTREAL ISLAND. LIST OF FOSSILS. AURIFEROUS DRIFT; 
 MIOCENE OF VERMONT. RECENT DEPOSITS. 
 
 In the preceding chapter is included all the information collected by 
 the Survey, on the subject of Economic Geology, up to the termination of 
 1862 ; but in the first sixteen chapters of the Report, comprehending the 
 General Geology, the description of the various rock formations and of 
 their distribution through the province has been brought only to the end of 
 1861. It is proposed in the present chapter, to introduce such additions 
 and modifications as are authorized by the field explorations of last season ; 
 to be followed by a general account of the facts ascertained from the com- 
 mencement of the Survey in regard to the Drift. In giving this additional 
 matter, the various rock formations will be considered in the order observed 
 in the previous portion of the work. 
 
 LAURENTIAN SERIES. 
 
 The additional information respecting the Laurentian series is confined 
 
 to the area represented on the map ; which shows the distribution of the 
 
 Limestones, crystalline limestones in the counties of Ottawa, Argenteuil, Montcalm, 
 
 Grenviiie and Two Mountains. On page 43, it is stated that the Grenville band had 
 
 band. been, traced in all its windings from Lachute to the seigniory of the Petite 
 
 Nation. It has now been farther traced nearly across this seigniory in 
 
 additional undulations. Starting from the exposures which have been 
 
 followed northward through the Augmentation of Grenville to the middle 
 
 of Harrington on the Riviere Rouge, it sweeps round to the southern 
 
 extremity of Lake Papineau. It thence proceeds northward, on the east 
 
CHAP. XXII.] LAURENTIAN SERIES. 837 
 
 side of this lake, to the upper end, and turning in Ponsonby, runs south- 
 ward on the west side, and follows the river Kinonge* (discharging the Petite Nation, 
 lake) to its mouth on the Ottawa. It appears to follow the Ottawa to Papi- 
 neauville, partially covered over by the Silurian deposits on the south side 
 of the river ; and then again proceeds northward by C6te Ste. Julie, which 
 is about as far as it has been traced. In the Augmentation of Grenville, 
 on Papineau Lake, and on the Kinong, the limestone appears to be divided 
 into two parts by a band of gneiss, which makes a considerable display in 
 the first named locality, but which from Papineauville to C6te Ste. Julie 
 has not yet been observed. A similar dividing mass of gneiss is observed 
 at intervals in that part of the Grenville limestone which runs across the 
 first three ranges of Harrington, on the east side of the township ; but 
 it did not here seem to be of sufficient importance to be indicated as a 
 separate feature on the map. 
 
 A band of limestone has been traced on the Maskinonge* River, across 
 four of the ranges of Ponsonby ; and though it approaches somewhat near Poneonby. 
 to the Grenville band, at the head of Papineau Lake, it is supposed to be 
 distinct from it, and to be a continuation of the Green Lake band (4 of 
 the section on page 45), its probable connection with which is indicated 
 by a dotted line on the map. This relation however has yet to be verified 
 by observation. 
 
 It has been stated on page 43 that the Laurentian strata in the area in 
 question, are affected by two sets of undulations, the axes of the more Undulations, 
 important running north and south. What appeared to be one of the most 
 prominent of these was given as starting in Chatham from the intrusive 
 syenite observed there, and gaining a position toward the west side of 
 Howard. When this was stated, there were indications which seemed to 
 render it probable that the Grenville band of limestone, where it runs 
 northeast from the north end of Lake Louisa, would be traceable north- 
 ward through Wentworth, and establish an anticlinal between the limestones 
 of Harrington and those of Morin. After much exploration, we have not 
 succeeded in tracing the band in the direction expected. It appears rather 
 to return along the north edge of the lake, and to join the limestone on the 
 east side of the Harrington trough, in the second range of Wentworth. 
 This distribution would materially alter the supposed relations of the Morin Morin 
 and Grenville bands. The former could not then be considered as superior Iune8tone - 
 to the latter, but as either its equivalent, or inferior to it. In the former 
 case, there would still be a prominent anticlinal between the Harrington 
 and Morin bands ; but in the latter case, the Morin limestone running under 
 that of Harrington, the prominent anticlinal will disappear. 
 
 Although the dips of the strata in this whole region are of very little 
 avail in establishing the sequence of the deposits, yet the preponderance 
 of such evidence as they in this instance afford, would rather favor the 
 
838 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXII,. 
 
 Anortiio- 
 sites. 
 
 supposition that the Morin band is inferior to that of Grenville. The Morin 
 band, in that part of its distribution which approaches St. Jerome, is 
 flanked on either side by an interstratification of orthoclase gneiss with a 
 pyroxenic anorthosite ; and as it there approaches the great area of anor- 
 thosite which occurs to the east, this interstratification of beds of the 
 two rocks was considered as indicating a passage from the orthoclase gneiss 
 of Grenville to the anorthosites of Morin, Abercrombie, Rawdon, and 
 Chertsey. But by placing the limestone band of Morin beneath that of 
 Grenville, the orthoclase gneiss of Grenville will intervene stratigraphically 
 between the beds at St. Jerome and the anorthosites to the east (which 
 are still considered newer rocks), and will interrupt the passage. In this 
 position, the Morin band would correspond with that of the Lake of Three 
 Mountains and of Green Lake in Clyde, and with that of Great Beaver 
 Lake and Lake Sam ; the latter lake being on the west line of the township 
 of Grandison. In other parts of its distribution no anorthic feldspars have 
 been observed to be associated with the band, except at the Lake of Three 
 Mountains ; where in addition to the mass of albitic rock supposed to be a 
 vein (page 36), the gneiss bounding the limestone on the east side contains 
 an admixture of a white anorthic feldspar, which may be oligoclase or 
 albite. This gneiss, which contains at the same time orthoclase and quartz, 
 is however very distinct from the anorthosite rock of St. Jerome ; and if 
 it be regarded as its stratigraphical equivalent, it would be necessary to 
 suppose such a Variation in the composition of the original deposits of the 
 two localities, as is not unfrequent in other sedimentary strata. 
 
 From Lake Sam and the Trembling Lake, the two limestone bands 
 (4 and 2 of the section on page 45) which underlie the Grenville band ? 
 have been traced southward through the township of Desalaberry, folding 
 in succession upon an anticlinal axis, and returning northward to the sixth 
 and eighth ranges respectively. The higher of the two bands however, 
 in the sixth, seventh, and eighth ranges, and a little farther northward on 
 labradorite. the west side of the anticlinal, is interrupted by a mass of anorthosite or 
 labradorite rock, which apparently covers it up. A similar phenomenon 
 appears to occur in Morin, where the limit of the labradorite rock described 
 on page 33, starting from the southwest boundary of Abercrombie, and 
 running across the north corner of Mille lies, immediately flanks the 
 limestone band on the north. On entering Morin, it is separated from the 
 limestone, in the first and second ranges, by a considerable mass of brown- 
 weathering gneiss. The margin of the labradorite approaches the lime- 
 stone band again hi the third range, and this band is concealed in its farther 
 progress westward. Thence the margin crosses the southeast corner of 
 Howard, enters Wentworth for a short distance, and returns to Howard ; 
 which it traverses northward, obliquely crossing the line between it and 
 Montcalm, and then the line between Montcalm and Wolfe, about two miles 
 
 Overlying 
 
 Howard. 
 
CHAP. XXII.] LAURENTIAN SERIES. 839 
 
 west of Beresford. From this it is said to gain the northeast line of Wolfe, 
 not far from Grandison. From the interruption by it of the Morin limestone 
 near Howard, it seems probable that the anorthosite rock overlies the whole 
 Grenville series unconformably, and that the mass of it on the west side of 
 Desalaberry is an outlying portion. If on exploration to the eastward 
 of the Trembling Mountain, it should be farther ascertained that the two 
 inferior limestone bands of the Grenville series disappear on reaching the 
 margin of the anorthbsite, it may be considered as conclusive evidence of 
 the existence in the Laurentian system of two immense sedimentary for- TWO forma- 
 mations, the one superimposed unconformably on the other, with probably tl( 
 a great difference in time between them ; and it will be an interesting 
 subject of inquiry whether the intrusive rocks which have been found 
 intersecting the lower division, give any clue to events which may have 
 happened in the interval. 
 
 Should it be established that the great mass of anorthosite feldspar rocks 
 really belongs to a distinct and more recent formation than the immense 
 series of orthoclase gneiss beneath, it would be in strict conformity with 
 the principle laid down on page 573. According to this, the proportion of 
 alkalies to the alumina in silico-aluminous rocks will, other things being 
 equal, be greater in the older sediments ; and the group of rocks in which 
 the alumina is combined with potash and soda, almost to the exclusion of 
 other bases, would seem to belong to a far earlier period than that giving 
 rise to rocks in which a large proportion of these alkalies is replaced by 
 lime. This newer formation, although characterized by a predominance 
 of anorthosites, appears to contain in some parts, interstratified beds of 
 orthoclase- gneiss, quartzites, and limestones, all of which are found asso- 
 ciated with it near New Glasgow. 
 
 Some of the dolerite dykes among the intrusive masses have during the Doierite 
 past season been traced to much greater distances than stated in the dykes * 
 previous part of the Report. Taking them in the order in which they are 
 given on page 38, it will be seen by the map that the one on the thirteenth 
 lot of the fourth range of Grenville has now been traced as far as the fifth 
 lot of the second range of the Augmentation of Grenville, a distance of 
 six and a half miles ; in the course of which it sweeps down toward the 
 mouth of the Rouge, and touches the north side of the Ottawa. On the 
 most western lot to which it has been followed in the Augmentation, it 
 appears to join another dyke, which is probably a branch having a more 
 direct course from the lot in Grenville already mentioned. Eastwardly, 
 after running about a mile, the dolerite, as stated on page 38, is cut off by 
 the syenite ; but it occurs again in three of the bays indenting the south 
 side of the syenite, in the intervals between which it is interrupted and 
 destroyed by this newer intrusive rock. It continues beyond the syenite, 
 and is seen on the line between the seventh and eighth lots, and between 
 
840 
 
 GEOLOGY OF CANADA, 
 
 [CHAP. XXII. 
 
 Chatham. 
 
 Grenville. 
 
 Wentworth. 
 
 the seventh and eighth ranges of Chatham. It is farther seen in Argen- 
 teuil, about three miles beyond the east boundary of Chatham, on the 
 right bank of the North River ; the whole distance which it has now been 
 traced being upwards of twenty miles. 
 
 The dyke occurring on the eleventh lot of the fifth range of Grenville 
 to the west of the syenite, is probably to be identified with one to the 
 east of this intrusive mass, on the tenth and eleventh lots of the eighth 
 range of Chatham, which answers better for the dyke mentioned on page 
 39, than the more southern one there assigned to it. To the westward, it 
 has now been followed to the west boundary of the Augmentation of Gren- 
 ville, near the line between the third and fourth ranges. It is accompanied 
 by a parallel dyke, seen at intervals, about a quarter of a mile to the north 
 of it. The two probably come together on the twenty-fifth lot of the fifth 
 range of Grenville ; but they separate again after the distance of a lot, and 
 remain distinct to the line between the Augmentation and the seigniory of 
 the Petite Nation. The distance between the east and west points to which 
 this dyke has been thus traced, would be about twenty-four miles ; but a 
 dyke occurs four or five miles farther on, which has been traced at inter- 
 vals for about seven miles, through COte Ezilda to C6te St. Joseph of the 
 seigniory. To the north and south of it, in this vicinity, other nearly 
 parallel dykes occur ; and the whole of these will probably be found to have 
 some reticulating relation to the two ranges of dykes already mentioned. 
 
 The great dyke of Wentworth (page 38), from the point where it is 
 intersected by the syenite on the twenty-second lot of the first range of this 
 township, has now been traced westward to the western boundary of the 
 Petite Nation seigniory in C6te St. Andre*, a distance of thirty miles ; and 
 eastwardly, about seventeen miles, to C6te St. Eustache of Mille lies. The 
 whole distance which it has been followed is thus about forty-seven miles, 
 but it probably ranges very much farther in both directions. Its width in 
 C6te St. Eustache is about 230 yards ; and as there are about five miles 
 between this and the sixth lot of the fourth range of Chatham Gore, in 
 which the details regarding it are but imperfectly known, it may be found 
 that in swelling to this increased measure, it has been joined by some 
 important but undiscovered dyke. Between the twenty-fourth lot of the 
 ninth range of Grenville and the fifth lot of the sixth range of the Aug- 
 mentation, there are about four miles in which the details of the dyke 
 have still to be made out. In its whole course, the bearing of this main 
 dyke is about five degrees south of west and north of east. The dykes 
 to the south of it are nearly parallel with this ; but on the whole, they 
 probably converge toward it westwardly. 
 
 Small exposures of similar dykes have been met with in several places, 
 but the only additional instances worthy of mention are two : one of them 
 running from the sixth range of Harrington to the eighth of Wentworth ; 
 
CHAP. XXII.] HURONIAK SERIES. 841 
 
 and another near the north line of the former township, running from the 
 twelfth to the twenty-third lot : only the extremes of this however have 
 been observed. Both of these dykes run nearly parallel with the main 
 one already mentioned* 
 
 HURONIAN SERIES. 
 
 It was stated on pages 61 and 62 that between the St. Mary and Mis- 
 sissagui Rivers the rocks of the Huronian series are arranged in the form 
 of a trough^ the longitudinal axis of which runs along the valley of the 
 Thessalon ; and that a flat anticlinal arch appears to separate this trough Thessaien. 
 from another to the eastward of the Mississagui. It was further stated 
 that a band of limestone (belonging to the division 5 of the Huronian 
 series, given on page 56), which had been met with on the Little White 
 River, about five miles above its junction with the Mississagui, probably 
 constituted a part of the western outcrop of this eastward trough, but that 
 this band had then still to be traced around it. 
 
 The work of the past season, in connection with the Huronian rocks, 
 has been' devoted chiefly to the investigation of their distribution in the sup- 
 posed synclinal area in question. The band of limestone on the Little White Limestone. 
 River, sweeping round on either hand from the position where it crosses 
 it, trends at some distance from the opposite sides of the river toward the 
 Mississagui, leaving on its tributary a peninsular-shaped area of the lower 
 slate conglomerate, 4 of the section mentioned above ; but as the band of 
 limestone approaches the valley of the main stream, it becomes lost under 
 the drift, and has not again been seen either up or down the Mississagui. 
 The strike of the lower slate conglomerate 4, however leads to the sup* 
 position that in the downward bearing of the Mississagui the limestone 
 attains the valley of the Marsh River ; and that following this in a south- 
 easterly direction across the township of Thompson, and for five miles 
 beyond, it then turns upon a synclinal axis, and reaches the Lake of the 
 Mountains, on the Blind River. The upward course of this stream gradu- 
 ally diverges from that of the Marsh River, of which it is a tributary, and 
 the limestone is traceable up its valley by various exposures for about nine 
 miles, to the neighborhood of Lake Macomang. Running about a mile 
 inland, parallel with the southwest side of this lake, it comes upon its 
 shore, and is seen on the northeast side, at the narrows, about four miles 
 from the foot of the lake. Beyond this, it probably turns a little westward 
 of north, but it has not been farther traced. 
 
 In the upward bearing of the Mississagui, above the mouth of the Little 
 White River, the course of the upper slate conglomerate, 6 of the Huro- 
 nian series, indicates that the limestone probably crosses the main stream 
 about four miles above its tributary ; that it traverses it again about six 
 
842 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 miles farther up, and that turning eastward of north, with a change in the 
 course of the river, it crosses Salter's base line, near the western extremity 
 of Lake Katigamaigouska. Here large loose angular slabs of limestone 
 are mingled with others of a slate so like the limestone in aspect and hard- 
 ness, that without the aid of an acid it would be difficult to distinguish the 
 one from the other. Neither of these rocks were seen in place, but it is 
 probable that the parent beds of both were not far distant. Two miles 
 beyond this point the Huronian rocks are interrupted by hills of granite. 
 
 Katigamai- Lake Katigamaigouska appears to lie wholly in the upper slate conglom- 
 erates 6, with the exception of the most northeastern bay, which pre- 
 sents the base of the red quartzites 7 ; while Lake Wahcomatagaming, 
 which receives the water of the previous lake, shows the upper slate con- 
 glomerates 6, on its west side, and the red quartzites 7, on its south 
 and east sides ; with the exception of its most eastern bay, where the base 
 of the red jasper conglomerates 8, is exposed. A peninsula, extending lon- 
 
 wahcoma- gitudinally from the western extremity, divides Lake Wahcomatagaming 
 into two parts. The eastern three fourths of this peninsula, presenting a 
 rugged surface, are composed of the red quartzites 7, which here display 
 a band of purple slates at their base. At the summit of the upper slate 
 conglomerate 6, as was remarked in other parts of this lake, but more 
 particularly on Lake Katigamaigouska, about 600 feet of this division 
 6, is a green flinty slate which appears to be almost destitute of peb- 
 bles. The northern shore of the lake, and the mountains north from 
 it, appear to be composed of granite and syenite ; in both of which 
 there is occasionally observable an obscure gneissoid structure, giving 
 them the aspect of gneiss, so that here, as in the valley of the Spanish River 
 (page 61), it is very difficult to say whether they are intrusive or altered 
 rocks. They are supposed however to be of Laurentian age. Striking 
 along the lake, they run parallel with the stream discharging it, and 1 come 
 upon the Mississagui about three miles above Salter's base line. On the 
 shore of Lake Wahcomatagaming, these Laurentian rocks are in contact 
 with masses of greenstone, but the relation between the two is uncertain. 
 From Lake Katigamaigouska, the base of the red quartzites 7, strikes for 
 Lake Kaikaquabick, a tributary of the Little White River ; but this stream 
 itself, as far as ascended (which was about five miles in a straight line 
 above the band of limestone) , flows over the upper slate conglomerate 6 ; 
 which is here, as on Lake Katigamaigouska, characterised at the summit 
 by green flinty slates without pebbles. 
 
 The total thickness of the strata which came under observation in the 
 area examined, may be estimated as given in the following ascending 
 series ; in which the numbers prefixed to the divisions correspond to those 
 on pages 56 and 57 : 
 
CHAP. XXII.] HURONIAN SERIES. 843 
 
 Feet. 
 
 4. Lower slate conglomerate, being only the higher part of it, 900 Section. 
 
 5. Limestone, 300 
 
 6. Upper slate conglomerate, with 600 feet at the top without pebbles, . . 2,600 
 
 7. Red quartzites, 2,000 
 
 8. Red jasper conglomerates, being only the lower part, 500 
 
 6,300 
 
 All of these divisions, with the exception of the limestone band 5, and the 
 green slates without pebbles at the top of 6, are interstratified with masses 
 of greenstone. Some of these masses in the red jasper conglomerates 8, Greenstones. 
 may be from fifty to eighty feet thick, and those in the red quartzites from 
 50 to 100 feet; while one in the upper slate conglomerates, seen on 
 Lake Macomang, was estimated at from 150 to 200 feet. A consid- 
 erable area of greenstone, associated with the lower slate conglomerates 
 of 4, occurs along the Mississagui, but it was not found practicable to 
 determine its volume, from the flatness of the country and from the nearly 
 horizontal attitude of the strata. Upon the whole, the amount of inter- 
 stratified greenstone in this region does not appear to be quite so great as 
 in the Thessalon trough. There is also less greenstone in the form of 
 dykes. Two of these however which are seen on Lake Wahcomataga- Dykes, 
 ming are respectively thirty and forty yards wide, and cross from the 
 peninsula to the east shore, converging northeastwardly. Another dyke 
 not far from the foot of Lake Macomang, is between fifty and sixty yards 
 wide, and runs nearly east and west ; while a fourth which intersects the 
 Mississagui at the third fall, in the bearing N. 65 W., is about twenty- 
 five yards wide, and appears to be accompanied by a dislocation. 
 
 Indications of copper ores were observed in several parts of the area copper ores, 
 under description. The principal of these occur at the east end of the 
 line between the townships of Patton and Thompson, in an interstratified 
 mass of greenstone, which appears to belong to the upper slate conglom- 
 erate 6. This greenstone is situated near the synclinal axis, upon which 
 the limestone band has been shown to turn near the Lake of the Mountains, 
 and it is intersected by numerous parallel quartz veins running nearly 
 east and west. Most of these contain both iron and copper pyrites ; and 
 in some of them, varying in breadth from one to five feet, the latter ore 
 occurs in quantities which render them worthy of trial. A mass of green- 
 stone belonging to the same slate conglomerates of 6, but not far above 
 the limestone band 5, occurs on a small island in the west bay of Lake 
 Macomang, in front of the position where the limestone is exposed on the 
 northeast shore. The greenstone is intersected by a vein, which is three 
 feet wide, and contains bitter-spar lining the walls, with calc-spar in the 
 middle, which is traversed by reticulating strings of bitter-spar. Iron 
 pyrites is disseminated in large quantity in this vein, associated with a 
 smaller amount of yellow copper ore. 
 
844 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXII. 
 
 Moderate Throughout the whole area examined, the strata present very moderate 
 angles of inclination, in much of it not exceeding five degrees. They 
 seldom rise to fifteen degrees, and twenty degrees may be considered as 
 exceptional. The geological forms which guide the distribution of the 
 strata, are in consequence not readily reduced to rule ; and until the 
 contour of the outcrop is more fully traced out, it would be premature to 
 say much of the structure of the area. But it may be inferred from what 
 
 Synclinal, has been shown that there is in it at least one shallow synclinal, the axis 
 of which runs between the Marsh and Blind Rivers, nearly parallel with 
 the Mississagui ; and that this synclinal is traversed by a low transverse 
 
 Anticlinal, anticlinal arch, coincident with the valley of the Little White River. 
 
 Phillips, 
 burgh. 
 
 Section. 
 
 QUEBEC GROUP. 
 
 The investigations in connection with this group during the past season 
 have been confined chiefly to two localities at the opposite extremes of 
 Eastern Canada ; the one being in the neighborhood of Phillipsburgh, and 
 the other on the Strait of Belle Isle. 
 
 On pages 275-279, a partial series of the rocks occurring near Phillips- 
 burgh, with their enclosed fossils, is given in detail. In the following list 
 these rocks are comprehended in the divisions A and B, in the description 
 of which the lists of fossils, and the more minute particulars, are not repeated. 
 To this series are now added the divisions C and D, which are given with 
 their ascertained fossils, and with such general characteristics as have been 
 observed. The whole succession is, in ascending order, as follows : 
 
 A. 
 
 Feet. Feet. 
 
 Division A. 1. Dark grey and yellowish-white dolomites, weathering grey and yellowish- 
 brown, 400 
 
 2. White and dove-grey pure compact limestones, 100 
 
 3. Reddish-grey brown-weathering dolomites, and black dolomites with 
 
 some thin-bedded black limestones. 200 
 
 700 
 
 B. 
 Division B 1. White and dove-grey pure limestones, with some yellow-weathering mag- 
 
 nesian bands, 120 
 
 2. Dark grey and black limestones, some of the beds magnesian, 120 
 
 3. Dark bluish-grey thin bedded nodular limestones, with thin layers of 
 
 bluish-grey slate, probably magnesian ; the surfaces of some of the 
 beds weathering into a red or yellow ochreous arenaceous earth, . . 150 
 
 4. Black slaty thin bedded nodular limestones, with two or three thick beds 
 
 of purer limestone toward the base,* 300 
 
 6. Black limestones, some of them massive, weathering bluish-grey ; inter- 
 stratified toward the bottom with black and dark grey yellow- 
 weathering magnesian beds, 350 1040 
 
 * It is stated on page 279 that the parts 4 and 5 of this division are absent on the 
 province line. Part 5 is wanting ; but the chief portion of 4, with certain thick beds 
 toward the base, which are not mentioned on page 279, appears to be in place tfiere. 
 
CHAP. XXII.] 
 
 QUEBEC GROUP. 
 
 845 
 
 c. 
 
 Feet. Feet. 
 
 1. Black and dark grey compact pure limestones, weathering lead-grey, 
 
 with a few bands of dove-grey. The beds are all massive, and afford 
 abundance of a few species of testaceae ; the whole of which appear 
 to have the peculiarities of being large-sized and thick-shelled, and 
 of occurring in numerous isolated patches, which vary in diameter 
 from about three to ten feet. The fossils are several undescribed 
 species of Murchisonia and Pleurotomaria, Ecculiomphalus Canadensis, 
 E. intortus, E. spiralis, several undescribed species of Ophileta, 
 Maclurea ponderosa, several undescribed species of Orthoceras, and 
 one of Nautilus. Toward the base, Maclurea ponderosa seems to be 
 somewhat smaller than in the upper part of the deposit, and toward 
 the top one or two beds appear to be of a partially conglomerate 
 character, ................................. ................ 150 
 
 2. Black slates, or possibly thin bedded black limestones, with a few 
 
 thicker beds toward the top ; the mass is altogether very imper- 
 fectly seen, ................................................. 1*70 
 
 Division C. 
 
 320 
 
 Conglom- 
 erates. 
 
 1. Black limestone conglomerates, composed chiefly of the ruins of the Division D. 
 
 thick bedded limestones of division C. The enclosed masses 
 vary in size from pieces of an inch in diameter, to blocks containing 
 between fifty and sixty cubic feet, and are cemented together by 
 a calcareo-magnesian paste. Of this, however, from the closeness 
 with which the masses are packed together, there is but a very 
 small quantity. The limestones are generally close grained, and 
 black or dark grey in color, but there are mingled with them a few 
 scattered blocks of a lighter colored yellow-weathering dolomite, 
 some of them a foot in diameter. Many of the masses of limestone 
 contain fossils, and the species are almost wholly confined to those 
 already stated as characterising the parent beds C 1. There appear 
 to be at least two principal bands of this conglomerate, each varying 
 in thickness in different parts from about 50 to 100 feet. There is 
 an interval between them of from 100 to 150 feet, occupied by black 
 slates holding rounded masses of limestone, which convert parts of 
 the mass, varying in thickness from ten to twenty feet, into slaty 
 congomerates. In some parts, either the interval between the main 
 two bands of conglomerate increases considerably, or there is a 
 third band, with similar slates, intervening between it and the 
 second. The whole is contained in a thickness of from 250 to. ... 300 
 
 2. Black and greenish argillaceous slates, probably interstratified with 
 
 occasional thin calcareous bands, and thin lenticular patches 
 
 of limestone conglomerate, as well as more important bands Conglom- 
 
 of yellow-weathering dolomitic slates. The whole is ter- eratea. 
 
 minated by a band of black limestone conglomerate similar in char- 
 
 acter and thickness (from 50 to 100 feet) to those already mentioned, 
 
 and containing Maclurea ponderosa in one of the few places in which 
 
 the band has been seen. This whole mass of strata is very imper- 
 
 fectly exposed, and much uncertainty exists as to its true general 
 
 character. Its thickness may be from 750 to ................... 1000 
 
 3. Grey and black striped slates, some parts of which are calcareous, and 
 
 weather slightly brownish. They are interstratified with occa- 
 sional thin beds of black limestone, weathering lead-grey, as well as 
 
846 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 Feet. Feet. 
 
 many strong and solid beds of brown-weathering magnesian limestone, 
 Dolomitic and brown-weathering dolomitic slates. Some of the latter are marked 
 slates> by an abundance of fucoids resembling Buthotrephis flexuosa of Emmons. 
 Occasional beds of sandstone, from one to three feet in thickness, are 
 met with. About the middle of the mass there has in one place been 
 observed a bed of limestone conglomerate from five to ten feet thick, 
 and other similar ones may occur in different parts of the vertical thick- 
 ness, 1500 2800 
 
 4860 
 
 It has been stated on page 276, that on the province line, the limestones 
 included in division B of the above series, are arranged in the form of a 
 trough, with a moderate dip on the west side, and a precipitous one on the 
 east ; and on page 279, that the axis of this synclinal occurs near one of 
 the iron posts marking the boundary of the province, on the summit of a hill 
 Province west of Rock River, as represented in the annexed figure 442. The bear- 
 line section. i ng O f fa Q ax j s } g a ^ out g, 22 W. In this bearing, at the distance of 
 about 300 yards from the iron post in question, the black limestones near 
 the base of part 4* of division B, are seen to turn upon the axis ; and the 
 white limestones of B 1, mentioned on page 280 as probably concealed at 
 this point, have also been seen to turn upon this axis about 350 yards 
 beyond. The thin bedded black limestones belonging to part 3 of division 
 A, are exposed upon the axis about 500 yards still farther on ; but before 
 reaching the white and dove-grey limestones, 2 of division A, where they 
 are seen upon the axis, there is an interval of about a mile and three 
 quarters, occupied by an alluvial flat. The outcrop of these white lime- 
 stones is, without difficulty, traceable southward from the province line, 
 along the Phillipsburgh and Highgate Springs road, for about a mile and 
 a quarter ; but it separates from the road farther on, and, crossing the 
 Rock River between 500 and 600 yards from its mouth, the base of the 
 limestones 2, after showing a subordinate twist of some importance, comes 
 upon the main synclinal axis about 400 yards somewhat south of west 
 from the house of Mr. Church. The dolomites of part 1, division A, 
 sweep round behind the pure limestones, A 2, and, crossing the road a 
 little south of Mr. Church's house, come against the red Conocephalites 
 beds of the Potsdam group. The strata, A 1, occupy a place on the 
 axis for upwards of a mile ; beyond which, the limestones, A 2, again make 
 their appearance, perhaps let down by a transverse dislocation, and here 
 seem to constitute an outlier, with a length of about three quarters of 
 a mile, and a breadth of nearly half a mile at the widest part. At the 
 southern extremity of this outlier, the strata appear to converge toward 
 the synclinal axis ; on the east side of which, amidst some confusion, they 
 show a westerly dip, as they approach to within fifty or sixty yards of the 
 red beds of the Potsdam group, near the house of Mr. Robey. 
 
 * On page 280 these limestones were stated to belong to part 2 instead of to part 4. 
 
CHAP. XXII.] 
 
 QUEBEC GROUP. 
 
 847 
 
 <" 
 
 n. V -y // 
 
 -s -/// 
 
 
 O oa 
 
 TO o; 
 
 O + 
 
 ! 
 ss 
 
 ^. o 
 
 < PL) 
 ^^ 
 
 
 *M O 
 
 I? 
 
 From the province line northward, the white 
 and dove-grey limestones, 2 of division A, fol- 
 low the Phillipsburgh road for nearly two miles, 
 occupying the valley of Strite's Pond, and 
 running parallel with the coast of Lake Cham- 
 plain at a distance of about 800 yards. Near 
 Phillipsburgh they are seen on Mr. Cheeseman's 
 land, on the fifth lot of St. Armand ; and though 
 they thence gradually diverge from the margin 
 of the lake, they are traceable in a continued 
 straight course to the vicinity of Blood's Cor- 
 ners, nearly three miles farther on. In this 
 neighborhood, the higher beds of these lime- 
 stones enter the township of Stanbridge on the 
 first lot of the ninth range, and, crossing the 
 lot obliquely to the north side, they fold over Anticlinal, 
 an anticlinal axis on the Bedford road, where 
 they show a precipitous dip to west of north. 
 
 From the province line, the white limestones, 
 1 of division B, maintain a course parallel to 
 those of division A, and are traceable, without 
 difficulty, for the same distance northward. 
 East of Philipsburgh, they are a little more 
 than three quarters of a mile from the lake- 
 shore ; and the more fossiliferous overlying 
 black limestones, and thin bedded red-weather- 
 ing limestones, B 2 and B 3, which succeed, 
 form an escarpment to the east of them. The 
 surfaces of these upper beds here weather to a 
 red ochreous earth, and abound in the casts of 
 fossils, from which the calcareous matter once 
 filling them has been dissolved out. More 
 than a mile farther northward, near the house 
 of Mr. Hollis Hastings, they present the same 
 relation to the white limestones, B 1, and the 
 same weathered and fossiliferous condition. It 
 is probable that these strata are equally fossilif- 
 erous throughout ; but the undecomposed rock 
 being very hard and tough, it is only when 
 favorably weathered, that the organic forms can 
 be obtained in a state sufficiently perfect to be 
 identified, or indeed can be detected at all, un- 
 less with great difficulty. From the exposure 
 
848 GEOLOGY OP CANADA. [CHAP. 
 
 last mentioned, the white limestones, B 1, preserve their course in a well 
 stanbridge. marked valley until they enter the township of Stanbridge, on the first lot 
 of the ninth range ; beyond which they are obscure. The magnesian 
 limestones, A 3, which immediately underlie them, can however be followed 
 from the first to the second lot of this range, where they fold over the 
 Anticlinal, anticlinal axis already mentioned. The evidences of this are met with 
 on the Bedford road, near the house of Mr. J. Hall ; and indications 
 of the white limestones, B 1, occur a little farther eastward on the same 
 road ; where they are probably very near the axis, but somewhat on the 
 north side of it. 
 
 The bearing of this axis is about N. 65 E., and the evidences of the 
 anticlinal form are sufficiently well marked for upwards of a mile farther on 
 this road, to the line between the seventh and eighth ranges of Stanbridge ; 
 though it is necessary to proceed about a quarter of a mile to the south- 
 eastward of the road for some of the facts which prove the case. These 
 are on the second lot of the eighth range, where the dip of the strata is 
 southward, at angles of from ten to twenty degrees ; while on the north 
 side of the road it is northward, at angles of from forty-five to eighty- 
 five degrees, and often a few degrees beyond the perpendicular. Along this 
 part of the road, the escarpments not being well preserved, and the general 
 color of the strata being black or dark grey, it is not eas^ to assign the 
 beds to their different divisions ; though they all probably belong to 2, 3, 
 and 4 of division B. In this part the whole development of rock on the 
 north side of the anticlinal axis does not exceed between 300 and 500 
 yards in breadth. In this there appear to be one or two minor undulations ; 
 and although the white limestones, both of A 2 and B 1, are exposed in it 
 Blood's near Blood's Corners, it has not yet been found practicable to trace out 
 comers. ^fc. res p ect i v e connections in detail. In one of these exposures, which is 
 quarried, toward the west end of the second lot of the ninth range, not far 
 from the house of Mr. Schneider, a white limestone supposed to belong to 
 B 1, presents on the surface a narrow wedge-shaped mass, upward of a 
 quarter of a mile long, dipping on both sides southeastward at high angles. 
 The small end of the wedge points to the northeast, and the whole mass 
 overturn presents a sharp overturn anticlinal form ; the true character of which 
 anticlinal. wou i<j never be suspected, were it not for the presence of a yellow- 
 weathering magnesian bed of about a foot thick, which flanks it on both 
 sides, and folds over it at the extremity. 
 
 Across the seventh range, the rocks on the immediate axis of the main 
 
 anticlinal are concealed by drift ; but there are exposures on the Bedford 
 
 Bedford road, which runs about 300 or 400 yards northwest of the axis, and these 
 
 road. extend in one place as much as three quarters of a mile beyond the road. 
 
 This locality is on the land of Mr. Corey, on the sixth and seventh lots of 
 
 the seventh and eighth ranges of Stanbridge ; where there is a great display 
 
CHAP. XXII.] QUEBEC GROUP. 849 
 
 of the limestones, 1 of division C, which are extensively quarried and burned Corey's 
 in the neighborhood. The largest exposure is on the seventh lot of the ! 
 eighth range, showing a breadth of about 350 yards, dipping S. 78 E. 
 < 16-20. From this the strata run into the sixth lot of this range ; and 
 then apparently sweeping round the extremity of a trough, having a subor- Synclinal, 
 dinate undulation dividing it into two parts, they gain the adjacent por- 
 tions of the sixth and seventh lots in the seventh range. From the south- 
 west corner, they appear to traverse the latter lot obliquely, and then to 
 cross the southeastern corner of the eighth lot ; but here, proportionally 
 reduced in breadth by an increase in slope, they dip N. 42 W. < 
 55 70 ; thus proving their synclinal arrangement. Near the northern 
 extremity of the first and largest exposure mentioned, after an interval 
 of about 130 yards, leaving room for part 2 of division C, these lime- 
 stones are followed by the lowest band of the black limestone conglomerate Limestone 
 belonging to part 1 of division D. The exposure showing this is near the con ^ lomerafH 
 northwest corner of the seventh lot just mentioned; and the same 
 succession occurs on the southern side of the synclinal, where the lime- 
 stones, C 1, cross the southeast corner of the same lot ; while there are two 
 intermediate exposures of conglomerate, the one at the bottom and the 
 other at the top of D 1, with thin limestones and slaty conglomerates 
 between them. 
 
 The strata which come from beneath the massive limestones, 1 of division 
 C, and are exposed on the Bedford road, where it crosses the seventh 
 range of the township, are black limestones, many of them thin bedded, and 
 appear to belong to the upper part of division B. In conformity with this, 
 we should expect the limestones, C 1, and the succeeding conglomerates 
 of D to assume a place on the south side of the anticlinal, which runs 
 parallel with the road. The limestones of the upper part of division B 
 enter a little way into the eighth range, and the lowest band of conglom- 
 erate accompanies them, leaving space between for the strata of division 
 C ; which however are here concealed. Slaty conglomerates are met 
 with about half a mile farther on, in the town of Bedford, on the Pike Bedford. 
 River.* These are similar to some of the slaty strata associated with the 
 stronger conglomerates, and probably belong to division D ; but the fossils 
 occurring in the enclosed calcareous masses do not appear to include any 
 of the thick-shelled species so characteristic of the stronger bands. The 
 fossils met with are Orthis, an Ophileta like 0. uniangulata, with new 
 species of Agnostus, Ampyx, Asaphus, and Illcenus. 
 
 Black slates are seen both below and above this mass of slaty conglom- 
 erate ; and about half a mile somewhat westward of north from it, there 
 occurs an exposure of limestone conglomerate, which is supposed to belong 
 
 * By inadvertence, Bedford was stated, on page 276, to be on the Yamaska, instead 
 of on the Pike River. 
 
850 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. XXII. 
 
 Conglom- 
 erates. 
 
 Synclinal 
 axis. 
 
 Moore's 
 Corners. 
 
 to the summit of division D. Neither the massive limestones of C, nor any of 
 the succeeding conglomerates, have yet been observed on the axis of the 
 anticlinal, in what may be considered its prolongation from the eighth 
 range, the country being very much covered with drift. The same may 
 be said of the area on the southeast side of the anticlinal, between Bed- 
 st. Annand. ford and the north line of St. Armand, and a mile farther to the southwest. 
 The presence, and the course of the rocks of G and D under the drift, are 
 however pretty conclusively proved by well characterized exposures of 
 conglomerates on the twenty-ninth lot of St. Armand. These occur on 
 the north side of the lot, and nearly in mid-length of it. They are two 
 in number, and may probably belong to the two bands in part 1 of division 
 D. The beds dip S. 70 E. < 28, and are comprised in a breadth of 
 about 140 yards ; giving, with the uncertain interval which separates them, 
 a thickness of about 190 feet. They present many very large blocks of 
 black limestone, in which are found Murchisonia, Pleurotomaria Lauren- 
 tina,) Ecculiomphalus spiralis, Madurea ponderosa, M. matutina, and 
 Orthoceras. The nearest underlying rocks, exposed to the west of them, 
 apparently belong to the summit of division B. They occur at a distance 
 of about 700 yards, and their slope is about fifteen degrees. This interval 
 would give a vertical thickness of about 500 feet, which is more than 
 sufficient to include the strata of division C. 
 
 It was stated on pages 279 and 280, that on the east side of the syncli- 
 nal axis which crosses the province line on the hill west of Rock River, 
 the outcrop of one of the beds of part 4 of division B, had been traced 
 northeastward, in a nearly vertical attitude, for about three quarters of a 
 mile ; but that the turn of the higher divisions of the group on the axis 
 had not been ascertained. Dips have since been observed, inducing the 
 supposition that the axis is not removed more than 250 yards to the north- 
 westward of the nearly vertical bed above alluded to, so far as this has been 
 traced ; that it occurs at a somewhat less distance westward of Moore's 
 Corners, and that northward of this place it nearly coincides, for three quar- 
 ters of a mile, with the road to Blood's Corners ; leaving it where the road 
 makes a turn to the northwestward, on the twenty-sixth lot of St. Armand, 
 and where the strata of the upper portions of divisions B are exposed, dip- 
 ping westward at an angle of three or four degrees. This general course, 
 continued about a mile farther, would bring the axis to the immediate 
 vicinity of the conglomerate masses of D 1, on the twenty-ninth lot. About 
 200 yards eastward of these masses, there appears in the side of a rising 
 ground, a series of thin bedded slaty limestones, dipping about S. 87 E. 
 < 30, and occasionally becoming magnesian. These are followed by beds 
 in which pure grey limestones predominate, containing many specimens 
 of Stromatopora, Ophileta, and Orthoceras. These pure limestones are 
 penetrated and surrounded by a yellowish dolomite, giving to sections of 
 
CHAP. XXII.] QUEBEC GROUP. 851 
 
 the rock a broadly and irregularly mottled surface, which does not Dolomites, 
 however appear to be due to a conglomerate structure. The whole 
 exposure has a breadth of about 150 yards, and with the rise in the 
 ground, would give a thickness of about 250 feet. These strata, probably 
 belonging to the upper part of division B, appear to present the southwestern synclinal, 
 termination of a trough, one side of which runs about north, and the other 
 about N. 50 E. ; while the synclinal axis may have a course of N. 30 E. 
 On this axis, about half a mile from the end of the trough, there is another 
 exposure of conglomerate, between which and the sides there would be 
 room for the massive, limestones of division C. This exposure, holding 
 Eospongia, Madwrea matutina, Holopea, and Orthoceras, occurs near 
 the east end of the thirtieth lot, and there is little doubt that it is equiva- 
 lent to one of those of D 1, on the twenty-ninth ; but to account for 
 their relative positions, there must run between them either an anticlinal 
 or a dislocation. The attitude of the conglomerates on the twenty-ninth 
 lot, and of the thin bedded limestones to the east of them, with the narrowness Fault. 
 of the space between, make it probable that there is a break. 
 
 On the southeast side of the trough just described, the section above 
 mentioned is augmented by an addition of strata at the base, and presents 
 a more precipitous slope ; the dip of the lowest beds, which consist of thin 
 bedded limestones, being about N. 40 W. < 55-75. Strata belonging Potsdam 
 to the* Potsdam group come up behind these, at a distance of between s rou P- 
 eighty and ninety yards. They consist of a mixture of pure limestone 
 and dolomite, somewhat like that of division B just described, but inter- 
 stratified with layers of slate, and many beds of white sandstone, all white 
 without observed fossils. These strata have the same strike as the sa 
 thin bedded black limestones above them, and they slope in the same 
 direction, but at a more moderate angle, their dip being about N. 40 
 W. < 30-40. The exposures of these beds are seen on the land of the 
 Hon. Mr. Moore, between 300 and 400 yards north of his residence ; and 
 with another exposure occurring a little way southward, on the adjoining 
 parts of the twenty-seventh and twenty-eighth lots, near the house of Mr. G. 
 Carruthers, they show pretty clearly that the apparent arrangement of 
 the Phillipsburgh and Potsdam rocks is due to a fault. On the southeast Great fault, 
 side of the road, in the latter locality, the Potsdam beds show extensive 
 surfaces of white sandstone and of brown-weathering sandy magnesian 
 limestone, interstratified with one another and dipping at a very low angle 
 eastward of north. Approaching the road, they bend over a little toward 
 it ; and from fifty to sixty yards on the northwest side of it, they come 
 into contact with the Philipsburgh strata, which stand in a nearly vertical 
 attitude against the terminal edges of the v Potsdam beds. The two forma- 
 tions are seen in contact for about 600 yards. At the northeastern end of 
 the exposure, the Phillipsburgh strata, of which there may be altogether 
 
852 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXII. 
 
 id ge 
 
 J 
 
 Ig- 
 
 be o 
 
 a & 
 
 .2 bo 
 
 2 H 
 
 'So 
 
 T3 a 
 
 a thickness of between 300 and 400 feet, are thin bedded black lime- 
 stones and nodular shaly limestones ; their dip being N. 60 E.< 75 - 90. 
 But proceeding southwestwardly, a band of pure whitish limestone, 
 mixed with brown-weathering light grey dol- 
 omite, becomes gradually interposed between 
 the thin slaty limestones and the Potsdam 
 beds ; and the dip of the former at the same 
 time becoming gradually overturned, ulti- 
 mately overhangs the perpendicular as much 
 as sixty degrees. Along the junction of the 
 two formations, broken masses of strata are 
 thrust in irregular attitudes between them, 
 and the whole exposure presents the aspect 
 of a well-marked dislocation. In the dia- 
 gram 443, showing a section across the 
 conglomerates on the twenty-ninth lot, the 
 band exposed on the thirtieth lot is intro- 
 duced in the position which it would occupy 
 were it continued far enough southward. 
 This diagram also sufficiently illustrates 
 the contact of the Phillipsburgh strata with 
 those of the Potsdam group, as just described. 
 In this neighborhood, both of these groups 
 become concealed by drift about a mile 
 northeastward of the exposures which have 
 been described on the land of the Hon. Mr. 
 Moore, on the twenty-ninth lot of St. .Ar- 
 mand ; and they have not as yet been traced 
 much beyond the house of Mr. J. Rosen- 
 berger, on the one hundred and thirtieth lot 
 of St. Armand, which is the one abutting 
 against the thirtieth lot. 
 
 Returning to the northwest side of the 
 whole mass of rocks belonging to the Quebec 
 group, which we have been investigating, 
 there is still something to be added in re- *s J 
 
 . t-3 
 
 gard to the distribution of the limestone con- pt 
 
 glomerates in Stanbridge. From the seventh lot of the seventh range 
 of the township, where, as already stated, there is an exposure of the conglom- 
 * erates at the base of division D, they are traceable to the northeastward, 
 by an exposure which crosses the Henryville road, about a mile westward 
 of Bedford, and extends to the left bank of the Pike River. The length 
 of this exposure is somewhat under half a mile, and it exhibits both of the 
 
 
 , 
 g 
 
 if 
 
 S. 
 
CHAP. XXII.] QUEBEC GROUP. 853 
 
 bands of conglomerate of D 1. To the right of the Pike River, there is a Pike River, 
 drift-covered interval of about three quarters of a mile ; beyond which the 
 conglomerates again appear on the twelfth lot, and can be followed thence 
 with facility to the north side of the eighteenth lot, the distance being 
 about two miles. In this, they gradually pass from the seventh to the sixth 
 range, and in the latter half of their course keep close upon the line divid- 
 ing these ranges. The general dip is about S. 75 E. < 40-45 ; but irreg- Transverse 
 ularities occur in some parts, occasioned by transverse dislocations. There 
 appears to be one of these on the thirteenth lot, another on the line between 
 the fourteenth and fifteenth lots, and a third probably occurs at the Wall- 
 bridge mills, on the fifteenth lot, where the Beaver Brook finds a passage 
 across the bands. The strata are concealed across the nineteenth lot ; but the 
 conglomerates again appear for 300 or 400 yards on the twentieth, and 
 finally gain the twenty-first lot. Their course across this lot is about N. 
 40 E. ; and gaining the north side of the lot, toward the east end, the 
 upper band is seen to make a turn in folding over an anticlinal axis, on Anticlinal, 
 the north side of which it returns in a course about S. 70 W., for 600 
 yards ; showing a high dip to the westward of north. 
 
 None of the strata belonging to part 2 of division D have been observed 
 in connection with this run of the division from the seventh lot of the 
 seventh range, before reaching the fourteenth lot of the sixth range of 
 Stanbridge. Here the conglomerate band at the top of D 2, is exposed 
 for about 300 yards along the Farnham road, showing a breadth of about 
 fifty yards. Indications of it are seen again on the Beaver Brook, 
 on the fifteenth lot ; and it is said to have been struck in sinking a well, 
 on the east side of the road in the seventeenth lot. On the west side of the 
 road there occurs a band of brown-weathering black dolomitic slates, 
 which underlies the conglomerate. The most northern, and the only other 
 observed exposure of this conglomerate band 2 of D, occurs on the 
 twenty-second lot of the fifth range ; where it dips northward at an angle 
 of from forty to fifty degrees, and is evidently on the north side of the 
 anticlinal axis over which the lower conglomerate 1 of D, folds in the 
 next range. 
 
 The only examinations which have yet been made of the strata of part 
 3 of division D, are upon a road running eastward from the Farnham 
 road between the eighteenth and nineteenth lots, and upon another 
 road running eastward from the Wallbridge mills, on the fifteenth lot. The 
 strata seen on both of these roads are chiefly brown-weathering dolomitic 
 slates. On the more northern one they show a breadth of about two miles, slates> 
 extending about 700 yards into the fourth range ; on the other road, with a 
 breadth of a mile and a quarter, they have been observed to about the 
 middle of the fifth range. About nine chains west of the line between the 
 fifth and sixth ranges, the dolomitic slates are interstratified with a ten- 
 
854 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXII. 
 
 Hudson 
 
 River 
 
 formation 
 
 feet band of black limestone conglomerate ; and about eleven chains east of 
 Anticlinal, the line, they fold over the axis of an anticlinal, which is probably a con- 
 tinuation of the one passing near Blood's Corners. What effect this anti- 
 clinal, in its farther prolongation, may have upon the distribution of the 
 rocks of the division D has not yet been ascertained. 
 
 Immediately to the northwest of the mass of rocks belonging to the 
 Quebec group, which have thus been followed from Vermont to the twenty- 
 first lot of the sixth range of Stanbridge, there runs the whole way, a 
 depression, occupied partly by Lake Champlain, and partly by low flat 
 land, often covered with swamp. Beyond this, at a variable but moderate 
 distance, there is a ridge of black slates resembling those of the Hudson 
 River formation, and considered equivalent to them, between which and the 
 Phillipsburgh series, there is supposed to be a great break. These slates 
 are seen within 500 yards of the exposure of the conglomerates of D 1, 
 already mentioned as occurring on the twentieth lot of the township ; 
 and dip in the same southeastward direction, with a slope of forty-five 
 degrees. They are seen also on the twenty-first lot ; and here their strike 
 would bring them to within 250 yards of the conglomerate band, where it 
 is doubled over, very probably by the effect of the dislocation, to a precipi- 
 tous dip westward of north. On the road between the eighteenth and 
 nineteenth lots, the distance would be about 700 yards, and on the road 
 west of Bedford, about half a mile. On a road in the sixth lot the 
 black slates would be about half a mile west from the massive limestones of 
 the division C ; but about half a mile southwestward of these, there start up 
 from the intermediate flat ground two isolated masses of strata dipping west- 
 ward of north, at high angles, and showing in ascending succession about 
 seventy feet of dove-grey limestone, fifty feet of white-weathering sand- 
 stone, and twenty fe6t of thin bedded slaty black limestone. These rocks, 
 which are distinct from and higher than any of the divisions first described, 
 Division E. may for convenience be designated as division E. They resemble in 
 sequence and lithological character the lower part of the strata of St. 
 Dominique, and of Highgate Springs ; to which they are still farther 
 assimilated by the occurrence in the thin bedded limestone of Stenopora 
 Chazy for- fibrosa, a fossil which is not met with lower than the Chazy formation in the 
 undisturbed outcrop of the Lower Silurian series at the base of the Lau- 
 rentian hills. These two isolated masses of strata stand one behind the 
 other, at a distance of about 250 yards ; and in the more northern one, 
 following a small twist, there is a fault running parallel with the general 
 trend of the black slates, and producing a displacement of about fifty yards. 
 This carries a part of the northern mass nearer to the southern, and it is 
 probable that there may be other breaks or twists between them. It would 
 seem that a part of the Chazy has here been brought up from beneath 
 the Hudson River formation ; and there would be quite room enough 
 
 nation. 
 
CHAP. XXIL] 
 
 QUEBEC GROUP. 
 
 855 
 
 under the concealed space between the isolated masses of the former, and 
 the black Hudson River slates, for the Birdseye and Black River, as well 
 as the Trenton formation. 
 
 At Phillipsburgh these black slates come against the strata of part 1 
 of division A. The relation of the strata on the western and eastern sides 
 of the great fault which there runs between them, as well as of those on the Highgate 
 opposite sides of its continuation at Highgate Springs, has already been 
 
 444. SECTION AT HIGHGATE SPRINGS, VERMONT. 
 
 Horizontal and vertical scale, three inches to a mile. 
 
 L i] level of lake ; s s, sea level ; A A, lowest division of the Quebec group in the 
 Phillipsburgh series, page 844 ; B E, the Chazy formation, with the dove-grey lime- 
 stones at its base, page 854; Bl, Black River formation; Tr, Trenton formation; 
 u, Utica formation ; /, proximate place of fault. The portion from a; to is concealed. 
 
 given on pages 273-275. The strata on the west side of the fault, at the . 
 latter place, belong to the Chazy, the Birdseye and Black River, the Trenton, 
 and the Utica formations, and the accompanying diagram, 444, shows their 
 arrangement. The Trenton at its final outcrop, has a western dip, and there 
 would be room in the covered space between it and the Quebec group for 
 the Birdseye and Black River formation, as well as for the Chazy, and 
 the dove-grey limestone which may be a part of it. In the diagram these 
 formations are introduced in the position which they probably occupy to the smith's 
 eastward of the strata exposed. At Smith's lime-works, about eight miles lime - works - 
 
 445. SECTION AT SMITH'S LIME-WORKS. 
 
 West. 
 
 TrBl/E 
 
 E f Potsdam group. 
 
 East. 
 
 / E E/' Potsdam. 
 
 Horizontal and vertical scale, three inches to a mile. 
 
 L L, level of Lake Champlain ; s s, sea level ; E B, Chazy formation, with lower 
 dove-grey limestones, as above ; si, Black River formation ; Tr, Trenton formation ; 
 //, fault ; /'/') break or overlap bringing up the Potsdam group. 
 
 southward of Highgate Springs, these formations (probably on the east 
 side of another synclinal) become inverted, as described on page 280, and 
 a wood-cut, 445, is now given to illustrate their attitude. In this a line is- 
 introduced, showing the position of the great break that must here occur ; 
 but as stated on page 281, no evidences have been found to show that the 
 
856 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 beds on the west side of this position do not run conformably under those 
 to the east. Both to the north and the south of the lime-works there 
 have been observed some additional facts in connection with the rocks 
 involved in this inversion, which deserve to be noticed. 
 
 Between the high road and the railway from St. Alban's to Swanton, and 
 about a mile and a half northward from Smith's lime-works, there occurs an- 
 other exposure of the rocks of division E . The dove-grey limestone approaches 
 to within 240 yards of the high road, and shows a breadth of about the 
 same measure, with a dip E. < 30-80. The west side of this mass, in its 
 strike to the south, would come close upon the east side of an exposure of the 
 sandstone ; which, with a dip in the same direction as that of the limestone, 
 has a breadth of 220 yards, with an inclination of from thirty-five to fifty- 
 five degrees. This would give it a greater thickness than where seen else- 
 where, but its apparent volume may possibly be increased by disturbances. 
 On the west side it becomes interstratified with the black limestone, which 
 terminates the exposure, and approaches to within about 120 yards of the 
 railway. These masses are precisely in the strike of those at the lime- 
 works, and a continuation of the strata in the same direction would carry 
 them, in less than a mile, across the road over the flat land between the 
 red strata of the Potsdam group (page 281), and the Missisquoi bridge 
 southeast of Swanton. Less than another mile in the same direction 
 would bring us to a development of the dove-grey limestone about a mile 
 east from Swanton, on the road to Highgate Falls. The strata of this 
 exposure, which has a length of about 400 yards, and a breadth of about 
 200, are arranged in the form of a trough converging northward ; the dip 
 on the west side being about S. 72 E. < 55-80, and on the east S. 60 
 W. < 40 85. But to the southwest of this there is another and a very 
 considerable ' exposure of dove-grey limestone between Swanton and the 
 Missisquoi bridge already mentioned. The area which it occupies has a 
 length transverse to the measures of about 1200 yards, terminating south- 
 eastwardly at the margin of the river, and a breadth, with the measures, of 
 about 700 yards. The general strike of this mass appears to be about 
 N. 15 W. ; which would carry it a little to the westward of the exposure 
 on tjie road to Highgate Falls. The general dip of the strata is to the 
 eastward : the* angles of inclination, as ascertained on the east and west 
 sides of it, vary from thirteen to twenty-five degrees ; but in the interme- 
 diate part, there occur one or two undulations, which serve to diminish the 
 average rate. This area has very probably a farther extension northward? 
 and may join the west side of the one just described as occurring more to 
 the north ; the strike of that side of the more northern exposure being 
 directed towards it. Its position and attitude would seem to indicate that 
 it is on the western side of a trough, of which the exposures of dove-grey 
 limestone farther south are on the eastern, and more precipitous or over- 
 
CHAP. XXII.] 
 
 QUEBEC GROUP. 
 
 857 
 
 w 
 
 to o 
 
 p 
 
 >-> 03 
 
 I* 
 
 turn side, and that these masses have above them in the middle, a con- 
 forming mass of the sandstone and black limestone. The diagram 446, 
 represents a section running east and west across the Mississquoi River, 
 at the bridge southeast of Swanton. It illustrates the relation of the 
 dove-grey limestone which is west of the bridge, to the strata of division 
 
 E to the south of it, and to those of the 
 |g Potsdam group to the eastward. 
 
 To the southward of Smith's lime-works the 
 same series of strata occur at the lime-works 
 of Mr. Rich. They still present the same 
 inverted attitude, and Professor Emmons states 
 that OrtJioceras is here met with in the dove- 
 grey limestone. Still farther southward, about 
 a mile beyond Stephen's Brook, the dove-grey 
 limestone is seen close against the red strata 
 of the Potsdam group ; and about a quarter of 
 a mile to the west of it there is a small ex- 
 posure of the black limestones, the sandstone 
 being probably concealed in the interval. The 
 dove-grey limestone continues along the cliff 
 in a narrow band for about a mile. There 
 is then an interval of about half a mile from 
 which it is absent, but it again becomes exposed 
 in the vicinity of St. Alban's Bay, at the mouth st. 
 of the ravine leading up to St. Alban's, and on Bay ' 
 the opposite sides of it. On the north side it 
 runs along the escarpment of the Potsdam 
 strata for nearly half a mile, approaching to 
 within twenty yards of it. Both rocks dip 
 about S. 80 E. ; but while the Potsdam beds 
 present a pretty uniform inclination of from 
 fifteen to twenty degrees, the inclination of 
 the dove-grey limestone varies from fifteen to 
 sixty-five degrees. The breadth of the lime- 
 stone is here about 180 yards, and on the 
 J western side of it, which would be the top, 
 there occurs a Pleurotomaria very like 
 
 P. Quebecensis. The dove-grey limestone here, as farther north, is 
 succeeded by the sandstone, the two being seen in contact, and the 
 black limestone follows. On the south side of the ravine there are two 
 exposures of the dove-grey limestone, one nearly touching the red strata 
 of the Potsdam group, and the other about a quarter of a mile to the north- 
 east of it, on the left side of the rivulet which flows out from the ravine. 
 
 T? a 
 % 'So 
 
 
 
858 GEOLOGY OP CANADA. [CHAP. XXII. 
 
 The mass near to the Potsdam strata dips in the same direction with them, 
 about S. 70 E., but at a higher angle; the inclination of the latter being 
 from seven to fifteen degrees, while that of the former is from twenty to 
 forty-five degrees. The more western exposure of the dove-grey limestone 
 is followed by the sandstone ; which becomes interstratified with thin beds 
 of black limestone, and is limited by a thick bed of this rock, studded with 
 nodules of black chert. This is seen where the rivulet flowing from the 
 ravine falls over the escarpment formed by the limestone. In its strike, 
 nearly half a mile to the south, a limestone of the same color occurs, hold- 
 ing StropJiomena alternata, a Maclurea like M. Atlantica of the Chazy, 
 fossils* 1 w *th a Pleurotomaria, (these two being seen in section,) together with 
 an Asaphus like A. platycephalm. The first and last of these species 
 ascend to the Hudson River formation. Opposite to the ravine, and in a posi- 
 tion which is westward of the northward strike of the black limestones, there 
 occur -two exposures of dove-grey limestone, constituting two mounds or 
 hillocks, belonging probably to one mass of rock, with a length of about 
 500 yards, and a breadth of 150. In the arrangement of this mass, there 
 appears to be a curve, the dip at the west end being about S. 55 E.<58, 
 while on the southwest side it is about 1ST. 35 E. < 50-60. The mass 
 appears to be underlaid by black slates similar to those at the Missisquoi 
 bridge, west of S wanton ; and it may belong to the west side of the same 
 synclinal as the dove-grey limestone at the east bridge, and have a con- 
 cealed outcrop connection with it. It is probable that there may be a 
 transverse dislocation running up the ravine at St. Alban's Bay, throwing 
 the measures on the south side of it to the westward. This would apparently 
 pass between the rivulet which falls over the cherty limestone, and the two 
 hillocks which have been mentioned, and would keep to the north of the 
 road to St. Alban's. On this road, about a mile west of St. Alban's, there 
 is a band of limestone conglomerate, holding large masses of grey pure 
 limestone, imbedded in a brown-weathering calcareo-magnesian paste ; 
 which is traceable for upwards of a quarter of a mile north of the road 
 before it disappears : the place of the fault would probably be a little north 
 of this. About a quarter of a mile farther west, on the road, this conglom- 
 erate is followed by a mass of whitish sandstone, weathering brown; at 
 the base of which there is another band of conglomerate, with fewer and 
 smaller masses of pure limestone. Immediately beneath this occurs a band 
 oboUeia of dark grey slightly micaceous slate, with Obollela cingulata. Its posi- 
 siates. on - g gjjQ^ 1200 yards from the escarpment of the Potsdam red strata, 
 where these come in contact with the dove-grey limestone on the south 
 side of the ravine. The average inclination of these strata is about eleven 
 degrees, which would give a thickness of about 680 feet. The thickness 
 in the Potsdam section to the east of Swanton (page 281), from the white 
 and red dolomites to the top of the Paradoxides bed, is 650 feet ; and the 
 
CHAP. XXIL] QUEBEC GROUP. 859 
 
 slates in the two localities so closely resemble one another that there is not 
 much doubt of their equivalency. 
 
 It will be seen from what has been said, that between St. Alban's Bay TWO <us- 
 and the middle of Stanbridge, there are two great dislocations connected location8 - 
 with the Quebec overlap ; the western one running from the outside of the 
 hillocks of St. Alban's Bay, by Swanton, Highgate Springs, and Phillips- 
 burgh, to the twenty-first lot of the sixth range of Stanbridge ; and the 
 eastern from the mouth of the ravine at St. Alban's Bay, by Smith's lime- 
 works, the Missisiquoi valley southeast of Swanton, the Rock River on 
 the province line, and the house of Mr. J. Carruthers, to the one 
 hundred and twenty-ninth lot of St. Armand. It was stated as probable, 
 on page 283, that these two faults would join one another somewhere in the 
 neighborhood of Smith's lime-works. This statement must now be modified. 
 The.junction is evidently south of St. Alban's Bay, and it would require far- 
 ther examination to know how near it may approach to Burlington. From 
 the position of the highest dove-grey limestone on the Highgate Falls road, 
 east of Swanton, and of the lowest, near Mr. Robey's residence, it is 
 evident that a dislocation must pass between them, from the eastern to the 
 western fault. To determine the position from which this starts from the 
 eastern fault, will require additional facts ; but about a mile south from 
 Robey's, there is an exposure of grey pure limestone, and about half a mile 
 east from this another ; the former showing Ophileta, and the latter in one or 
 two of its beds almost made up of Stromatopora compacta^ a species hith- 
 erto not found lower than the horizon of the Chazy formation. Possibly 
 some evidence may hereafter be obtained near these exposures, to eluci- 
 date the matter. In the meantime, it is probable that this intermediate General 
 break joins the western fault somewhere not far from the mouth of the structure. 
 Rock River ; and it would appear that included between the east and west 
 faults, from the intermediate break southwards, we have an area composed 
 of a mass of conformable deposits, of which the Trenton formation is at 
 the summit ; while between the same faults, from the intermediate break 
 northward, are included deposits belonging wholly to the Quebec group. 
 The strata in each area are arranged in the form of a trough, with a com- 
 paratively gentle dip on the west, and a precipitous or overturn dip on the 
 east side ; and as the strata of the more northern area approach the west 
 fault, it is seen in some parts that they become precipitously bent over 
 toward it. The northern trough-like area, as has been shown, is divided 
 into two subordinate forms of the same character, by an anticlinal with a 
 gentle dip on the east, and a precipitous, occasionally overturn dip on the 
 west. Were this anticlinal to pass into a fault by the disruption of the 
 strata on the west side, it would represent the probable character of the 
 greater disturbances to the east and west of it ; the one to the west being 
 supposed to be directly connected with the break and overlap at Quebec. 
 
860 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 Between Stanbridge and Quebec no fossiliferous strata have been met 
 with similar to those of the divisions A, B, and C of the Phillipsburgh 
 series. The nearest approach to the material of any of these beds occurs 
 in some of .the lighter colored masses of limestone enclosed in the Point 
 k^ s conglomerates. The strata accompanying these closely resemble 
 crates, those' associated with the conglomerates of division D in Stanbridge, partic- 
 ularly the brown-weathering magnesian limestones and magnesian slates ; 
 the latter of which in both localities are characterized by the same fucoid 
 in similar abundance. The limestone masses in the Stanbridge conglom- 
 erates, in as far as these have been examined, appear however to be chiefly 
 derived, as has already been stated, from the dark colored limestone of 
 division C. If with these there were mingled any considerable proportion 
 of the ruins of the lighter colored limestones of A and B, the general 
 lithological resemblance of the Stanbridge and Point LeVis conglomerates 
 would be sufficiently close to leave little doubt of their equivalency. 
 With the exception of the locality at Bedford, the Stanbridge conglomer- 
 ates have however yielded scarcely any fossils other than those which 
 characterise the dark colored limestone of C. None of the species belong- 
 ing to this division have ever been met with in the Point EC* vis conglomer- 
 stanbridge ates, and the only fossils common to these, and to the Stanbridge conglomer- 
 erate8 m a * es are Ophileta uniangulata, which occurs in the latter in one of the 
 exposures on the Henryville road ; and two specimens from Bedford. One 
 of these strongly resembles Agnostus Orion, and the other is the hypostoma 
 of an Asaphus, identical with a specimen from the island of Orleans. 
 Eight of the most characteristic species of the divisions A and B of the 
 Phillipsburgh series occur in the conglomerates of Point LeVis. These are 
 Camerella caldfera, Holopea dilucula, EcculiompTialus Canadensis, E. 
 intortus, Bathyurus Saffordi, B. Cordai, Ohierurus Eryx, and MenocepJia- 
 lus globosus ? The occurrence of these fossils, and the general structure of 
 the Point LeVis conglomerates, seem to support the opinion that some of 
 the rounded masses enclosed in these may be derived from the ruins of 
 limestones equivalent to those of A and B of Phillipsburgh, in the same 
 way as the masses of the Stanbridge conglomerates are derived from C. 
 This would place the two series of conglomerates on the same horizon ; and 
 although the difference in time might not be great, it would make the Point 
 Le*vis rocks somewhat younger than the lower divisions of Phillipsburg. At 
 the same time however, some of the fossiliferous portions of the Point Le*vis 
 bands, having the same color and texture as the supposed boulders, pos- 
 sess the character of original sediments or concretionary masses, and it is 
 difficult to separate the fossils of these from those of the rolled masses. 
 
 It is not yet certain how many of these conglomerate bands there may be 
 in succession at Point LeVis, but it will be seen from a plan in the Atlas 
 accompanying this Report, that there are supposed to be at least nine. 
 
CHAP. XXII.] QUEBEC GROUP. 861 
 
 On this plan, the heavy black bands represent the known exposures of 
 the limestone conglomerates, while the dotted lines between different 
 exposures represent their supposed connection. Some of the geographical 
 undulations are shown by what are designated on the plan as the Coast Ridges at 
 Ridge, and the North, Middle, and South Ridges. The main feature of 
 the Coast Ridge is a thick band of limestone conglomerate, extending in 
 a hill and precipice, which overlook the beach from Patton's wharf to the 
 neighborhood of the Lower Ferry ; beyond which it gives place to the 
 cliff which is immediately behind the houses near the Lower, Middle, 
 and Upper Ferries. The North Ridge is a hill, which rises up from and 
 runs parallel with the road passing in front of the Temperance Monument 
 or Cross, and attains its greatest height in a band of limestone conglom- 
 erate, about 300 yards southeastward. The Middle and South Ridges 
 are respectively about a quarter and three quarters of a mile to the 
 southeast of this. 
 
 Southeastward from the St. Lawrence, the limestone conglomerates of Distribution 
 Point LeVis are distributed over a breadth of more than two miles. In ol 
 the Middle and South Ridges they are arranged in two well marked anti- 
 clinal forms ; and the axis of a third anticlinal is suspected to run along 
 the road on the north side of the North Ridge. In the North Ridge there 
 are four bands, numbered 1, 2, 3, 4, on the plan ; on which is represented, 
 in addition, a long lenticular bed, 4 a , subordinate to 4, but separated from 
 it by slate. This lenticular bed is composed of brown-weathering magne- 
 sian limestone, but appears to contain few or none of the included masses 
 of pure limestone which characterize the conglomerates. On the north 
 side of the Middle Ridge are exposed five additional bands, numbered 5, 
 6, 7, 8, and 9 on the plan. From the dotted lines on this the relation of 
 the whole will be understood. 
 
 The distribution of the fossils in these bands is shown in the following Fossils, 
 catalogue, in which there is a column for each of the nine bands mentioned, 
 and also for each of three bands marked D, G, and A on the plan. The 
 first of these three occurs at the margin of the St. Lawrence, in front of the 
 Coast Ridge, and the other two along the cliff to the southwest. To these 
 three bands no certain stratigraphical place is assigned ; but should an 
 anticlinal form really exist on the north side of the North Ridge, they 
 would probably be a repetition of some of the lower bands in the series 
 from 1 to 9, which is in ascending order. With the exception of those 
 otherwise marked, all the determined species have been described by the 
 palaeontologist of the Survey. 
 
862 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXII. 
 
 LIST OF FOSSILS FROM THE VARIOUS BANDS AT POINT LEVI8. 
 
 
 D 
 
 G 
 
 A 
 
 1 
 
 2 
 
 3 
 
 4 
 
 5 
 
 6 
 
 1 
 
 8 
 
 9 
 
 Tetradium ? 
 
 
 -X- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 ,V- 
 
 
 
 
 
 
 Lingula Mantelli, 
 
 
 
 
 
 
 # 
 
 -X- 
 
 
 
 
 
 
 " Irene, 
 
 
 -V- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 # 
 
 
 
 
 
 
 
 
 
 
 Obolella Ida 
 
 
 
 
 
 
 .V. 
 
 X- 
 
 
 
 
 
 
 
 
 
 -X- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 .V- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 .V. 
 
 -X- 
 
 7 
 
 .V. 
 
 -X- 
 
 
 
 
 
 
 
 
 
 .V. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 .V- 
 
 
 
 
 
 " " 2,.. 
 
 
 
 
 
 
 A'. 
 
 
 
 
 
 
 
 3 
 
 
 
 
 
 
 
 * 
 
 
 
 
 
 
 
 
 
 -X- 
 
 
 
 
 
 
 
 
 
 
 Orthis gemmicula, 
 
 
 
 
 
 
 
 
 3fc 
 
 
 
 
 
 " Tritonia, 
 
 
 
 
 
 
 
 
 -V- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 -V- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " Electra 
 
 
 
 
 
 
 
 
 .V. 
 
 
 
 
 
 " Hippolyte, . 
 
 
 
 
 
 
 
 
 _Y- 
 
 
 
 
 
 " Evadne, 
 
 
 
 
 
 
 
 
 .V. 
 
 
 
 
 
 " Mycale, 
 
 
 
 
 
 
 
 
 .'.'. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 -V. 
 
 
 
 
 
 c< Quebecensis, 
 
 
 
 .V. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 n u 2 
 
 
 
 
 
 
 
 * 
 
 
 
 
 
 
 " " 3,.. 
 
 
 
 
 
 
 
 X- 
 
 
 
 
 
 
 " " 4 . 
 
 
 
 
 
 
 
 
 
 
 
 
 X- 
 
 
 
 
 
 
 
 -V. 
 
 -y- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " Arethusa, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 -X- 
 
 
 
 
 
 
 " intortus, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 Pleurotomaria vagrans, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " Postumia, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " Quebecensis, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 2,. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 3, 
 
 
 
 
 
 
 
 
 
 
 
 -X- 
 
 
 " " 4. . , 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " 
 
 * 
 
 
 " 
 
 
 " 
 
 
 
 
 
 
 " " 2, . 
 
 
 " 
 
 
 
 
 
 
 
 
 
 
 
 n 3 
 
 
 ' 
 
 
 
 
 
 
 
 
 
 
 
 tt ^ 
 
 
 * 
 
 
 
 ' 
 
 
 
 
 
 
 X- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
CHAP. XXII.] 
 
 QUEBEC GROUP. 
 
 863 
 
 FOSSILS FROM POINT LEVis. Continued. 
 
 
 D 
 
 G 
 
 A 
 
 1 
 
 2 
 
 3 
 
 4 
 
 5 
 
 6 
 
 7 
 
 8 
 
 9 
 
 
 
 
 
 
 
 
 -V. 
 
 
 
 
 
 
 
 
 
 
 
 - 
 
 
 
 
 
 
 - 
 
 
 Holopea dilucula (Hall) 
 
 
 
 
 
 
 
 * 
 
 
 
 
 
 
 
 
 
 
 
 
 
 -"- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 .V. 
 
 
 
 
 
 
 " Hvrie 
 
 
 
 
 
 
 
 ,v. 
 
 
 
 
 
 
 " Orphyne, . . ; 
 
 
 
 
 
 
 
 -'- 
 
 
 
 
 
 
 " Venillia . 
 
 
 
 
 
 
 X- 
 
 -y- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 -V. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 .V. 
 
 
 
 
 
 
 
 
 
 
 
 
 ,Y. 
 
 -V. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " " 2,.. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 3, 
 
 
 
 
 
 
 
 A'- 
 
 
 
 
 
 
 4 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " " 5,.. 
 
 
 
 
 
 
 
 A'. 
 
 
 
 
 
 
 " > " 6. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " Dictys, 
 
 
 
 
 
 
 
 -Y- 
 
 
 
 
 
 
 " Alethes, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " Syphax, . 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " undescribed, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 Nautilus, " 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 Orion, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 Arionellus cylindricus, 
 
 
 
 
 
 
 -V. 
 
 
 
 
 
 
 
 " subclavatus, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 Bathyurus capax, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " dubius, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " bituberculatus, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " armatus, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " Saffordi, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " Cordai, 
 
 
 
 
 
 
 A-. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 .V. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " Eryx, . . 
 
 
 
 
 
 
 
 //. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 _". 
 
 
 
 
 
 
 Dikelocephalus magnificus, 
 
 
 
 
 
 
 'X- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 y- 
 
 
 
 
 
 
 
 " Oweni, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
864 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXII. 
 
 FOSSILS FROM POINT LEVis. Concluded. 
 
 strait of 
 Belie isle, 
 
 -. il'J 
 
 
 D 
 
 G 
 
 A 
 
 1 
 
 2 
 
 3 
 
 4 
 
 5 
 
 6 
 
 7 
 
 8 
 
 9 
 
 Dikelocephalus Belli, 
 
 
 
 
 
 
 
 .*'. 
 
 
 
 
 
 
 " megalops, 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " undescribed .... ... 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " (Olenus) Logani (Devine), 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 .- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " Salteri (Devine), 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 " 
 
 
 
 
 
 
 
 
 
 
 In describing the rocks on the strait of Belle Isle, it was stated on 
 pageg 287-292 that the strata on the north side, belonging to the Potsdam 
 group, descend to the water at an inclination of about sixty feet in a 
 mile ; and that those immediately opposite, on the south side, apparently 
 belonging to the Calciferous formation, rise from the water at an angle so 
 small that it was nearly impossible to distinguish it by the eye. The beds 
 under the strait thus appeared to form a shallow trough ; and the strata 
 along the coast, southward from Anchor Point, showing a very small slope to 
 the southwest, seemed, along the water-line, to be turning from the extremity 
 to the side of the trough in question. An examination of the coast of the 
 island from Anchor Point northward to Cape Norman, has shown that the 
 same strata descend with a very gentle slope all the way in that direction also. 
 It is inferred therefore that in neither direction is this small inclination at 
 right angles to the strike, and that the true dip must be between them, or 
 toward the southeast. The scarcely appreciable rise mentioned as occur- 
 ring on the southwest side of the strait must probably therefore be only 
 local, and there is consequently no reason for supposing that the beds under 
 the strait are arranged in the form of a trough; although it is possible, as will 
 be seen farther on, that they may be on the north side of a synclinal form, of 
 which the axis would be at some distance to the southeast. If, in this case, 
 it be assumed that the dip of the beds under the strait is southeastward all 
 the way across, it would be necessary to assign to them a much greater - 
 thickness than that given to division 3 of the section on page 289. 
 Instead of 250 feet, their volume would probably be between 800 and 900 
 feet. This would better accord with the thickness which has since been 
 found by direct measurement to belong to their supposed equivalents in 
 Bonne Bay. 
 
CHAP. XXII.] QUEBEC GROUP. 865 
 
 In the ascending section of the Labrador and Newfoundland rocks given Section, 
 on pages 288-290, the divisions were arranged under the numerals 1 to 
 16. Some of these divisions have since been re-measured in greater detail 
 than before ; while with respect to others, the examination of their equiva- 
 lents in other localities has shown that these divisions include additional 
 strata. In giving these farther results, it will be convenient to designate 
 the divisions by letters, and to indicate the subordinate parts of each by 
 numerals. To facilitate a comparison of the present results with those stated 
 in the previous chapter, a summary of the section already referred to is 
 here given, with the former numerals, but having the letters now to be 
 used, prefixed. The thickness formerly assigned to these divisions, and 
 the localities in which they were observed, are also appended. 
 
 POTSDAM GEOUP. 
 
 Feet. Feet. 
 
 A. 1. Red and grey sandstones, Ance au Loup, . . . . 231 Potsdam 
 
 B. 2. Grey, reddish, and green limestones, " " .... 143 group. 
 
 C. 3. White sandstones, concealed, Strait of Belle Isle, 250 
 
 624 
 
 QUEBEC GROUP. 
 
 D. 4. Grey and reddish magnesian limestones, ... St. Barbe Bay, 150 Quebec 
 
 E. 5. Dark grey limestones, " " 400 group. 
 
 F. 6. Dark grey geodiferous limestones, Port au Choix, .... 400 
 
 G. 7. Dark grey limestones, " .... 130 
 
 H. 8. Greyish-blue limestones, " .... 340 
 
 I. 9. Light yellowish-grey magnesian limestones,.... " " .... 150 
 
 K. 10. Grey and whitish magnesian limestones, Point Rich, 130 
 
 L. 11. Light bluish-grey limestones, " 130 
 
 M. 12. Light bluish-grey limestones, Table Head, 550 
 
 N. 13. Black bituminous limestones, " 200 
 
 2580 
 
 0. 14. Grey calcareous sandstones and black shales, . . . Cow Head, 700 
 
 P. 15. Grey and white limestone conglomerates, " 700 
 
 1400 
 
 Q. 16. Greenish sandstones and red shales, Bonne Bay, 2000 
 
 6604 
 
 Between one and two miles inland from the northeast side of the East 
 Arm of Bonne Bay (page 292), there arises a range of hills of Lauren- Bonne 
 tian gneiss, 2,000 or 3,000 feet in height, on the flank of which is exposed Bay- 
 the following measured section : 
 
 A. Feet. Feet. 
 
 1. Blackish-blue fine grained slate, with a cleavage independent of the bed- Diyirion A. 
 
 ding. Of this slate only 105 feet of the upper part are seen; the 
 lower part is concealed in the space between the upper portion and 
 the gneiss, and may comprise a thickness of about 230 feet, 335 
 
 2. Blackish-blue slate interstratified with grey quartzites, in beds of from six 
 
 inches to three and four feet. In the eighty feet at the bottom, the 
 quartzites greatly predominate, and they constitute fifteen feet at 
 the top, while the intermediate 175 feet consist chiefly of slate, ... 270 
 
 - 605 
 B* 
 
866 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 B. 
 
 Feat. Feet. 
 
 Division B. 1. Light grey yellow- weathering limestone, in beds of from one to three inches 
 thick, interstratified with blackish-blue slightly calcareous slate, 
 both containing small specks of silver-white mica, which are more 
 abundant in the limestone than in the slate. The limestones hold in 
 abundance fragments of trilobites, chiefly belonging to three or 
 four species. Among them is Paradoxides (Olenellus) Vermontana, 
 a new species of Bathyurus, and the pygidium of a species so 
 closely resembling B. extans of the Birdseye and Black River for- 
 mation, that it can scarcely be distinguished from it, and may pos- 
 sibly be the same, 80 
 
 2. Greyish-green micaceo-arenaceous shale, interstratified with a few beds 
 
 of greyish quartzite weathering slightly yellow, 80 
 
 3. Strata concealed, 30 
 
 4. Reddish granular quartzite in thick beds, with numerous parallel joints 
 
 in two directions, dividing the beds into rhomboids, 105 
 
 5. Grey and greyish- green micaceo-arenaceous shale in beds from a quarter 
 
 of an inch to an inch thick, interstratified with a few beds of grey 
 very ferruginous, sandy dolomite, and fewer of grey quartzite, .... 127 
 
 6. Reddish quartzite, in beds of from one to two feet thick, 34 
 
 7. Grey arenaceous dolomite, weathering yellowish-brown, interstratified 
 
 with reddish quartzite, in beds of from one inch to one foot thick, and 
 with reddish and greyish micaceo-arenaceous shale, predominating 
 toward the top. The beds of dolomite and shale contain fossils, 
 among which are Obolella chromatica? Obolus Labradoricus, Para- 
 doxides Vermontana, Conocephalites, a new species of Bathyurus, and 
 
 one or more undetermined species of Salterella, 27 
 
 483 
 
 0. 
 
 Division C. 1. Whitish quartzite in beds of from six inches to two feet, interstratified with 
 light grey micaceo-arenaceous shale, in layers of from six inches to 
 one foot, which occur at intervals of from five to ten feet, 150 
 
 2. White and reddish quartzite, in beds of from one to three feet thick, 
 
 interstratified toward the bottom with a grey arenaceous dolomite, 
 weathering yellowish-brown, 160 
 
 3. White and reddish quartzite, in beds of from one to three feet thick, inter- 
 
 stratified with greenish micaceo-arenaceous shale, constituting 
 about one half the amount, 90 
 
 4. Grey pure limestone, in beds of from one to three feet thick, marked with 
 
 a few reticulating strings of yellowish-weathering dolomite. The 
 rock is a mass of comminuted organic remains, among which are 
 Paradoxides Vermontana,, and undetermined species of Bathyurus 
 and Salterella, as before, 20 
 
 5. Blackish-blue soft shale, interstratified with grey yellow-weathering lime- 
 
 stone, probably magnesian, in beds of one or two inches thick. The 
 quantities of shale and limestone are about equal, and the whole is 
 intersected by reticulating strings of calc-spar, 35 
 
 6. Grey pure limestone, composed of comminuted organic remains, belonging 
 
 to Paradoxides, Bathyurus, and Salterella, as before, 27 
 
 7. Bluish-black soft shale, interstratified with grey yellow-weathering dolo- 
 
 mitic bands as before, 60 
 
CHAP. XXII.] QUEBEC GROUP. 867 
 
 Feet. Feet. 
 
 8. Grey pure limestone, probably composed of comminuted organic remains 
 
 as before ; underlaid by bluish-black shale enclosing nodules of blue 
 compact limestone ; some of which weather yellowish-brown, and 
 are probably magnesian, 13 
 
 9. Bluish-black soft shale of the same character as before, interstratified with 
 
 a few beds of quartzite, 68 
 
 623 
 
 1711 
 
 The summit of the above section occurs on the east side of Deer Brook Eaet Arm, 
 Bay on the East Arm of Bonne Bay, and its base about six or seven miles 
 up the East Arm from the mouth of Deer Brook. All of the beds can be 
 seen coming to the coast in succession, with a westward dip, and an inclina- 
 tion of from twenty to sixty degrees. Where the beds of the base were 
 observed, the measures appear to fold over an anticlinal axis, and for 
 about 100 yards they dip to the eastward. For two miles beyond this, 
 along the east side of East Bay, the greatest confusion prevails, and noth- 
 ing reliable in regard to the sequence can be obtained from the exposures. 
 East Bay and West Bay are two deep southward parallel indentations of 
 the coast, which form the extremity of the East Arm. The area between them 
 is from one to two miles wide, and the strata in it appear to lie in the form 
 of a synclinal. The axis of this synclinal would run about north and 
 south, and in the former direction it would strike to the eastward of the 
 anticlinal just mentioned as occurring on the north side of the East 
 Arm, while the axis of this anticlinal would strike into West Bay. The 
 distance across the East Arm, on the axis of the synclinal, from the posi- 
 tion where the lowest beds of the section above given would come upon it, 
 to the position where it would be crossed by the lowest beds between East 
 and West Bays, would be about the same as that occupied by the whole 
 section between the Laurentian gneiss and the coast of Deer Brook Bay. 
 On the west side of this bay there occur some limestones of a peculiar 
 color and character, whose stratigraphical place would be a few hundred feet 
 above the highest beds in the section just given. About the same distance 
 above the base of the strata between East and West Bays, similar lime- 
 stones occur; and there is therefore not much doubt that the strata 
 between these bays come in immediate or proximate sequence to those 
 already given in the section C. These additional strata are as follows : 
 
 C. Continued. 
 
 Feet. Feet. 
 
 10. White quartzite, in beds of from two to three feet thick, interstratified Division C. 
 
 with striped olive-drab and black compact arenaceous magnesian 
 brown-weathering limestone, which constitutes one fourth of the 
 mass, and holds small disseminated masses of iron pyrites, 58 
 
 11. Strata concealed, 150 
 
868 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 Feet. Feet. 
 
 12. Blackish-grey limestone ; it is divided into beds of from two to eight 
 
 inches, and under the influence of the weather breaks up into thin 
 scales, 54 
 
 13. Smoke-grey compact pure limestone, striped with ochre-yellow arenaceo- 
 
 ferruginous limestone, passing into brick-red. The grey and yellow 
 alternate in lenticular layers, varying in thickness from a quarter to 
 half an inch, and the rock presents a very peculiar and striking 
 aspect. The yellow and red colors may be the effect of weathering, 
 but in breaking up the rock the same alternation of these with the 
 grey limestone was apparent in the interior. Rock of the same 
 character occurs on the west side of Deer Brook Bay, 30 
 
 14. Olive-grey brown-weathering ferruginous sandy dolomite, containing 
 
 thin lenticular patches and thin beds of pure smoke-grey limestone, 
 
 with disseminated cubes and small masses of iron pyrites, It 
 
 308> 
 
 D. 
 
 Division D. 1 . Greenish- white and yellowish-white magnesian limestone,in massive beds, 
 some of which are ferruginous and weather buff, while others re- 
 main unchanged in color. They are interstratified with beds of ash- 
 grey limestone, weathering yellowish, and near the middle with two 
 bands of grey calcareo-arenaceous shale, one of two, and the other 
 of three feet thick. These massive limestones terminate in a four- 
 feet bed of smoke-grey pure limestone in thin layers, interstratified 
 with thin layers of probably magnesian limestone, weathering ochre- 
 yellow. The bed, for the thickness of a foot, is arranged, on the ' 
 strike, in a series of curves or arches, which span from two to three 
 feet, separated by straight intervals, varying from one to two feet. 
 The curved portions appear to hold a greater number of the yellow- 
 weathering layers than the straight parts, and these layers have 
 in general a lenticular form. The top and bottom of the bed are 
 arranged in even layers, which fill up the inequalities of the inter- 
 mediate part, 174 
 
 483 
 
 The surface between East and "West Bays rises into a mountain of 
 500 or 600 feet in height, in which the strata dip in directions conforming 
 to their synclinal arrangement, at angles varying from twelve to twenty- 
 west Bay. five degrees. Proceeding southward along the east side of West Bay, they 
 are seen to accumulate above one another to the amount of 1400 feet, in 
 addition to the preceding section. These higher strata consist almost 
 entirely of limestone of various shades of grey, with two or three bands 
 Divisions E, of black, the latter usually thin bedded. Of the lowest 200 feet, about 
 F, ana G, ^ Q fifths weather to various shades of yellow and brown ; of the succeeding 
 300 feet the proportion of yellow-weathering beds is about one sixth, and 
 in the remaining 900 feet they are but few. If these yellow-weathering beds 
 are, like the similar ones in the detailed section just given, magnesian, it 
 would appear that the proportion of magnesia gradually diminishes in 
 ascending this portion Of the series. In the whole of these 1400 feet, 
 
CHAP. XXII.] QUEBEC GROUP. 869 
 
 which are supposed to represent the divisions E, F, G, referred to on page 
 865, the only strata in which fossils were observed occur at about 400 feet 
 from the top ; where the surfaces of various beds, in a thickness of between 
 ten and twenty feet, are marked by the weathered-out forms of silicified 
 fossils, consisting of undetermined species of Pleurotomaria and Ophileta. 
 
 From West Bay, the strata strike, in a general way, along the coast to 
 the westward : they are much contorted, and it is difficult to make out any 
 true continuous succession of the beds. At the west horn of the bay, 
 however, the whitish massive magnesian limestones of division D occur ; 
 and in the contorted strata for a couple of miles beyond, the peculiarly 
 striped smoke-grey and ochre-yellow thin bedded limestones of C 13 
 are occasionally seen. At the promontory which faces the west horn of 
 Deer Brook Bay, the strata become vertical, or nearly so, but somewhat 
 more regular ; and the absence of any beds weathering yellow or brown 
 appears to indicate a proximity to the horizon of the silicified fossils above 
 mentioned. About 800 feet of dark grey limestones are here exposed, at 
 the summit of which there occurs a bed holding Maclurea, Orthoceras 
 piscatory and Leperditia. Of the genus Maclurea, the opercula were the 
 only parts observed, and these are silicified ; but the bed is supposed to 
 be higher in the series than the band with silicified fossils between East 
 and West Bays, inasmuch as it is immediately followed, not by the dark- 
 grey limestones, but by about 200 feet of light grey limestone ; a good deal 
 of which, although it does not weather yellow, is magnesian. The summit of 
 these 200 feet is fossiliferous, and contains undetermined or undescribed 
 species of Orihis, OpJiileta, Maclurea, Nautilus, Amphion, Asaphus, and 
 Leperditia. The 800 feet are probably comprised in the divisions F and 
 G, while the 200 feet may constitute a part of H. 
 
 The divisions M and N of the Newfoundland rocks have been, in a 
 general way, described from exposures occurring at Table Head. The Table Head, 
 total thickness was here estimated from measurements by pacing, but few 
 details were ascertained ; and the fossils collected having been lost, from 
 the necessity of abandoning them on the coast through stress of weather, 
 it was considered expedient to re-examine the locality. The following section, 
 detailed ascending section is the result. It commences between 600 and 
 700 feet lower than the strata comprised in the division M, or 12, as pre- 
 viously given on page 284, and the lowest part of these additional strata 
 are considered equivalent to some of those at Point Rich. 
 
 H. Feet. Feet. 
 
 1. Bluish-grey limestone in beds of from one to two inches, interstratified 
 
 with grey sub-crystalline yellow-weathering magnesian limestone in Division H. 
 
 beds of from three to six inches thick. The beds are fossiliferous, 
 containing the genera Orthis, Ophileta, Maclurea, Pleuroto- 
 maria, Murckisonia, Orthoceras, and Bathyurus. The described species 
 are Orthis electra ?, Maclurea matutina ?, and Ort hoceras piscator, . . 100 
 
 2. Strata concealed, 165 
 
 265 
 
870 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 I. 
 
 Feet. Feet. 
 Division I. i Light yellowish-grey mottled and sub-crystalline magnesian limestone, 
 
 with geodes of calc-spar. The limestone is divided into beds of from 
 six inches to one foot, and shows occasional fossils, the only 
 
 recognizable species being Maclurea matutina, 65 
 
 2. Light yellowish-grey mottled magnesian limestone as before, interstrati- 
 fied with greyish-black limestone in beds of from three inches to 
 one foot. The magnesian beds contain Maclurea matutina, *70 
 
 135 
 
 K. 
 
 Division K. j. Light grey sub-crystalline limestone, with greyish-black limestone, both 
 in beds of from two to six inches, and associated with a few bands 
 of greyish-white dolomite, from six to nine inches thick ; the whole 
 interstratified at intervals of from ten to twenty feet with black and 
 greyish-green shales. The light grey limestone and whitish dolo- 
 mite are fossiliferous, containing the genera Orthis, Ctenodonta, 
 Ophileta, Maclurea, Pleurotomaria, Murchisonia, and Orthoceras. 
 The described species are Orthis electra } Maclurea matutina, and 
 Orthoceras piscator, 100 
 
 L. 
 
 Division L. l. Greyish-white dolomite and greenish-grey compact limestone, both in 
 beds of from two to six inches thick, interstratified with about 
 three per cent, of black and greyish-green shale, all without observed 
 fossils, 104 
 
 2. Light reddish-grey magnesian limestone, in beds varying from fifteen 
 
 inches to two feet in thickness. The rock breaks from the cliff in 
 which it is exposed, in rectangular blocks of several feet long and 
 wide, and would make an excellent building stone. No fossils were 
 observed, 16 
 
 3. Brownish-grey hard limestone, in beds of from six inches to two feet ; 
 
 Fossils occur at the base, among which are the genera Stenopora, 
 Orthis, Murchisonia, Asaphus, and Leperditia, 65 
 
 4. Reddish-grey magnesian limestone, in beds of from two to six inches, 
 
 without observed fossils, , 6 
 
 191 
 
 M. 
 
 Division M. 1. Brownish-grey limestone in beds, varying in thickness from six inches to 
 six or seven feet; interstratified at distant intervals with reddish-grey 
 dolomite in beds of from three to nine inches, which constitute one 
 or two per cent, of the whole. Both the limestone and the dolomite 
 are fossiliferous throughout ; the organic forms however are obscure 
 in the whole, with the exception of about a foot of the limestone 
 at the base, and six feet at the top, including a bed of the dolomite, in 
 the whole of which the fossils are silicified. The genera at the 
 base are Eospongia, Orthis, Ophileta, Pleurotomaria, Murchisonia, 
 Orthoceras, and Jlsaphus. At the top the same genera occur, but 
 there is a greater number of species, and it is probable that the fos- 
 sils of these two parts represent those of the whole mass, 350 
 
 In the fossiliferous beds of divisions K and L, and in part 1 of M, 
 there are several species of each genus, and the same species seem 
 to range through the whole. The described species are Orthis electra t 
 
CHAP. XXII.] QUEBEC GROUP. 871 
 
 Feet. Feet. 
 
 Maclurea matutina, and Orthoceras piscator ; but the chief part of the 
 species of the remaining gasteropods and cephalopods are so closely 
 allied to some of the common forms of the Trenton group, that it 
 scarcely appears doubtful that they are the same. The most striking 
 resemblances are to Orthoceras Sigsbyi, and O. Jlllumettense of the 
 Birdseye and Black River, and to Murchisonia gracilis, M. bellicinta, 
 and M. perangulata of the Trenton formation. 
 
 2. Bluish-grey limestone, in beds varying from six inches to ten feet in thick- 
 ness, the thicker beds being made up of layers of one or two inches, 
 distinguishable in section by slight differences in color, but without 
 any tendency to separate. Some of the beds are nodular, and crum- 
 ble under atmospheric influences. Fossils are abundant in all the 
 beds, but are not readily separated. They consist chiefly of Steno- 
 porafibrosa, Orthis, like O. Platys, Rhynchondla allied to R. plena, 
 Camerella varians, new species of Maclurea, and Orthoceras ; with 
 O. piscator, 0. Allumettense ?, 0. Bigsbyi ?, jlmphion, JLmpyx, dsaphus, 
 Illeenus, and Leperditia, 308 
 
 658 
 
 N. 
 
 1. Blackish-grey nodular fossiliferous limestone, in beds of from one to three Division N. 
 
 inches thick, becoming bituminous toward the top. The fossils are 
 Orthis, Strophomena, Rhynchonella allied to R. plena, a new species 
 of Camerella, Orthoceras piscator, 0. Jlllumettense ? jJmphion, Jlsa- 
 phus, Holometopus Angelini, Illcenus, and Leperditia, 81 
 
 2. Black bituminous limestones, in beds of from one to three inches thick, 
 
 interstratified with fine brittle black bituminous shale in layers vary- 
 ing from a quarter of an inch to three inches. The prevailing fossils 
 are Stenoporafibrosa, Lingula allied to L. Philomela, Orthis, Stropho- 
 mena, Rhynchonella allied to R. plena, a new species of Camerella, 
 with C. varians, Orthoceras, jlgnostus, Jlmphion, dmpyx, Jlsaphus, 
 Endymion Meeki, Holometopus Jlngelini, Illcenus, Nileus scrutator, and 
 Leperditia, 174 
 
 3. Black bituminous shale, with Graptolithus, Lingula, Orthoceras, and 
 
 Paradoxides or Olenellus, 22 
 
 277 
 
 1626 
 
 The grey, yellowish, and greenish-white magnesian limestones of division Bay st. 
 D of the Newfoundland section, occur at Bay St. Barbe. The dark grey Barbe 
 limestones, interstratified with yellow-weathering magnesian beds, of divi- 
 sion E (5 on page 289), which succeed, occupy a valley which runs obliquely 
 into the land in a direction about 1ST. E. This is the bearing of the strike, 
 and in it a similar valley comes out upon the coast, about twenty miles 
 from Anchor Point, just beyond West Point. From this point to Cape 
 Norman, and to the east side of Pistolet Bay farther on, the chief part of Pistoiet Bay. 
 the coast was examined in detail. A thin bedded argillaceous limestone 
 occurs in the bay, at West Point, holding a small Lingula ; but in the thirty 
 miles between this and Cape Norman, no organic remains were observed. 
 The rocks consist of dark grey limestone, interstratified with grey yellow- 
 weathering magnesian bands, and present a series of low escarpments along 
 
872 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 the coast. The dip of the strata is about S. 45 E. < l-4 and the bearing 
 of the coast about N. 60 E. In this bearing the strata accumulate above 
 one another, all the way, and the thickness is estimated to be between 
 cape Nor- 400 and 600 feet. At Cape Norman the bearing of the coast changes to 
 one more nearly transverse to the measures, which, after a short distance 
 become affected by undulations. Southeastward from the strike of the beds 
 of Cape Norman there are accumulated between 300 and 400 feet of strata 
 above the preceding, consisting of dark grey limestones, without observed 
 fossils ; but at the summit of these there occur about twenty feet of dark 
 grey and light reddish-grey limestones, interstratified with one another, 
 which are marked by the occurrence of the genera Ophileta, Maclurea, 
 Pleurotomaria, Murchisonia, Ortkoceras, Piloceras, Nautilus, and Bathy- 
 urus ; the only described species being Piloceras Canadense. Many of the 
 species are identical with, and others strongly resemble, those of division 
 H of the Port au Choix rocks. In lithological character and paucity of fossils 
 the strata from West Point to Cape Norman resemble those of divisions 
 E and F of Bay St. Barbe, and there seems little doubt that the whole 
 series is an unbroken repetition of the four divisions E, F, G, and H. 
 
 The position of the fossiliferous strata just mentioned is about 100 feet 
 over the level of the sea, and they appear to strike for about the south corner 
 ^ormau of Norman Cove. They dip at a small angle to the northwestward ; and 
 for about three quarters of a mile to the southeast of them, the strata 
 exposed are either flat, or dip at about the same rate and in the same direc- 
 tion as the fossiliferous beds, until reaching the next cove southeastward of 
 Norman Cove. Here, after a short interval of concealment, there occurs 
 an exposure of about ten feet of black bituminous shales. These beds con- 
 tain the genera Grraptolithus, Orthis, Lingula, Agnostus, Ampyx, Triar- 
 thus, Holometopus, Endymion, Cheirurus ?, and Paradoxides or Olenel- 
 lus. The described species are Holometopus Angelini, and Endymion 
 Meeki. In most of their species, and in their lithological characters, these 
 beds strongly resemble those of parts 2 and 3 in division N of the Table 
 Head section ; and there is not much doubt that the two series are on the 
 same horizon. Such being the case, there must be a dislocation between 
 the north and south sides of the cove, throwing the measures down about 
 1400 or 1500 feet on the southeast side. 
 
 The visible breadth of the black limestones and shales is about twenty 
 yards ; and on the southeastward side they are overlapped by bluish-grey lime- 
 stone, between which and the black beds there appears to be a fault, with 
 &n underlie to the southeastward at an angle of ten degrees. This lime- 
 stone presents a confused and ragged surface, on which no evidences of 
 stratification were observed for a breadth of three quarters of a mile, and 
 only .occasional obscure indications of stratigraphical divisions for a quarter 
 of a mile farther. These obscurely marked beds dip at angles varying from 
 
CHAP. XXIL] QUEBEC GROUP. 873 
 
 sixty to ninety degrees, and sometimes on one side and sometimes on the 
 other of the strike ; which, with many irregularities, is, on the average, 
 about N. E. In the obscurely stratified part of the rock, fossils are met 
 with in three or four spots : the genera are Orthis^ Ophileta, Maclurea^ 
 Pleurotomaria, Murchisonia, Orthoceras, Amphion, and Leperditia. All of 
 the species are identical with those occurring in division M of the Table 
 Head section, the most characteristic having the peculiarity of an identity 
 or close alliance with forms of the Trenton group. The Orthis resembles 
 0. platys, and this, at Table Head, is not found lower than part 2 of the 
 division M. 
 
 This rock forms the whole of the west coast of Pistolet Bay, and the 
 fossiliferous part observed is opposite to Schooner Island, from which it is Schooner 
 distant about a mile. At the southwest point of this island, between high 
 and low water mark, there is a small exposure of black graptolitic slates, 
 following grey slate interstratified with grey sandy limestone ; and there 
 may probably be a run of these rocks along the northwest side of the island. 
 They are succeeded by dark grey limestone , which occupies the whole of 
 the island, with a southeast breadth of three quarters of a mile. In the 
 northwest half of this the rocks present a confused and ragged surface, 
 without any indication of bedding ; but in the remainder the stratifi- 
 cation is sufficiently distinct. The beds are from an inch to a foot in 
 thickness, and they dip irregularly to the southeast at angles varying from 
 two to twenty degrees. Fossils occur in the rock on the southeast side of 
 the island, the genera being Eospongia, Ophileta, Mcalurea, Pleuroto- 
 maria, Orthoceras, Nautilus, and Piloceras. They resemble those of the 
 neighborhood of Norman Cove, and the rock is probably a repetition of the 
 divisions H and I (8 and 9 on pages 289 and 290) of the Port au Choix 
 beds, brought up by a great fault on the northwest side of the island. 
 
 The same rock occurs on the peninsula at Burnt Cape, on the opposite side Burat Ca P e - 
 of Pistolet Bay, the distance across being about four miles. On the west 
 side of the peninsula between high and low water mark, there is a breadth 
 of between forty and fifty yards of grey and greenish slates, interstratified 
 with dark grey brown-weathering sandy magnesian limestone in beds^ of 
 from one to four inches, and occasionally a foot in thickness. They dip 
 about S. 70 E. < 32. They are followed by a mass of grey limestone, 
 which rises into a cliff of about 100 feet high, and for a breadth of about' a 
 quarter of a mile shows a ragged surface, with no divisions into beds. The 
 limestone weathers to a mottled black and white. The black parts, although 
 holding more lime, yield more slowly to the atmosphere than the white, 
 which appear to owe their color to the presence of grains of white sand. 
 This mass is followed by about an equal breadth of bluish-grey limestone, 
 which rises over the last in an escarpment of about fifty feet. It is 
 divided into beds varying in thickness from six inches to several feet, and 
 
874 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 dips about S. 70 E. < 5-10. Both of these limestones are character- 
 ized by fossils. Those in the western mass are few and obscure ; they con- 
 sist of Orthoceras, and Piloceras Canadense : while those in the eastern 
 are well defined, and more numerous ; the genera being Orthis, Ophileta, 
 Madurea, Pleurotomaria, Murchisonia, and Orthoceras. The latter show 
 the peculiar species belonging to M 2, of Table Head ; while the former 
 are similar to those of divisions H and I of Port au Choix. 
 
 On the narrow isthmus joining the Burnt Cape peninsula with the west 
 shore of Pistolet Bay, and separating the waters of this from those of 
 Ha-ha Bay, the limestones, M 2, on the east side of the peninsula, become 
 covered over by blapk and dark grey slates, interstratified with dark 
 brown-weathering very sandy magnesian limestones, resembling the strata 
 on the west side of the peninsula, and those on the west side of Schooner 
 
 Pistolet Island. These strata line the east side of Pistolet Bay for upwards of two 
 miles to the southward of the isthmus. Their dip is irregular : its direc- 
 tion varies from N. E. to S. E., but on the average it may be about 
 S. 80 E. < 2-50. About 200 feet above the limestone of the penin- 
 sula there appear on the surface of one of the beds impressions of grapto- 
 lites. From the recurrence of these slates in this position, it seems probable 
 that between their equivalents, and the limestone on the west side of the 
 peninsula, there is a great upthrow fault. Whether there is any disloca- 
 tion coincident with the escarpment which runs along the middle of the penin- 
 sula, is uncertain. The breadth of these slates is upwards of a mile : they 
 have a well-marked and regular cleavage, but the dip of the stratification, 
 though sufficiently distinct, is very irregular both in direction and inclina- 
 tion ; the former varying from N. E. to S. E., and the latter from five to 
 thirty degrees. It is in consequence difficult to estimate their thickness, 
 but it can scarcely be much under from 750 to 1000 feet ; and they may 
 represent the strata of division 0, which are numbered 14 in the section 
 given on page 290, and were there described as consisting of grey cal- 
 careous sandstones, interstratified with greenish and black slates, which 
 predominate toward the top. 
 
 The slates on the east side of Pistolet Bay are dark grey, sometimes 
 greenish, and are striped with thin bands of black. They are silicious 
 rather than argillaceous, and have a considerable degree of hardness. 
 Resting upon them in conformable stratification, and thus apparently occu- 
 
 section. pying the place of division P (15 of page 291), is the following succession 
 of beds, in ascending order : 
 
 Feet. 
 
 1. Olive-green fine grained calcareous diorite, traversed by seams of white 
 quartz, and distinctly marked on the transverse surfaces by numerous 
 small waved lines, which show the stratification. These are due to 
 laminae of a dark green chlorite-like mineral, resembling that in the 
 diorite of Upton (page 604), to which portions of this mass bear a 
 close resemblance, 30 
 
CHAP. XXII.] 
 
 QUEBEC GROUP. 
 
 875 
 
 Feet. 
 
 Diorite. 
 
 Black 
 slate. 
 
 2. Greyish-green diorite, gneissoid in structure, with numerous transverse 
 
 joints, which are filled with white quartz. It cleaves readily with the 
 elemental layers into thin plates, which are coated with films of a 
 dark green chloritic mineral. Some of the layers are chiefly composed 
 of a greenish-white compact feldspar, while others have a porphyritic 
 aspect from the presence of uncleavable feldspar grains in a blackish- 
 green base, ................................................... 20 
 
 3. Fine grained feldspathic rock, striped with narrow bands of black and 
 
 greyish-green. The former portions are sub-translucent, with a scaly 
 fracture, a feeble waxy lustre, and weather opaque white. Interstrati- 
 fied with this mass are bands of from one to two inches of a similar 
 feldspathic rock, greyish-white, sub-translucent, impalpable, and with 
 a conchoidal fracture. Like the greenish portions, it weathers opaque 
 white, and has the aspect of an amorphous triclinic feldspar, ....... 15 
 
 4. Fine grained black slate, with thin dark grey bands. It resembles the 
 
 slates at the base of this section, but has nearly the hardness of quartz, 
 and besides its slaty structure, has a conchoidal fracture. It is inter- 
 stratified with bands of from one to six inches of -granular diorite, in 
 which the feldspar greatly predominates. Their color is greyish, with 
 greenish layers which resemble the lighter colored portions of 2. Thin 
 bands of serpentine, like those of 6, are also interstratified with these 
 slates. Along the outcrop, numerous graptolites were found in loose 
 masses of a black slate apparently identical with that of the band,. . 30 
 
 5. Fine grained greenish feldspathic rock, with blackish-grey streaks and 
 
 clouds. It much resembles 3, but encloses flattened pebbles of an 
 apparently unaltered bluish-grey limestone, which are sometimes two 
 inches in length, .............................................. 6 
 
 6. Dark olive-green or blackish-green serpentine in layers, from a few 
 
 lines to more than two inches in thickness, interstratified with similar 
 bands of greenish-white diorite. The serpentine contains small plates 
 of diallage, in addition to which, thin layers, composed chiefly of small 
 crystalline grains of black hornblende, are occasionally interposed 
 between the serpentine and the greenish-white material, and in some 
 parts forms bands of half an inch in thickness. The serpentine is cut 
 by transverse joints, which are lined with films of what appears to 
 be chlorite, ........................................... . ....... 20 
 
 121 
 
 These rocks are immediately succeeded by a mass estimated at about 
 1000 feet in thickness, consisting in part of a blackish-green serpentine, 
 holding diallage, and in part of a fine grained dark olive-green diorite ; 
 which is traversed by thin irregular seams of carbonate of lime, and 
 resembles somewhat the parts 1, 3, and 5 of the above section. The 
 serpentine of this mass, like that of the Quebec group in Eastern Canada, 
 contains small portions both of chrome and nickel ; and these metals were chrome and 
 also detected by analysis in two of the thin bands of serpentine from part mckel - 
 6 of the section.* The white layers interstratified with this are, unlike the 
 
 * In addition to the chrome and nickel which these serpentines have in common with 
 similar rocks of the same age in Eastern Canada, it is worthy of remark that copper 
 ores, with specular iron, have been found associated with the serpentines of Newfound- 
 
 Conglom- 
 erate. 
 
 Serpentine. 
 
876 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 serpentine, but partially decomposed by sulphuric acid, which however 
 takes up a large amount of alumina, with some protoxyd of iron, a little 
 lime, and much magnesia, leaving an undecomposed granular silicate. 
 
 Succeeding to these serpentines and diorites, there is a great develop- 
 ment of massive greenish chloritic sandstones, which often become suffi- 
 ciently coarse grained to constitute conglomerates, with white quartz pebbles 
 attaining occasionally half an inch in diameter. The thickness of this mass, 
 though not determined, must be considerable, as the- rock occupies a 
 breadth of several miles, and there is not much doubt that it represents 
 the Sillery division of the Quebec group. 
 
 Dislocations. Of the four dislocations on Pistolet Bay, one, as already stated, is a 
 downthrow, while the other three are upthrows to the southeast. The 
 absence of stratification in each of the masses of limestone on the upthrow 
 side of these three faults, is probably occasioned by the grinding of the 
 strata in the movements occurring at the time of displacement, and by 
 the subsequent cementing of the mass by the infiltration of carbonate of 
 lime. In one of the faults it is very evident that the unstratified limestone 
 overlaps the black shales in contact with it, at an angle of five degrees to 
 the plane of the lower beds, or of ten degrees to the horizon; and some- 
 thing analogous may occur in connection with the other faults. In this, 
 the dislocations would resemble those of Quebec and of Phillipsburgh. All 
 of these faults have a southwest bearing, and run with the general strike ; 
 and it appears not improbable that some of them may have a connection 
 with the faults which are noticed on page 292 as occurring between St. 
 John's Island and Bonne Bay. These dislocations are there described as 
 probably transverse to the measures ; but farther investigation induces the 
 supposition that they run with the strike, or nearly so. They are all 
 upthrows on the southeast side. 
 
 The most northerly of the disturbances in this part appears to be an 
 
 land, and resembling the ores of the Quebec group in the Eastern Townships. A beau- 
 tiful variety of steatite, holding traces of nickel, and colored emerald-green by oxyd of 
 nickel, occurs with these serpentines. In this connection it may be noticed that in 
 addition to the copper, lead, cobalt, nickel, arsenic, chrome, silver, and gold, already 
 Antimony, described, antimony is now to be added to the mineral wealth of the Quebec group. A 
 deposit of this metal has lately been discovered in the township of South Ham, on the 
 twenty-eighth lot of th.e range east of the Gosford road. It is described as occurring in 
 a vein or bed, of from six to sixteen inches in thickness, in argillite, which is penetrated 
 by numerous smaller veins of the ore. The greater portion of the antimony is in the 
 metallic state, as lamellar, or more rarely, as finely granular native antimony ; but the 
 sulphuret, antimony glance, also occurs in small radiating prismatic crystallizations. 
 Besides these, the white oxyd of antimony, both massive and fibrous, is found in 
 this locality, associated with small crystalline tufts of the red oxysulphuret of anti- 
 mony, kermesite. These latter ores are probably only the results of superficial oxyda- 
 tion. From the specimens already obtained from this locality, it would appear prob- 
 able that antimony exists here in workable quantity. It is accompanied by quartz and 
 a little brown-spar. 
 
CHAP. XXII.] QUEBEC GROUP. 877 
 
 undulation in the measures, rather than a fault, the axis of which would 
 run on the inside of St. John's Island, and through Point Rich. The influ- 
 ence of this undulation is visible in the turn of the strata between Port au 
 Choix and Point Rich, and in the attitude of the limestone composing a 
 small island about 100 yards southeast of that of St. John, where for a 
 breadth of 275 feet the beds are turned up to the dip N. 40 W. < 33. 
 This undulation gives to the area between it and the north shore of the 
 Strait of Belle Isle the form of a trough, the axis of which would run 
 through the Island of St. John. The second disturbance occurs at Port 
 Saunders, near the entrance to Hawke's Bay ; and as it brings the division Hawke's 
 F, on the southeast, against L on the northwest, it would appear to be a Bay ' 
 break of about 1200 feet. What is supposed to be a continuation of this 
 break occurs about a mile and a half inland, opposite St. John's Island ; 
 where the division Gr, on the northwest, is brought against some of the quartz- 
 ites in the upper part of the Potsdam group, on the southeast. The rela- 
 tion of the two points at which the break has been observed would give to 
 it a bearing not far removed from northeast. The third disturbance has 
 already been alluded to as occurring on the shore, a little southeast of 
 Table Head. Its continuance is seen near the head of Hawke's Bay, where 
 the division E, on the northwest side, comes against the white quartzites 
 of the Potsdam group on the southeast ; and again about six miles inland 
 opposite St. John's Island. Here the quartzites of the Potsdam group 
 are exposed in nearly horizontal strata on both sides of the fault ; but on 
 the southeast they show an escarpment rising quickly to a height of a 
 thousand feet, and maintaining for ten miles a straight course in the bear- 
 ing of the fault, which seems to be nearly if not quite parallel with the 
 previous one. The upthrow is estimated to be about 1300 feet. A fourth 
 disturbance has already been mentioned as occurring at Portland Creek, 
 but no especial facts have been ascertained to determine its bearing. A 
 fifth is the anticlinal seventeen miles south of Portland Creek, mentioned 
 on page 292 as affecting the limestone conglomerates of division P, and 
 as running between Steering Island and Cow Head. 
 
 On a further examination of the strata of Cow Head, Oheirurus and Cow Head. 
 Lichas were added to the genera previously met with in the limestones ; 
 and in the black shales were obtained several additional species of Grap- 
 tolitidae, among them Phyllograptm typus and P. angustifolius. Between 
 Cow Head and Bay St. Paul, a distance of three miles, no rocks are 
 exposed on the coast; but the limestone conglomerates appear again 
 about a mile and a half within the bay, on the north side. Here in a 
 small anticlinal hillock, a band of the conglomerate is associated with 
 black and greenish shales, in which graptolites are obscurely seen. About 
 a mile farther in, the bay is divided into two parts by a strait called the 
 Narrows ; and while the outer part is about two and a half miles long, 
 
878 GEOLOGY OP CANADA. [CHAP. XXIL 
 
 and shallow, the inner is five miles long, from one to two wide, and very 
 deep. On both sides, at the Narrows, there are exposures of conglomerate, 
 interstratified with thin bedded light grey limestones, and black calcareous 
 
 Graptoiites. shales. In the limestones occur obscure specimens of Graptolithus, with 
 better preserved specimens of Orthis, Lingula, Ophileta, and Leperditia'; 
 while in the shale the graptolites are abundant and well preserved. 
 Among them are G-raptolithus bryonoides, and several other species, with 
 Dictyonema. South of the Narrows, on the inner bay, there are several 
 exposures of limestone conglomerate, interstratified with red and green 
 shales, and greenish-grey sandstones, in beds varying in thickness from six 
 inches to a foot. With the red shales are associated a few beds of red 
 limestone, and others of a greyish limestone, weathering yellow, and probably 
 magnesian. The conglomerates run along the shore from Bay St. Paul to 
 Broom Point and beyond. They are said to compose Martin's Point and 
 Green Point ; and being found farther on running along the north shore of 
 Bonne Bay, from the mouth to the entrance of the East Arm, it appears 
 probable that their strike coincides with the coast the whole way. 
 
 st. Paul's About a mile and a half from the head of St. Paul's Bay, on the south 
 side, there occurs an exposure of thick bedded grey limestone running 
 nearly north and south, in an almost vertical attitude. It has a breadth of 
 about 400 feet, and comes in contact, on its east side, with Laurentian 
 
 Laurentian gneiss. Of this there is an exposed breadth of about 100 yards, which is 
 followed by a mass of brownish limestone, weathering yellow. This lime- 
 stone has a breadth of about 140 yards, and presents a rough jagged sur- 
 face, without any indications of bedding. On the east side it is succeeded 
 by the gneiss, which rapidly rises into a mountain, attaining a height of prob- 
 ably 2000 feet in the distance of a mile. This mountain belongs to a range, 
 which, southwardly, attains the position where it has already been mentioned 
 in Bonne Bay ; and in an opposite direction it holds a course which brings it 
 to a point about sixteen miles east of Table Head ; the whole distance along 
 which it is seen being about seventy miles. In the grey limestone which 
 is at the foot of the range in Bay St. Paul there are a few obscure fossils, 
 the genera of which appear to be Ophileta and Ecculiomphalus. The lime- 
 stone here in contact with the gneiss is supposed to belong to division E ; 
 while on Deer Brook, about sixteen miles to the south, the whole thickness 
 of the Potsdam rocks (about 2000 feet) intervenes between the two. This 
 would appear to indicate a fault, but no facts were observed on the coast 
 to correspond with such a break. The position where such a fault, if it 
 should run parallel with the others, would come upon the coast, was however 
 but imperfectly examined. 
 
 If the thickness of the strata under the strait of Belle Isle be assumed 
 to be 800, instead of 250 feet, agreeably to what has already been proposed, 
 a comparison between the vertical sections of the fossiliferous rocks of this 
 
CHAP. XXII.] 
 
 QUEBEC GROUP. 
 
 879 
 
 region, as ascertained in 1861 and in 1862, will be as given in the following TWO sections 
 table. In this the letters already used are prefixed to those portions com P ared - 
 which are supposed to be approximately equivalent, and the localities in 
 which the strata have been measured, are designated. The two vertical 
 black lines show, by the breaks in them, the interruptions in the continuity 
 of the different parts of the series. The upper part of the Table Head 
 portion, and the whole of that at Cow Head, are common to the two 
 sections. 
 
 A 
 
 1861. 
 Anse au Loup,. . 
 
 Feet. Feet. 
 231 
 
 Bonne Bay, 
 
 1862. 
 Feet. Feet. 
 605 
 
 B 
 
 tt 
 
 143 
 
 
 
 . . . 483 
 
 c 
 
 Belle Isle Strait, 
 
 800 
 
 a 
 
 932 
 
 D 
 
 St. Barbe Bay, . . 
 
 1174 
 150 
 
 
 
 2020 = POTSDAM GROUP. 
 174 
 
 E 
 
 
 
 400 
 
 
 
 500 
 
 F 
 
 Port auChobr,.. 
 
 400 
 
 
 
 500 
 
 G 
 
 it 
 
 130 
 
 CI 
 
 400 
 
 H 
 I 
 
 it 
 ti 
 
 340 
 150 
 
 Table Head, 
 u 
 
 265 
 . 135 
 
 K 
 
 Point Rich, . . . 
 
 130 
 
 11 
 
 . . 100 
 
 L 
 
 it 
 
 130 
 
 It 
 
 . . 191 
 
 M 
 
 Table Head, . . . . 
 
 550 
 
 11 
 
 658 
 
 N 
 
 a 
 
 200 
 
 It 
 
 277 
 
 
 p 
 
 Cow Head, 
 
 
 700 
 700 
 
 Cow Head, . 
 
 
 700 
 700 
 
 
 
 3980 
 5154 
 
 
 460o = QUEBEC OROUP. 
 6620 
 
 The Paradoxides in the divisions A, B, and C of this series, and many 
 of the lithological characters of these divisions, leave little doubt that this 
 part belongs to the same horizon as the Red sandrock of Vermont (page 
 281). The graptolites, both simple and compound, of and P, with the 
 general structural aspect of these divisions, leave as little doubt that this 
 portion is equivalent to the strata of Point Le'vis ; while at the same time it 
 contains in some abundance Maclurea ponder osa, one of the thick-shelled 
 and peculiar gasteropods which so strongly mark the conglomerates of 
 Stanbridge. Though the organic remains of the intermediate part, inclad- 
 ing divisions from D to N, are different from those of the Phillipsburgh lime- 
 stones, yet the latter agree with this middle portion of the Newfoundland 
 rocks in containing fossils of the Calciferous formation ; those of New- caiciferous 
 foundland belonging to the base, and those of Phillipsburgh to the summit formation - 
 of this formation. It is thus evident that we have in the Newfoundland 
 series, the Potsdam and the Quebec groups, and that the latter there 
 overlies the former. This might be considered sufficient to establish 
 that the Phillipsburgh and Stanbridge series is younger than the Red 
 sandrock of Vermont ; and it has been shown by the details already given 
 
880 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. XXII. 
 
 Sillery 
 formation. 
 
 in regard to the structural arrangement in the neighborhood of Phillips- 
 burgh, that there is no stratigraphical evidence to contradict this conclusion. 
 The horizon of the Point LeVis rocks is that assigned to the diorites and 
 serpentines of the Eastern Townships ; and this appears to be the strati- 
 graphical place of the diorites and serpentines of Pistolet Bay, where the 
 metamorphic strata show evidences of association with the graptolitic slates 
 of the Newfoundland series. The sandstones which succeed to the serpen- 
 tines of Pistolet Bay would thus appear to occupy the horizon which has 
 been provisionally assigned to those of the Sillery formation near Quebec. 
 Farther research however is yet required to establish the true relation of 
 this formation to the Quebec group. 
 
 GASPfe LIMESTONES AND SANDSTONES. 
 
 Four anti- 
 cliuals. 
 
 The additional information which has been obtained during the past 
 season in regard to these rocks, refers to their distribution in an area 
 eastward of a line running southward up the Magdalen, and its tributary 
 the Cold Water Brook, and extending to the valley of the Douglastown 
 River. Their distribution in this area is already partially described on 
 pages 406-410 ; where it has been stated that three anticlinal axes run from 
 the coast into the interior ; the most northern starting from Cape Haldi- 
 mand, the second from Tar Point, and the third from Point Peter ; while a 
 fourth was ascertained to coincide with the valley of the Douglastown 
 River for twenty-five miles of its course, and to reach within thirteen 
 miles of its mouth. It was further stated on page 409 that the Haldimand 
 anticlinal was probably continued in one occurring near the source of the 
 Cold Water ; and on page 410, that the axis of the Tar Point anticlinal 
 would probably coincide with the valley of the York River for fifteen miles 
 above Silver Brook. In each of these cases the course of the axis of the 
 anticlinal, as will be shown presently, is more northward than that which 
 was assigned to it. 
 
 It has been shown on page 406 that the Gaspe* limestones are traceable 
 from Little Gaspe* Cove, on the north side of the Northwest Arm, and its 
 tributary the Dartmouth River, for twenty-four miles, to a north turn in the 
 upward course of this stream, not far from Serpentine Mountain. The bear- 
 ing of the limestones in this distance is about N. 30 W., and they have now 
 been followed upwards of sixteen miles farther in the same direction, along 
 Dartmouth the south side of the valley of the Dartmouth ; where they form the flank and 
 River ' crest of a conspicuous mountain range. At the extremity of this distance 
 the mountain range is intersected by a deep transverse valley, which holds 
 the upper part of the Dartmouth River ; and the limestones have been 
 traced between one and two miles on the west side of this transverse 
 
CHAP. XXII.] GASPti SERIES, 881 
 
 valley, where they continue in the same bearing as before. They here 
 constitute a mountain, divided into two parallel ridges, in the northern one 
 of which the limestones dip to the south ; while in the southern they appear 
 to be nearly vertical, with a probable dip to the north. On this part of the 
 Dartmouth, the northern outcrop of the limestones is about three miles north 
 of the strike of the south-dipping limestones of Terrace Mountain ; and as 
 the Two-ridged Mountain dies down before reaching the Magdalen, and its 
 limestones disappear in this direction, it is inferred that they first fold upon 
 a synclinal, and then upon an anticlinal axis, before joining those of Terrace 
 Mountain. The anticlinal appears to be a continuation of that of Cape Hal- 
 dimand ; the effect of which, in the intermediate distance, is seen in several 
 places. Between Gaspe* Basin and Mount Serpentine, it brings up the lime- 
 stones through the sandstones in three or four mountain-tops along the range 
 which flanks the south side of the Dartmouth, Mount Serpentine, which Mount 
 presents an area of between two and three miles belonging to the Quebec erpen 
 group, is flanked on the south by a margin of the limestones, and on the 
 north by the sandstones. Its presence in this place seems to be due 
 partly to the effect of the anticlinal, and partly to the inequalities of the 
 ancient sea-bottom on which the limestones were deposited. The limestones 
 have been observed a short distance to the west of this area, and it is possi- 
 ble that they may be brought to the surface on the crown of the anticlinal 
 all the way to its intersection by the Dartmouth. The measured thickness 
 of the Gasp limestones at the falls in the north turn of the Dartmouth, 
 north of Mount Serpentine, is about 2000 feet. At this place, and along 
 the Dartmouth, the strata at the base are of a somewhat soft and arenaceous 
 character, and occasionally pass into flaggy calcareous sandstones fit for 
 scythe stones. Both varieties are different shades of bluish-grey, and Limestone, 
 weather to a brownish-grey. In the arenaceous limestones of the neigh- 
 borhood of the falls, some of which are nodular, fossils occur. Among 
 them are undetermined or new species of Orthis, Strophomena, and Mur- 
 chisonia, with a branching coral. In a band of arenaceous limestone at about 
 the same horizon, on Eden's Brook, between seven and eight miles higher 
 up the valley, two undetermined species of lamellibranchiate shells occur 
 in a good state of preservation ; and hi a similar but finer grained and softer 
 bed at the bend near the Two-ridged Mountain, Strophomena rhomboid- 
 alls is found in abundance, associated with an undetermined coral. Above 
 the arenaceous limestones, the escarpment is composed of dark grey hard 
 flaggy limestones and shales, with several hundred feet of hard limestone 
 toward the top ; but in these parts no fossils were observed. 
 
 The sandstones on the north side of Mount Serpentine, are a continu- Gaspe- Bay 
 ation of those occupying the Gaspe* Bay synclinal (pages 396 and 406) ; 
 and like them, are characterized by a multitude of carbonized fragmentary 
 remains of land-plants, among which Psilophytonprinceps is the most abun- 
 
 F * 
 
882 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 dant. From the presence of fragments of the sandstones in the channels of 
 various north-flowing brooks, intersecting the limestone on the south side of the 
 Dartmouth, and joining this river, it appears probable that these rocks are 
 continued in this synclinal some thirteen miles farther. A brook flowing 
 parallel with the others, and joining the Dartmouth about three miles below 
 the Two-ridged Mountain, is free from these fragments of sandstone, and 
 may therefore mark the northwestern limit of the Gasp6 sandstones in this 
 synclinal. In the valley of the Dartmouth, for the sixteen miles below the 
 Two-ridged Mountain, the limestones are underlaid by rocks resembling 
 Quebec those of the Quebec group. They consist in the lower part of the distance 
 of one or two exposures of sandstone like that of the Sillery series, and in 
 the upper part, of limestone conglomerates resembling those of Point LeVis. 
 Black Black slates accompany the conglomerates, and in these are occasionally 
 interstratified thin lenticular bands of fibrous limestone like those of the 
 Chatte River (page 420). These may belong to the lower black slates, 
 which are supposed to underlie the Quebec group (page 266). In one of 
 these bands there was met with an imperfect trilobite, very much resem- 
 bling Paradoxides Harlani. It shows the glabella, part of the right cheek, 
 and nine segments of the thorax, and would, if complete, be about four 
 inches long. The imperfection of the specimen however is such, that it 
 may possibly be a Dalmanites instead of a Paradoxides. 
 
 Haidimand The Cape Haldimand anticlinal having thus been shown to run between 
 anticlinal, ^e Two-ridged Mountain and Terrace Mountain, the Tar Point anticlinal, 
 which is the next to the southward, would be the one corresponding with 
 that near the source of Cold Water Brook. Its course between Tar 
 Tar point Point and this brook, would carry it obliquely across the mouth of the 
 anticlinal. p ou gi a gtown River, and that of the York River. It would come upon 
 Silver Brook about two miles from the junction of this tributary with the 
 rork York River, and at this place the Gaspe* sandstones present an anticlinal 
 arrangement which serves to confirm the course given to the axis. This 
 position is about a mile north of the oil-spring mentioned on pages 403 
 and 789. The Gasp6 limestones and sandstones on the Cold Water, on the 
 north side of this anticlinal, and the corresponding limestones on the south 
 side, on York River, have been mentioned on page 408. The breadth of the 
 latter is about a mile and a half, and they are visibly limited to the south by 
 the overlying sandstones ; which occupy a breadth of about two miles on a 
 south-flowing part of the river, and display a synclinal arrangement between 
 the limestones just mentioned, and another development of the same series, 
 brought up by the next anticlinal, which is that of Point Peter. The 
 position where the Gaspe* limestones of this part would sink beneath the 
 overlying sandstones to the eastward, on the axis of the Tar Point anticlinal, 
 has not been ascertained. Exposures of the limestone occur on the upper 
 part of the Dartmouth River, between eight and nine miles to the eastward 
 
CHAP. XXII.] GASPE SERIES. 383 
 
 of the most southern exposures on the Cold Water, and others about three 
 miles a little south of east from those just mentioned on the Dartmouth. 
 The limestones on the York River, subordinate to the Tar Point anticlinal, 
 are exposed on the strike for upwards of three miles ; and combining the 
 bearings thus ascertained on the opposite sides of this anticlinal, it seems 
 probable that the limestones would meet somewhere about six miles to the 
 westward of the sandstones on Silver Brook. 
 
 Assuming that the Point Peter anticlinal runs from the coast in a Point Petr 
 course nearly parallel with that of Tar Point, it would cross the Douglas- anticlinal - 
 town River about two miles west of the western limit of the township of 
 York ; and in this bearing it would reach the York River about five miles 
 above the northwest corner of the same township. On the south side of 
 the river at this place, a mass belonging to the Gaspe* limestones comes to Limestone 
 the surface, presenting a sharp anticlinal form. The rock is strongly 
 bituminous, giving indications of petroleum, and measures 167 feet across. 
 It is flanked on each side by the sandstones of the Gaspe* series, and prob- 
 ably shows a position on the crown of the Point Peter anticlinal, between 
 which and the exposures already alluded to as brought up by this anticlinal 
 on the York River, there is a distance of about sixteen miles. The trans- 
 verse breadth of these exposures on the York River is nearly two miles, York River, 
 in which the strata are arranged in the form of an anticlinal, with the 
 opposite sides converging toward the west at such a rate as to make it 
 probable, that in this direction, the limestones will become covered by the 
 overlying sandstones at the distance of about two miles from the river. 
 From one to two miles to the east of these exposures on the York River, 
 Keg Brook, a tributary of this stream, crosses the anticlinal in a deep Keg Brook, 
 ravine, and exposes the limestones in many places for two miles. In this 
 distance several tributary streamlets flow in deep gullies in the strike. All 
 the timber has been burnt off the declivities, and the surface is covered 
 with small bleached angular fragments of silicious limestone and shale. A 
 high bare ridge, known as Jack Mountain, lies in the form of a wedge 
 between Keg Brook and its lowest branch on the right. A mile up this 
 branch the strata dip S. 5 W. < 65, and consist of black petroleum-bear- 
 ing limestone in beds from one to six inches thick, with occasional partings 
 of shale. A short distance farther down, the dip is S. 28 W. < 26, and 
 the limestone beds are from three to seven inches thick. The anticlinal 
 bringing up these limestones, like most of the anticlinals in Gaspe*, is more 
 precipitous on its north than on its south slope ; its axis is therefore not in 
 the" middle of its breadth, and on Keg Brook it may be about a mile and 
 a quarter from the southern boundary of the limestone. In the York 
 River, just above this brook, the limestone at the summit of the formation 
 is divided into thick beds, of which some are dark grey, weathering reddish- 
 brown, and containing petroleum ; while others are nearly black, and hold Petroleum 
 
884 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 disseminated masses of chert. The dip is here S. 25 W. < 9', but the 
 average inclination on the south side of the anticlinal axis appears to be 
 about twenty degrees ; giving in the mile and a quarter, which the south side 
 occupies, a total thickness of about 2200 feet. Between six and seven miles 
 to the east of Keg Brook, and between two and three miles north of the 
 
 Mississippi York River, there occurs in the bed and banks of a branch of the Mississippi, 
 a brook tributary to this river, an exposure of about 1600 feet of the upper 
 portion of the formation. The exposure has a breadth of forty-five chains, 
 with a dip S. 4 W. < 34, and consists toward the top of dark grey hard 
 limestone, in uneven surfaced beds from six to eleven inches thick, with 
 drusy veins holding petroleum ; but the greater part of the section is 
 thinner bedded, and is interstratified with drab brownish-weathering shale, 
 How far the formation continues exposed to the eastward of this is uncer- 
 tain, but it is supposed that it may be covered by the succeeding sandstones 
 for between three and four miles before reaching the exposure already 
 mentioned as occurring on the axis of the anticlinal, five miles above the 
 township of York. 
 
 Between this spot and the mouth of Keg Brook, the Gasp^ sandstones 
 are displayed almost continuously in the bed and on the banks of the York 
 River, at the most southern bend of which they are removed about four 
 miles, across the measures, from the summit of the limestones. At this 
 
 Becharvaise P ar * ^ e J nave a northern dip, and rise into a prominent hill called Bechar- 
 
 Mountain. yaise Mountain ; which presents a long straight east and west ridge on 
 the south side of the river, about four miles to the north of the limestones 
 brought up on the succeeding anticlinal in the valley of the Douglastown. 
 
 sandstones. T^ e sandstones of York River are all greenish-grey in color, and inter- 
 stratified with frequent bands of greenish crumbling arenaceous shale. The 
 only observed exceptions to these prevailing strata consist of the resinous 
 
 Bed shale, beds described on page 792, and two thin layers of red shale occurring 
 between six and seven miles above the lowest exposure of limestone, besides 
 occasional bands of conglomerate. The sandstone beds vary from half 
 an inch to ten feet in thickness, and are uniformly of a moderately hard 
 and rather coarse even grained character. They frequently split into 
 smooth surfaced slabs of suitable thicknesses for flagstones, owing to the 
 presence of thin partings, with mica or carbonized remains of plants. The 
 thicker beds* are sometimes made up of very regular thin oblique layers, 
 constituting false bedding ; while at other times they are massive, and fit 
 for building purposes. The greenish arenaceous shales are most prevalent 
 near the base of the formation. They constitute about one half of the strata 
 in a thickness of several hundred feet overlying the limestones above Keg 
 Brook ; and they are also largely interstratified with the sandstones at all 
 other points on the river, where these approach the underlying limestones. 
 Small rounded pebbles are often seen disseminated through the sand- 
 
CHAP. XXII.] QASPfc SERIES. 885 
 
 stones, especially in the higher parts of the formation, sometimes in such 
 numbers as to constitute conglomerates^ These pebbly strata however do 
 not appear to be of such frequent occurrence as in Gaspe* Bay. 
 
 Calcareous bands, containing abundance of shells, are met with in some 
 places near the base of the sandstones. At the mouth of the Patawegia Brqok. Patawegia 
 joining the York River on the left bank, about three miles above the lowest B 
 exposure of limestone, a six-feet band of this kind occurs in a great thick- 
 ness of crumbling arenaceous shale, also holding fossils. Among those 
 which characterize the whole exposure are Zaphrentis, Orihis^ Stropho- 
 mena, Chonetes, Rensselceria ovoides^ Leptocoelia flabellites, Avicula, 
 several species of acephala of undetermined genera, Orthoceras and 
 Dalmanites. Undetermined species of Spirifer and Cyrtodonta are com- 
 mon in similar strata on Silver Brook ; and loose fragments of calcareous 
 sandstone, containing some of the above fossils, are found on the surface 
 between the York and Douglastown Rivers, south of the lowest exposure 
 of limestone. Carbonized remains of land plants are- abundantly dissemi- 
 nated through the sandstones of York River, as far as examined ; and in 
 many places they compose innumerable thin laminae or partings between Fossil 
 the arenaceous strata. Among these plants, as determined by Dr. Dawson, p ai 
 Psilophyton princeps is the most abundant, and it is accompanied in some 
 places by Leptopldeum rhombicum, a species occurring in the Devonian 
 sandstones of Perry in Maine, and Didymiphyllum reniforme, found in the 
 Hamilton group of New York. There occur in some beds two species of 
 fossil wood, resembling Prototaxites, but destitute of lines of growth and 
 medullary rays. These Dr. Dawson proposes to describe under the provi- 
 sional generic name of Nematoxylon, as N. simplex and N. minus. Among 
 -many fragments not sufficiently distinct to be described, there are some 
 apparently of a Lycopodites, resembling L. Milleri of Salter ; and others 
 are stems pitted, or marked with raised points, in the manner of certain 
 roots described by Salter from the Old Red sandstone of Caithness. 
 
 It was stated on paga 410 that the axis of the anticlinal on the Douglas- 
 town, leaving the river about five miles above the west side line of the town- 
 ship of York, appears to bear towards Point Peter. It is now however 
 considered more probable, that, gradually curving to the southeast, it will 
 come upon the coast at the village of Perc4. No facts, however, in regard p e rc< anticlinal, 
 to what is supposed tabe its course, have yet been ascertained between the 
 Douglastown and Malbay Rivers, in a distance of fifteen miles. The Malbay 
 River, for three miles from its mouth, is occupied by strata belonging to 
 the Bonaventure formation, and for between six and seven miles farther by 
 the sandstones of the Gaspe* series. In these, about a mile above the west 
 side-line of the township of Malbay, there are evidences of an anticlinal 
 arrangement, and this structure is supposed to mark a point in the axis of 
 the anticlinal in question. From this there appears to be a trend in the 
 
886 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXII. 
 
 Four anti- 
 clinals. 
 
 Grand 
 River, 
 
 ridges of the hills towards Perce*, which may indicate the farther course of 
 the anticlinal. 
 
 On a line a little westward of south from Cape Haldimand, the axes of 
 the four anticlinals which have been described are comprised in a distance of 
 between ten and eleven miles ; but on a line south from the mouth of the 
 Magdalgi they occupy a distance of twenty-five miles, and while they thus 
 separate from one another, they all gradually curve round from a north- 
 westward to a westward bearing. 
 
 On page 442 it is shown that the rocks of the Grand River, which enters 
 the Bay of Chaleur about eight miles west of Cape d'Espoir, consist, for 
 six miles up from its mouth, of dark grey slates, and dark grey limestones, 
 with arenaceous layers. The slates are partially calcareous, and the same 
 rocks have been ascertained to prevail on the river for twelve miles beyond 
 the distance above mentioned. The upward course of the river appears 
 to coincide, in a general way, with the strike of the slates, which is about 
 N. 40 W., while the dip is northeastward. These slates very much 
 resemble some of those of the Patapedia (page 417), and of Lake Temis- 
 couata (page 424) ; but no fossils have yet been obtained to determine 
 their exact horizon. 
 
 Malbay 
 River. 
 
 BONAVENTURE FORMATION. 
 
 The only additional information obtained in respect to the rocks of this 
 formation, relates to their distribution in the interior, between Point Peter 
 and the Grand River. Their occurrence on the Malbay River, for three 
 miles up from its mouth, makes it probable that the base of the formation 
 keeps about a mile north of the north side of Malbay, and continuing west- 
 ward, curves round and crosses the Malbay River as indicated. From its 
 intersection with this river the strike would bring the base to within about 
 a mile of the southwest angle of Malbay ; from which it would appear to run 
 southwest, inside of the north line of the township of Perce', nearly to the 
 <jrand River ; where its proximity is indicated by fragments of the conglom- 
 erates and red sandstones belonging to this formation, brought down by 
 a brook joining the Grand River on the left, about five miles from its 
 mouth. From this point it is probable that the base recedes, in the form 
 of a bay, toward Cape d'Espoir, leaving only a narrow border of the rock 
 along the coast to the mouth of the Grand River. 
 
 SUPERFICIAL GEOLOGY. 
 
 No solid stratified rocks newer than the palaeozoic formations already 
 described are known in Canada, These last are however in many parts 
 covered over with an accumulation of loose materials, constituting what is 
 
CHAP. XXII.] 
 
 SUPERFICIAL GEOLOGY. 
 
 887 
 
 often called diluvium or drift; which rests upon a very uneven surface, left 
 by the great and irregular denudation of the earlier rocks. These super- 
 ficial deposits have as yet been but imperfectly studied : the principal facts 
 known in their history will however be given in the following pages ; and 
 advantage will be taken of the published observations of persons not con- 
 nected with the Survey, to whom due credit will be given in the course of 
 the description. 
 
 These deposits, so far as yet known, may be considered in three groups, ciaewe 
 which are shown in the following table. The order in which the examples cation - 
 under each are placed must not be understood to imply any difference in 
 the age of these local deposits, which are in many cases equivalents. The 
 numbered groups, however, represent the order and succession of the three 
 great divisions of these superficial deposits, and in group II, the subdivi- 
 sions which are included under part 1 underlie those of part 2 in western 
 and eastern Canada respectively. The relations of these subdivisions 
 will be considered in their proper places. The Erie and Saugeen clays 
 and sands of western Canada, apparently belong to a distinct basin, and 
 are in part at least, of fresh-water origin ; so that their relations to the 
 lower and upper divisions of the stratified drift of eastern Canada and 
 Vermont cannot yet be determined. 
 
 III. 
 
 Shell-marl, calcareous tufa, peat. 
 Ochres, bog iron and manganese ores. 
 Modern alluvions. 
 
 II. 
 
 /^Algorna sand. 
 I Artemisia gravel. 
 
 ] Saugeen fresh-water clay and 
 
 sand. 
 1. Erie clay. 
 
 EASTERN CANADA. 
 
 'St. Maurice and Sorel sands. 
 Saxicava sand of Montreal. 
 Upper sand and gravel of 
 
 Beauport. 
 Upper Champlain clay and 
 
 sand of Vermont. 
 | Leda clay of the St. Lawrence 
 
 and Ottawa. 
 
 \ Lower shell-sand of Beauport. 
 Lower Champlain clay of 
 ( Vermont. 
 
 I. 
 
 Boulder formation, or glacial drift. 
 Auriferous drift of Eastern Canada. 
 
888 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 As- a preliminary to the history of the boulder formation, the grooving, 
 polishing, and rounding of the older rocks will first be mentioned ; after 
 which will be given the characteristics of the glacial or unstratified drift, 
 as seen both in eastern and western Canada. In describing the second 
 group, which corresponds to the lower and upper divisions of the 
 stratified drift, the deposits of western Canada, which exhibit peculiar local 
 differences, will be first considered. The two corresponding divisions in 
 eastern Canada will next be described, and will be followed by a notice 
 of the auriferous drift of southeastern Canada, and of the older tertiary 
 deposits in the adjoining state of Yermont. 
 
 ROUNDED ROCKS AND ICE GROOVES. 
 
 Bounded Rounded, grooved, and polished surfaces are often found on the older rocks 
 where these are naturally exposed, and are met with in still greater perfec- 
 tion wherever the ancient superficial deposits which cover them are artifi- 
 cially removed. The process which produced these results must therefore 
 have been contemporaneous with the transport of the drift over the surface, 
 or anterior to it. These phenomena have by geologists been attributed to 
 various agencies, but the evidences afforded in Canada appear to favor the 
 supposition that they have been caused by the action of glaciers. Along the 
 whole of the southern boundary of the Huronian and Laurentian hills, from 
 Lake Superior to Labrador, the rounded rocks, or " roches moutonne'es," 
 are very conspicuous, and the ordinarily rounded outline of these hills may 
 be due to glacial action. On Lake Superior the general direction of the 
 striae is southward ; but it varies slightly in different localities, and not far 
 from Fort William, Professor Agassiz observed them running about due 
 
 ice grooves, east, in a valley. The grooves are not always parallel, but frequently inter- 
 sect one another at small angles : the greatest is about forty-five degrees, 
 but in general the angle is very much less. The rocks along the north shore 
 of Lake Huron, and on- the multitude of small islands adjoining it, are 
 rounded and grooved in a very striking manner. As on Lake Superior, 
 the general direction of the striae is south, varying only a few degrees to 
 the east or west. Some of the small grooved islets, quite destitute of soil, 
 rise above the surface of the water like segments of spheroids, while others 
 are barely submerged, and render navigation very dangerous. The grooves 
 are also well shown along the rivers of the north shore, and around many 
 of the lakes in the interior. At one place, near the Bruce Mines, the 
 grooves were observed to run under an overhanging mass of rock, and to 
 mark both the wall and the roof. These, it would seem, must have been 
 caused by fragments imbedded in the yielding ice of a^ glacier. On Lake 
 Temiscamang also, a long narrow expansion of the Ottawa, the rocks are 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 889 
 
 furrowed in such a manner as to suggest that it is the result of glacial action. Glacial 
 Along this lake, as- well as along the Riviere Rouge, north of the Ottawa, M 
 the furrows conform in a general way to the directions of the river-valleys, 
 the limits of which appear to have guided the moving masses producing 
 the present grooves. In some, places on the Rouge, beds of quartzite, 
 interstratified with the crystalline limestone, .and having furrowed surfaces, 
 stand out boldly and abruptly from six to nine inches above the latter 
 rock ; which has been* probably slowly dissolved away by the subsequent 
 action of water. 
 
 On page 6 it is stated that the distribution of the innumerable lakes, 
 which appear scattered as if at random over the Laurentian region, is often 
 well explained by the peculiar geographical distribution of the strata, 
 resulting from their very corrugated condition, combined with the unequal 
 wear dependant upon the hardness and toughness of some parts of the 
 deposits, and the softness of others. The rock which is most characteristic 
 of the depressions is the comparatively soft crystalline limestone of the 
 series, and it appears probable that one of the main erosive forces has 
 been glacial action. Not only the lake-basins, but many of the river- 
 valleys, in which the lake-basins are only deeper part&> run on the bands of 
 limestone, and maybe due to the same cause. It has been shown on page origin of 
 IT that the arrangement of the great western lakes of Canada is traceable lake-basins - 
 to the arrangement of two parallel zones of strata, the softer members of 
 which have yielded with comparative facility to the wearing agency, pro- 
 ducing the excavations which hold the water. These great lake-basins 
 are depressions, not of geological structure, but of denudation; and the 
 grooves on the surfaces of the rocks, which descend under their waters, 
 appear to point to glacial action^ as one of the great causes which have 
 produced these depressions.* The following list of ice-grooves, with the 
 latitudes and longitudes of the places where they occur, will show some of 
 the directions in which glacial action has been exerted in different parts of 
 the province. The directions are all referred to the true meridian. 
 
 * Prof. A. C. Ramsay has lately endeavored to show that the lakes of Europe hare 
 been produced by the action of great glaciers, which, by their slow grinding action y 
 formed those depressions in the rocky strata which are now the basins of the lakes. 
 The facts above mentioned, and especially the glacial grooves continued beneath the 
 waters of the lakes, go far to show that the fresh-water basins of North America have 
 had a similar origin. This hypothesis points to a glacial period, when the whole region 
 was elevated far above its present level, and when the Laurentides, the Adirondacks, 
 and the Green Mountains were lofty Alpine ranges covered with perpetual snow, from 
 which great frozen rivers or glaciers extended far over the plains below ; producing by 
 their movements the glacial drift, and scooping out the river-valleys, and the basins 
 of the lakes. Dr. J. S. Newberry has pointed out in a very clear manner the evidences 
 of this former extensive glacial action in North America. (Annual of Scientific Discovery, 
 1863, page 252.) 
 
890 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXII. 
 
 LIST OP GLACIAL GROOVES. 
 
 No 
 
 LOCALITY. 
 
 LATITUDE 
 
 LONGITUDE DIRECTION. 
 
 1 
 2 
 3 
 4 
 5 
 6 
 7 
 8 
 9 
 10 
 11 
 12 
 13 
 14 
 15 
 16 
 17 
 18 
 19 
 20 
 21 
 22 
 23 
 24 
 25 
 26 
 27 
 28 
 29 
 30 
 31 
 32 
 33 
 34 
 35 
 36 
 37 
 38 
 39 
 40 
 41 
 42 
 43 
 44 
 45 
 46 
 47 
 
 
 o ; 
 46 46 
 46 56 
 46 54 
 46 52 
 46 26 
 46 26 
 46 33 
 46 33 
 46 24 
 46 31 
 46 26 
 46 25 
 46 27 
 46 26 
 46 25 
 46 18 
 46 16 
 46 15 
 46 16 
 46 19 
 46 18 
 46 15 
 46 32 
 46 31 
 46 35 
 46 34 
 46 25 
 46 28 
 46 28 
 46 23 
 46 22 
 46 22 
 46 17 
 46 16 
 46 11 
 46 16 
 46 16 
 46 14 
 46 12 
 46 16 
 46 11 
 46 12 
 46 10 
 46 19 
 46 18 
 46 8 
 46 49 
 
 O 1 
 
 84 29 
 84 27 
 84 22 
 84 22 
 84 00 
 83 59 
 83 58 
 83 58 
 83 55 
 83 54 
 83 49 
 83 48 
 83 46 
 83 46 
 83 45 
 83 44 
 83 39 
 83 39 
 83 31 
 83 25 
 83 24 
 83 17 
 83 24 
 83 22 
 83 19 
 83 17 
 83 15 
 83 13 
 83 10 
 83 7 
 83 4 
 83 4 
 83 1 
 82 59 
 82 57 
 82 53 
 82 55 
 83 20 
 83 13 
 83 13 
 83 2 
 83 2 
 82 53 
 81 9 
 81 11 
 81 39 
 80 26 
 
 o 
 
 S. 30 E. 
 S. 23 W. 
 S. 23 W. 
 S. 2E. 
 S. 40 W. 
 S. 25W. 
 S. 55 W, 
 S. 70 W. 
 S. 10 W. 
 S. 9W. 
 S. 17 W. 
 S. 17 W. 
 S. 25 W. 
 S. 15 W. 
 S. 15 W. 
 S. 
 S. 20 W. 
 S. 15 W. 
 S. 18 W. 
 S. 
 S. 12 W. 
 S. 25 W. 
 S. 15W. 
 S. 7W. 
 S. 17 W. 
 S. 32 W. 
 S. 43 W. 
 S. 19 W. 
 S. 46 W. 
 S. 21 W. 
 S. 15 W. 
 S. 25 W. 
 S. 8W. 
 S. 5 E. 
 S. 20 W. 
 S. 17 W. 
 S. 3W. 
 S. 22 W. 
 S. 15 W. 
 S. 10 W. 
 S. 12 W. 
 S. 12 W. 
 S. 13 W. 
 S. 45 W. 
 S. 41 W. 
 S. 49 W. 
 S. 23 W. 
 
 
 " east angle, 
 
 
 Macdonald Township ; southern boundary, .... 
 " " " " 
 Echo Lake ; island, 
 
 shore, 
 
 
 
 Thessalon Lake * western island 
 
 
 
 Rock Lake west and south sides 
 
 
 
 Palladeau Islands * one of the group .... 
 
 u n it 
 
 
 Wiibiquekobingsing Lake N W end 
 
 " S. E. end, 
 
 
 Katigamaigouska Lake 
 
 
 
 
 U tt 
 
 Little White River, 
 
 u a 
 
 " " " ...(other grooves S. 70 E.) 
 Mahcomang Lake 
 
 u 
 
 
 
 " " below " " 
 
 " " mouth, 
 
 " " Lake of the Mountains, 
 
 U It It tt 11 
 
 
 11 11 It It 
 
 
 11 island at its mouth, 
 
 U 11 It It 
 
 
 White-fish River, Round Lake, east side 
 
 " " " south side, 
 Long Lake, 
 
 Maskanongiwagaming Lake, north end, ....... 
 
 
CHAP. XXII.] 
 
 SUPERFICIAL GEOLOGY. 
 
 891 
 
 LIBT OK GLACIAL GEOOVES. Continued. 
 
 No. 
 
 LOCALITT. 
 
 LATITUDE 
 
 LONGITUDE 
 
 DIRECTION. 
 
 48 
 
 Wahnapitaeping Lake, 
 
 o ; 
 46 42 
 
 / 
 
 80 38 
 
 o 
 
 S. 23 W. 
 
 49 
 
 ti n 
 
 46 41 
 
 80 38 
 
 g 23 W 
 
 50 
 
 Maskanongi River .... 
 
 46 40 
 
 80 26 
 
 S 37W 
 
 51 
 52 
 53 
 
 Georgian Bay, western outlet of French River, 
 ti it it ti 
 
 45 55 
 45 55 
 46 10 
 
 80 56 
 80 55 
 79 33 
 
 S. 37 W. 
 S.45W. 
 S 35 W. 
 
 54 
 
 
 46 1 
 
 79 26 
 
 S 35 W. 
 
 55 
 
 
 44 34 
 
 80 57 
 
 S 41 W. 
 
 56 
 
 Brant, 
 
 44 12 
 
 81 13 
 
 S 10W. 
 
 57 
 
 
 44 35 
 
 80 52 
 
 S 12 W. 
 
 58 
 
 it 
 
 44 32 
 
 80 55 
 
 S. 23 W. 
 
 59 
 
 
 44 28 
 
 80 54 
 
 S. 5E. 
 
 60 
 
 St. Vincent, 
 
 44 32 
 
 80 35 
 
 S. 10 E. 
 
 61 
 62 
 63 
 
 Collingwood, Blue Mountains, (Pro/. Chapman,') 
 " " (Mr. J. Irving,) 
 Eramosa, at Rockwood 
 
 44 30 
 44 29 
 43 38 
 
 80 20 
 80 19 
 80 8 
 
 S. 22 E. 
 S. 69 E. 
 S. 38 E. 
 
 64 
 
 Blanchard, at St. Mary's, 
 
 43 16 
 
 81 11 
 
 S. 45 E. 
 
 65 
 
 
 43 19 
 
 80 14 
 
 S. 46 E. 
 
 66 
 
 " near Sheffield, 
 
 43 20 
 
 80 13 
 
 S 72 E 
 
 67 
 
 " " Troy, 
 
 43 15 
 
 80 12 
 
 S 76 E 
 
 fift 
 
 tt 
 
 40 -to 
 
 Oft 10 
 
 S 59 E 
 
 fiQ 
 
 it 
 
 40 IQ 
 
 PA -I ft 
 
 S 79 E 
 
 70 
 
 West Flamborough ... 
 
 43 21 
 
 Oft ) 
 
 fi 40 T? 
 
 71 
 
 72 
 
 " " .. (other grooves S. 69 W.) 
 it n 
 
 43 16 
 43 16 
 
 80 1 
 80 1 
 
 S. 74 W. 
 S 24W 
 
 73 
 
 
 43 15 
 
 79 56 
 
 S 71 W 
 
 174. 
 
 n 
 
 4.0 -i K 
 
 7Q KQ 
 
 SKQ TTfT" 
 
 75 
 
 York, Grand River, 
 
 43 2 
 
 79 54 
 
 S 68 E 
 
 76 
 
 77 
 
 Niagara Falls, (other grooves S. 8 W.) 
 
 43 7 
 
 44. 13 
 
 79 4 
 
 77 12 
 
 S. 28 W. 
 S 45 E 
 
 78 
 
 
 A A OR 
 
 76 24 
 
 S 10 W 
 
 7Q 
 
 
 44. 14 
 
 76 29 
 
 S 45 W 
 
 80 
 
 
 44 19 
 
 76 25 
 
 S 45 W 
 
 81 
 
 
 44 43 
 
 75 30 
 
 S 22 W 
 
 82 
 
 Newborough, (Dr. Geo, Lawsonj) 
 
 44 39 
 
 76 19 
 
 S 68 W 
 
 83 
 
 
 47 36 
 
 79 30 
 
 S 53 E 
 
 84 
 
 <( (c 
 
 47 33 
 
 79 28 
 
 S 78 E 
 
 85 
 
 " " West Bay (also S 36 W) 
 
 47 31 
 
 79 37 
 
 S 15 E 
 
 86 
 
 " " east shore, 
 
 47 30 
 
 79 29 
 
 S 38 E 
 
 87 
 
 it it n 
 
 47 24 
 
 79 26 
 
 S 18 E 
 
 88 
 
 
 47 21 
 
 79 28 
 
 S 18 E 
 
 89 
 90 
 
 " " H. B Co.'s post,... (also S. 13 W.) 
 
 47 19 
 
 47 18 
 
 79 25 
 79 26 
 
 S. 35 E. 
 S 14E 
 
 91 
 
 it it it it 
 
 47 13 
 
 79 25 
 
 S IE 
 
 92 
 
 it it n it 
 
 47 9 
 
 79 26 
 
 S 7 W 
 
 93 
 
 ii ti it ti 
 
 47 7 
 
 79 27 
 
 S 18 E 
 
 94 
 
 Allumettes Lake, Montgomery's 
 
 45 51 
 
 77 12 
 
 S. 25 E 
 
 95 
 
 
 45 25 
 
 76 37 
 
 S 45 E. 
 
 96 
 
 
 45 19 
 
 76 17 ! 
 
 s 
 
 
 
 
 
 
892 
 
 GEOLOGY OF CANADA. 
 
 LIST OB 1 GLACIAL GROOVES . Concluded. 
 
 [CHAP. XXII. 
 
 No. 
 
 LOCALITY. . 
 
 LATITUDE. 
 
 LONGITUDE 
 
 DIRECTION. 
 
 97 
 
 
 O 1 
 
 45 22 
 
 O f 
 
 75 42 
 
 O 
 
 S 45 E 
 
 98 
 
 Hull 
 
 45 26 
 
 75 44 
 
 S 45 E 
 
 99 
 
 
 45 28 
 
 75 44 
 
 S. 37 E. 
 
 100 
 
 
 45 26 
 
 75 42 
 
 S 45 E 
 
 101 
 
 Kemptville (other grooves- S 5 E ) 
 
 45 1 
 
 75 38 
 
 S 10 E 
 
 102 
 
 
 46 14 
 
 74 37 
 
 S 25 E 
 
 103 
 
 
 46 10 
 
 74 42 
 
 S t 12 E. 
 
 104 
 
 (other grooves S ) 
 
 46 5 
 
 74 41 
 
 g. 5 ^ 
 
 105 
 
 <( it 
 
 46 3 
 
 74 39 
 
 S 30 E 
 
 106 
 
 it 
 
 46 & 
 
 74 37 
 
 S 10 W 
 
 107 
 
 U 11 
 
 45 58 
 
 74 37 
 
 S. 20 E. 
 
 108 
 
 it it 
 
 45 55 
 
 74 40 
 
 S. 25 W 
 
 109 
 
 it it 
 
 45 51 
 
 74 39- 
 
 S 7 W 
 
 110 
 
 tt u 
 
 45 48 
 
 74 42 
 
 S 15W 
 
 111 
 
 Grenville (other grooves S 10 W ) 
 
 45 41 
 
 74 35 
 
 S 20 W 
 
 112 
 
 
 
 45 42 
 
 74 33 
 
 S 7W 
 
 113 
 
 a 
 
 45 41 
 
 74 33 
 
 S 5 W 
 
 114 
 
 tt 
 
 45 40 
 
 74 36 
 
 S 13E 
 
 115 
 
 Wentworth 
 
 45 45 
 
 74 25 
 
 S 20 W 
 
 116 
 
 
 45 25 
 
 73 58 
 
 S 45 W 
 
 117 
 
 
 45 50 
 
 73 53 
 
 S. 14 W. 
 
 118 
 
 
 45 37 
 
 73 47 
 
 9 19 W 
 
 119 
 120 
 
 Montreal, Mile-end quarries, .... (also S. 47 W.) 
 a E. of Papineau Road, 
 
 45 32 
 45 32 
 
 73 35 
 73 34 
 
 S. 67 W. 
 S. 40 W. 
 
 121 
 
 a -yy tt tt 
 
 45 32 
 
 73 34 % 
 
 S 44 W 
 
 122 
 
 " N of Mile-end . ..(also 8 51 W ) 
 
 45 31 
 
 73 36 
 
 S 6-1 W 
 
 123 
 
 
 45 4 
 
 7-2 42 
 
 S. 61 E 
 
 124 
 
 
 45 7: 
 
 72 40 
 
 S. 36 E. 
 
 125 
 
 Orford . . . . 
 
 45 24 
 
 72 13 
 
 S 43 E 
 
 126 
 
 
 45 24 
 
 71 53 
 
 S. 43 E 
 
 147 
 
 
 47 44 : 
 
 69 12 
 
 S. 64 E 
 
 128 
 
 it u 
 
 47 43 
 
 69 11 
 
 S. 49 E. 
 
 129 
 
 It U 
 
 47 43 
 
 69 2 
 
 S. 64 E. 
 
 130 
 
 tt It 
 
 47 41 
 
 68 58 
 
 S. 64 E. 
 
 131 
 
 It It 
 
 47 41 
 
 68 57 
 
 S. 44 E. 
 
 132 
 
 
 47 39 
 
 68 49 
 
 S. 54 E. 
 
 13S 
 
 
 47 36 
 
 68 43 
 
 S 52 E 
 
 134 
 
 (also S 55 ? E ) 
 
 47 36 
 
 68 42 
 
 S 66 E 
 
 135 
 
 it it 
 
 47 36 
 
 68 41 
 
 S 48 E 
 
 136 
 
 tt it 
 
 47 35 
 
 68 39 
 
 g 27E 
 
 137 
 
 
 47 99 
 
 68 19' 
 
 S 60 E 
 
 138 
 
 
 4'8 T 
 
 69 8 
 
 S 32 E 
 
 139 
 
 
 48 32 
 
 67 43 
 
 S. 80 E. 
 
 140 
 
 
 fin 10 
 
 64 2 
 
 S 27W 
 
 141 
 
 
 KA i IT 
 
 63 49 
 
 S 7 W 
 
 142 
 
 
 50 16 
 
 63 40 
 
 S. 27 W. 
 
 143 
 
 
 50 14 
 
 63 27 
 
 S 17W 
 
 144 
 145 
 
 Ste. Genevieve Harbor, opposite the island, .... 
 
 50 17 
 50 36 
 
 63 3 
 
 59 12 
 
 S. 12 W. 
 S. 32 E. 
 
 
 
 
 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY, 893 
 
 At the Pointe aux Morts, an ice-grooved surface, comprising many acres, 
 is exposed between high and low water mark. The main bearing of the 
 grooves, as stated in the list (142), is S. 27 W. Grooves in several 
 other directions however occur, and, from the manner in which they cross 
 one another, the following appears to be the succession of directions, from 
 the oldest to the newest : S. 27 W., S. 37 W., S. 47 W., and S. 31 W. 
 Toward the east side of the exposure there is a shoulder of rock eight or 
 ten feet high. Approaching this, a group of grooves, which are very dis- 
 tinctly marked, and can be followed for fifty yards, is observed to turn 
 gradually from S. 37 W. to S. 10 W. ; and two of the grooves, which 
 were about six inches apart and very deep, run into one. 
 
 BOULDER FORMATION AND SURFACE BOULDERS. 
 
 The boulders or erratic blocks, which are found irregularly distributed Erratic blocks, 
 over the surface of the province, appear to have been left by the washing 
 away of the lighter material from the formations in which they were once 
 imbedded, and to have been, for the most part, derived from the glacial 
 drift, in which they abound. These blocks are met with alike in valleys 
 and on hill-tops. In the former, they are found in great abundance in 
 many places where the boulder formation has been extensively denuded by 
 the action of water, and its lighter materials swept away. On elevations, 
 they are often seen resting upon the unstratified drift, which in the adja- 
 cent depressions of the surface is covered over by stratified sand and clay. 
 The boulders in any locality always present a greater or less admixture 
 of various kinds of rocks ; although some one species, either of local or 
 remote origin, often greatly predominates over the others. The blocks 
 appear, in almost all cases, to have travelled southward. A few excep- 
 tions to this have however been noted. Thus in the county of Rimouski, 
 in the valley of the Neigette River, there are found on the surface, 
 several large boulders of limestone, one of them forty feet in diameter, 
 belonging to the Gasp6 series, which have been moved several miles 
 northward or northeastward. Farther down the valley of the St. Law- 
 rence, blocks of trachytic granite have been carried northeastward from 
 the Table-topped Mountain down the valley of the Magdalen. Dr. Dawson 
 has described similar instances of the northward transportation of boulders 
 in Nova Scotia. 
 
 On the north shore of Lake Superior, mingled with the ruins of the 
 rocks immediately near, there are found numerous blocks of Upper Silurian 
 fossiliferous limestone, which have been brought from the northward. On 
 Lake Huron, the surface of Sugar Island, and of the flat land between 
 it and the Huronian hills to the north, is strewn with boulders of the 
 Silurian sandstone of the region, of Laurentian gneiss, and of the 
 
894 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 Lake Huronian rocks, including some of the characteristic jasper conglomerate. 
 Rounded blocks, mostly of Huronian age, are very abundant along the 
 whole north shore of Lake Huron. At one place, about thirteen miles 
 east of the Thessalon, the shore is so encumbered with them as to impede 
 the landing with boats. Here also blocks of the jasper conglomerate 
 are met with. On Lacloche, and the neighboring islands, rounded 
 boulders of a black trap are common ; and the ringing sound which they 
 give when struck is said to have been the origin of the name of Lacloche. 
 
 Huronian Huronian boulders are abundant on the French River, and around Lake 
 Nipissing ; and they become more numerous as we ascend the Sturgeon 
 and Wahnapitae Rivers, where they are sometimes seen perched on the bare 
 Laurentian gneiss, as much as a hundred feet above the water. Boulders of 
 the jasper conglomerate occur on Lacloche Island, and on the Fox Islands, 
 thirteen miles west of the French River, but have not yet been observed 
 on the coast to the east of this river. According to Dr. Bigsby, the south 
 and west sides of the island called the Giant's Tomb, four and a half miles 
 from the Christian Islands, are covered with boulders of labradorite and 
 other Laurentian rocks ; while they are absent from the north and east 
 sides. Boulders, most probably of Laurentian origin, have been observed 
 by Mr. Sanford Fleming to be abundant on the hills skirting Lake Huron, 
 from Penetanguishine to Nottawasaga ; and boulders of Laurentian rocks are 
 
 Lanrentian found in considerable numbers scattered over the high table land of western 
 Canada, south of Georgian Bay. A portion of this region attains an eleva- 
 tion of 1760 feet above the sea, and much of it is higher than the 
 Laurentide hills to the north, from which the boulders have been derived. 
 These blocks are generally more angular than those from a similar source 
 found at lower levels, and are associated with many others of local origin. 
 In the counties of Grey and Wellington, the erratic blocks of local origin 
 are largely mingled with others, both of Laurentian and Huronian age, 
 and the boulder formation is in many places seen beneath the stratified 
 gravel. In the south half of the county of Bruce, boulders are compara- 
 tively rare, and consist for the most part of Huronian rocks. On the 
 twenty-third lot of the seventh range of Goderich, is a group of very large 
 flat angular blocks of unfossiliferous sandstone, which have been quarried 
 for building purposes ; and angular blocks of a similar sandstone, of which 
 the origin is uncertain, are scattered over the whole country between 
 Goderich and Woodstock.. Boulders and pebbles of Huronian rocks are 
 found along the Detroit River, and the western part of the north shore of 
 Lake Erie. It is remarked by Mr. De Cew that in the southwest corner 
 
 Devonian of Windham, and along the east side of Middleton, very large boulders of 
 
 rocks. Devonian limestone, probably belonging to the Corniferous formation, are 
 of frequent occurrence, associated with others of Laurentian' origin. In 
 the latter township, the limestone masses are not found on the west side of 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 895 
 
 Big Creek, while those of Laurentian rock continue to be as abundant as 
 before. To the north of Brantford, Huronian rocks are abundant among 
 the erratic masses ; but boulders of Laurentian gneiss are unusually large 
 and numerous about Gait, and many buildings in the town are constructed 
 of this rock ; while in the Niagara district it is observed that, with the 
 exception of those of local origin, the blocks are chiefly Laurentian. 
 
 Boulders are abundant along the west side of Cook's Bay on Lake Simcoe, 
 and the Holland River, where they present mixtures of Laurentian, Huron- 
 ian, and Silurian rocks. Similar boulders are met with on the high land 
 south of Holland Landing, in Whitechurch and King ; and Prof. Chapman 
 notes the occurrence of a very large block of Black River limestone in 
 Albion, on the highest part of the Oak Ridge. Through Vaughan and 
 Markham, and along Yonge Street south to Toronto, boulders are somewhat 
 rare. Laurentian blocks occur everywhere along the north shore of Lake Lake Ontario. 
 Ontario, and the shore of the Bay of Quinte*, and are frequently found on 
 eminences back from the lake. In Darlington and Clarke, according to 
 Dr. Bigsby, the Silurian boulders generally occur in groups, and not 
 scattered like those of Laurentian origin. The latter are very numerous 
 throughout the counties of Hastings, Addington, and Frontenac, and are 
 often largest and most abundant on the highest ridges. One of these 
 ridges, which occurs on the twelfth lot of the third range of Sheffield, 
 presents, among other boulders, one of Laurentian crystalline limestone, 
 containing about 6500 cubic feet. 
 
 The glacial drift, with its boulders, forms the surface of the country 
 over much of the triangular area included by the St. Lawrence and Ottawa 
 Rivers, and the meridian of Kingston, especially in the southwestern 
 portion of this region. Stratified clays and sands however fill up depres- 
 sions of greater or less extent over this surface, and upon these parts 
 erratic blocks are of somewhat rare occurrence. Along the Ottawa River, Ottawa RIY 
 ridges of glacial drift or of boulders, running north and south, and resem- 
 bling moraines, are observed in very many places, and often produce Moraines 
 contractions in the channel of the river. One of these occurs at the 
 Hudson Bay Company's post about eighteen miles from the head of Lake 
 Temiscamang. At the Long Sault, just below this lake, an accumulation 
 of Laurentian boulders obstructs the passage of the river, and is greatly 
 instrumental in producing the rapids ; another is met with at the mouth 
 of the Maganasippi, or River of Round Stones, about twenty miles above 
 the Mattawa, where the well rounded boulders, which evenly pave the bed 
 of the stream, are remarkable for being very uniform in size, with a 
 diameter of ten or twelve inches. At the rapids of Roche Capitaine a 
 great accumulation of boulders rises into a ridge between the present 
 channel of the Ottawa, and a ravine, which is probably an old bed of the 
 river. A little above the mouth of Green's Creek, between nine and ten 
 
GEOLOGY OF CANADA, [CHAP. XXII. 
 
 miles below the city of Ottawa,, a line of boulders runs quite across the 
 river, greatly obstructing its navigation. Near L'Orignal, six of these 
 ridges, or lines, occur in the distance of a mile. Numerous large boulders 
 of Laurentian gneiss and labradorite are strewed on the surface of the 
 Lower Silurian rocks at Grenville, where the finer detritus which probably 
 once accompanied them has been washed away. 
 
 On Rigaud Mountain, there is met with a series of plains, destitute of 
 vegetation, and covered with boulders. These plains, which extend over a 
 large area, filling depressions in the surface of the mountain, begin on the 
 north side, about two hundred feet above the Lake of Two Mountains, and 
 rise gradually toward the south, until they attain a height of two hundred 
 and eighty feet, beyond which they slope away gradually to the south. On 
 the north side, near the summit, these rolled masses are arranged in paral- 
 lel ridges, from five to six feet high, twenty or thirty paces asunder, and 
 running about northwest* The boulders consist, in great part, of the trap 
 of the mountain, mixed with a few of sandstone. They are generally very 
 well rounded, and vary from three to eighteen inches in diameter. At a 
 depth of seven or eight feet from the surface, the same boulders are still 
 found, without admixture. The upper portions of the mountain, its southern 
 flank, and a considerable extent of country to the south of it, were found 
 to be thickly strewn with similar trap boulders, derived from the rock of 
 the mountain. On its northern flank however, and on the plain between 
 the mountain and the Ottawa River, the erratic blocks consist, for the most 
 part, of Laurentian boulders, and of large angular masses of a sandstone, 
 apparently belonging to the Potsdam formation. A linear distribution of 
 boulders is in some places observed around Mount Royal, where many of 
 the blocks are striated in a similar manner to those of Alpine moraines. 
 
 Boulders are very often found imbedded in the stratified clays and 
 sands throughout eastern Canada ; and some of the blocks which are here 
 and there met with on the surface of these deposits, may have been left 
 by partial denudation, while others may have dropped from floating 
 icebergs. The facts known with regard to the unstratified drift of eastern 
 Canada will be given farther on, in describing the stratified deposits of 
 that region. 
 
 BRIE AND BAttGEEN CLAYS, 
 
 Two divisions have already been indicated in the stratified clays of wes- 
 tern Canada, the lower of which had been partially worn away before the 
 deposition of the upper division, so that this rests unconformably upon it, 
 adapting itself to the irregularities of the denuded surface. The latter 
 is sometimes associated with beds of gravel and sand ; a layer of which, 
 belonging to the upper division, sometimes marks its contact with the under- 
 lying deposit. This, which will for convenience be designated as the Erie 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 897 
 
 clay, is, when moist,* of a blue color, with thin grey bands. It is com- Erie clay, 
 monly more or less calcareous, and always holds boulders and pebbles in 
 greater or less abundance. These, when of palaeozoic rocks, though par- 
 tially worn smooth, are generally somewhat angular, but are rounded when 
 from the Laurentian or the Huronian series. They are frequently scratched ; 
 and in some localities few of them are found without striae, which are 
 best preserved on the pebbles of limestone. These lower clays have as yet 
 yielded no fossils. 
 
 The upper division of these deposits, which is largely developed and Sa "een ciay. 
 well exposed along the Saugeen River, may be called the Saugeen clay. 
 With the exception of a yellow band sometimes found at the top, it con- 
 sists of a thinly bedded brown calcareous clay, generally containing but 
 few boulders or pebbles. The layers of clay, seldom exceeding an inch in 
 thickness, are separated by thin partings of a drab or olive color. 
 This division is sometimes underlaid by beds of sand, which separates it 
 from the Erie clay ; and in certain parts of its distribution it is also inter- 
 stratified with sands and gravels. The thickness of the lower clay has in no 
 one place been ascertained to be more than 200 feet ; but clays apparently 
 belonging to this division occur at various levels, from sixty feet below the 
 surface of Lake Ontario, to a height of perhaps one hundred feet above Lake 
 Huron ; showing differences in level of about 500 feet. In like manner, 
 clays having the characters of the upper or Saugeen division, are found from" 
 the level of Lake Ontario to at least 100 feet above Lake Huron, showing 
 differences of level nearly or quite equal to that of the lower clay. The 
 interstratified gravels and sands of the upper division occur principally in 
 the deposits on the higher levels. Fresh-water shells have in two or three 
 instances been found in beds apparently belonging to this division. 
 
 The Erie clay, with few interruptions, runs along the north shore of Erie cla y- 
 Lake Erie, from Long Point westward to the Detroit River, and appears 
 to underlie the whole country between this part of the lake and the main 
 body of Lake Huron. It is again found at Owen Sound, and along the 
 Nottawasaga River; and it occurs along the shores of Lake Ontario, and 
 as far east as Brockville. This clay appears to be more calcareous in the 
 northwestern part of its distribution than elsewhere A specimen from the 
 shore of Lake Huron, nearGoderich, contained thirty per cent, of carbon- 
 ate of lime ; and similar clays from Walkerton in Brant, Owen Sound, and 
 Linwood in Wellesley, are equally calcareous, and in many places unfit 
 for the manufacture of bricks. They are in such cases a blue marl, which 
 readily disintegrates, and might be used with advantage as an application 
 to sandy soils. 
 
 When less calcareous, the clays of this division are much esteemed for 
 
 * The color ascribed to any clay in these pages is always to be understood as 
 applying to it in an undried state. 
 
 G* 
 
898 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXII. 
 
 White 
 bricks. 
 
 Owen 
 Sound. 
 
 the manufacture of bricks, which are white, with a yellowish, or more rarely, 
 
 a greenish tinge when burned ; while the clays of the upper division appear 
 
 in every case to yield red bricks. Clays fitted for 
 
 the manufacture of white bricks are wrought at St. 
 
 Mary's, London, Woodstock, Dundas, Toronto, Co- 
 
 bourg, Belleville, Frankville in Kitley, and Easton's 
 
 Corners in Wolford. In all of these localities the lower 
 
 clay has the characteristic blue color, and is overlaid 
 
 by the unconformable brown clays. The boulders and 
 
 pebbles which are constantly present in it, are not in 
 
 sufficient numbers to interfere much with its use for 
 
 brick-making. These lower clays exhibit in many 
 
 instances a distinctly jointed structure, which appears 
 
 to be wanting in those of the upper division. 
 
 The principal facts known with regard to the rela- 
 tions and the distribution of these two divisions will 
 now be given, beginning to the westward. At Owen 
 Sound, recent road-cuttings in the terraces on each 
 side of the town exhibit, in a beautiful manner, the 
 relations of the two clays, which are shown in the 
 accompanying section, 447. The bedding of the lower 
 deposit, which is readily distinguished by its grey 
 stripes, is remarkably corrugated, while its denuded 
 surface slopes, on either side, to the valley between 
 the two terraces. In the terrace on the west side, the 
 blue clay, at the thickest part in the cutting, measures 
 eighteen feet, and is mingled with sand, with fragments 
 of rock from the Hudson River and Clinton forma- 
 tions, and with pebbles and boulders of gneiss. The 
 overlying brown Saugeen clay lies in nearly horizontal 
 beds, abutting unconformably against the sloping sur- 
 face of the Erie clay, and is largely interstratified with 
 beds of fine sand and loam, which are also brown. 
 This upper deposit extends over the whole terrace 
 between the west side of the Sydenham River and 
 the escarpment of the Niagara formation, which rises 
 half a mil to the westward. On the opposite side of 
 the river, at the same horizon, brown clay is met with, 
 from which red bricks are made ; and in the south- 
 east corner of the township of Sydenham, beds of 
 tenacious brown clay, interstratified with brown sand, 
 are found in digging wells below the Niagara escarp- 
 ment. 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 899 
 
 High banks of brown sand, capped with a thin bed of brown clay, are saugeen 
 seen in several places on the Saugeen, between Hanover and Walkerton ; Eiyer> 
 and the blue Erie clay is observed in the bank of the river, about two and 
 a half miles below the former place. In this neighborhood the upper 
 clay in some places appears as if pressed into th underlying sand, in 
 mammillary masses of various sizes. At Walkerton, a fine section of these 
 deposits is seen, at a bend of the river, on the twenty-eighth lot of the 
 first range north of the Durham road. Here, a bank rises one hundred 
 feet over the water, and displays bands of laminated brown clay, inter- 
 stratified with thick beds of fine sand, the whole resting on the blue clay 
 at the foot of the bank. In Brant, on the twenty-fifth lot of the second Brant, 
 range south of the Durham road, and about a mile south of Walkerton, 
 two terraces occur at Mr. Me Vicar's brick-yard. On the lower of these, an 
 excavation shows a section of about twenty feet of brown laminated loamy 
 clay, interstratified with beds of sand. A little to the south of this, rises 
 the second terrace, consisting of nine feet of brown clay. A grey calca- 
 reous sand underlies these clays, and has been penetrated to a depth of 
 twenty-one feet. A bed of hard cemented gravel and sand, three inches 
 in thickness, and with a ripple-marked surface, was found between this 
 sand and the overlying sandy clay. In the bed of .the Saugeen, and in its 
 west bank in South Brant, layers of coarse cemented gravel were observed, 
 which appeared to pass under a fine loamy yellow sand occurring higher 
 up in the bank. The banks of this river, in many places between Walker- 
 ton and its mouth, exhibit alternations of clay and sand. In the seventh 
 and eighth ranges of Brant, the east bank is more than one hundred feet 
 high, and is, for a considerable part, composed of brown clay. On the 
 opposite side of the river, on higher ground, about half a mile from the 
 bank, a well was sunk through eleven feet of brown clay. This was 
 underlaid by twelve feet of a gravelly light blue clay; on penetrating which 
 a sandy layer was reached, supplying abundance of water. In the north- 
 west corner of Brant, on the forty-first lot of range B, another well was 
 sunk, which gave, in descending, twelve feet of alternating layers of brown 
 clay, and brown and white sand. This was followed by thirteen feet of 
 stiif clay, composed of alternate layers of brown and dark olive colors, with 
 thin partings of fine white calcareous sand ; the whole being underlaid by 
 a soft tenacious blue clay, which was penetrated to a depth of twenty feet. 
 
 At the intersection of the Teeswater with the town-line between Elders- 
 lie and Brant, the brown clay is underlaid by the blue clay, the latter con- 
 taining pebbles, with an occasional boulder ; and in the village of Paisley, 
 at the junction of the Teeswater with the Saugeen, six feet of reddish- Teeswater. 
 brown clay, holding a few boulders and pebbles of Laurentian and Huronian 
 rocks, and interstratified near the base with layers of fine sand, rest upon 
 an unknown thickness of fine yellowish-white sand. The blue clay appears 
 
900 GEOLOGY OF CANADA. [G-HAP. XXII. 
 
 beneath the brown on the east side of the Saugeen, a little below Paisley ; 
 but the latter forms the surface on either side of this river, from the 
 north line of Brant to within three miles of its mouth. Its breadth here 
 has not been ascertained, but it probably overlies the blue clay throughout 
 the greater part of the country between the Saugeen and Lake Huron, 
 and may form part of the steep and high clay bank which overlooks the 
 lake the whole way from Clark Point to Port Frank, in Stephen, a distance 
 of fifty miles. It is said to occupy the valley of the Riviere aux Sables 
 (du nord), and is probably continuous between this and the Saugeen. On 
 the twenty-third lot of the seventh range of the township of Goderich, 
 yellow clay was observed, supporting boulders of Devonian and of northern 
 metamorphic rocks. In this region, it is to be remarked, that among the 
 boulders of metamorphic rock, those of Huronian age prevail to the west- 
 ward, but toward the east are gradually replaced by those from the 
 Laurentian series. 
 
 In Normanby, near to Neustadt, in the banks of the South Saugeen 
 River, are seen about seventeen feet of hard gritty bluish clay, filled with 
 pebbles, and overlaid by the same thickness of loose gravel. Striated 
 boulders of dolomite, which appear to have been washed out of the clay, 
 are found here. Again, on the west bank of this river, on the ninth lot of 
 the twelfth range of Normanby, beneath a few feet of yellow clay and fine 
 brown sand, are found about twenty-five feet of a similar sandy bluish clay, 
 holding pebbles. Wells sunk in the southern part of the township have 
 penetrated from twelve to twenty-four feet in a like deposit. The west 
 bank of this river, where it crosses the town line of Minto and Normanby, 
 exhibits about fifteen feet of fine yellow clay, which, like the overlying 
 clays and sands just named, apparently belongs to the Saugeen division. 
 The underlying material is here concealed. On the south side of the same 
 river, in the village of Mount Forest, at the corners of Normanby, Egre- 
 mont, Arthur, and Minto, there is a hill covered with gravel, beneath 
 which appears a fine blue clay. The surface of this appears to be deeply 
 worn by denudation, and the overlying gravel fills up the inequalities. 
 Beneath the gravel, clay is also observed in several other hills in the 
 vicinity. Along the river Ganistoga, in Maryborough, Peel, Wellesley, 
 and Woolwich, a very hard bluish-drab pebbly clay, locally known as 
 hard-pan, forms the subsoil. In sinking a well at Linwood, in Wellesley, 
 there were found eight feet of alternating sand, and yellow and drab 
 clay, followed by forty-two feet of the hard-pan ; beneath which was found 
 a bed of sand, affording a good supply of water. The pebbles of this 
 lower clayey deposit were generally small and well rounded: one of 
 nem contained fossils of the Trenton formation. Throughout the town- 
 ships just named, and those of Mornington, Elma, Logan, and part of 
 Arthur, drab clays, holding a few pebbles and boulders of gneiss and 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 901 
 
 greenstone, are generally distributed over the surface, which presents a 
 broadly undulating aspect. It is not certain whether the underlying bluish 
 pebbly clays of this region represent the Erie division : in some cases 
 they may belong to the more ancient unstratified drift. 
 
 Clays of different kinds may be said to predominate throughout all the 
 townships bordering on Lakes Huron and Erie, and the waters connecting Lake Huron, 
 them, from the mouth of the Saugeen on the one hand, to the mouth of the 
 Grand River on the other. The prevailing subsoil of the great triangular 
 area between these coast lines, so far as it has yet been examined, is like- 
 wise of clay. Although the steep bank of clay, often more than 100 feet 
 in height, already mentioned as stretching from Clark Point to Port Frank, 
 is the only part of the deposit which is actually washed by the waters of 
 Lake Huron, a continuation of the same bank is traceable, at a short dis- 
 tance back from the lake, both north and south from these points. North- 
 ward from Clark Point, it recedes very gradually from the shore for a few 
 miles, and thence continues to the Saugeen, at an average distance of two 
 miles from the lake ; the extreme variations being about one mile at its 
 nearest, and three miles at its greatest distance from it. The space between 
 this ancient lake margin (thirty-five miles in length) and the present shore, 
 is occupied by drifting sands. Southward from Port Frank, the continua- 
 tion of the clay terrace, which is sometimes visibly underlaid by strata of 
 the Devonian series, is seen at a short distance from the lake, for about 
 thirty miles, beyond which it appears to run farther inland. The interven- 
 ing area, on which the township of Sarnia is partly situated, is occupied 
 by loose sand. In the bank of the St. Clair, near the village of Sarnia, 
 the clay again makes its appearance, and continues thence southward to 
 Lake Erie. In the township of Plympton, the clay of this terrace was 
 found to contain fragments of the Corniferous limestone. 
 
 At the oil wells, on the thirteenth and fourteenth lots of the tenth range 
 of Enniskillen, two beds of gravel, of four and five feet respectively, have 
 been met with hi the clay, at depths of ten and forty-four feet from the 
 surface, making a total section of clay and gravel of forty-nine feet. Unio 
 circulus, U. gibbosus, and several valves of a Cydas, were obtained in the 
 upper bed of gravel ; and in this bed a deer's bone was also said to have 
 been found. Between the gravel and the overlying ten feet of clay, a thin 
 layer of impure mineral pitch, or half-dried petroleum, intervenes, enclosing 
 leaves of land-plants, and occasionally insects (page 524). Prof. Mather 
 has also noted the occurrence of fresh-water shells in the clay along the 
 Detroit River. 
 
 On the shore of Lake Erie, the two divisions of the clays are well exposed Lake Erie, 
 in cliffs, which, in the neighborhood of Port Talbot and Port Stanley, attain 
 an elevation of one hundred and fifty feet. The lower, or Erie clay, which 
 is bluish and somewhat calcareous, frequently holds angular fragments of 
 
902 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXII. 
 
 Brantford. 
 
 St. Cather- 
 ine's. 
 
 limestone, and small rounded boulders of the northern crystalline rocks. 
 This is overlaid by another deposit of clay, which is light brown above and 
 buff or yellowish toward the summit. This upper clay, generally brown- 
 ish in color, covers a considerable area in the townships bordering the east 
 side of the Grand River, below Brantford, and those on the lake between 
 the mouth of this river and the Niagara. The townships of Rainham and 
 Walpole are covered in many parts with a reddish-brown clay, of no 
 great thickness, which rests directly on the palaeozoic rocks. Similar 
 clays are said to continue through Woodhouse, Charlotte ville, and Wal- 
 singham. A cliff of reddish clay, holding angular fragments of Corniferous 
 limestone, and worn boulders of crystalline rocks, commences on the shore 
 of Lake Erie, three miles east of the Grand River, and extends about a 
 mile and a half farther eastward. At Niagara Falls the Silurian lime- 
 stone is covered by 120 feet of sandy loam, holding striated pebbles and 
 small boulders, and containing near the middle the shells of a species of 
 Cydas. It is overlaid by fifteen feet of thinly bedded reddish-brown clay, 
 containing similar pebbles and angular fragments. This deposit, whose 
 summit is sixty feet above the level of Lake Erie, forms a bank which 
 continues up to Chippawa. 
 
 Beneath the upper clays of the region just indicated, blue clays belong- 
 ing to the lower division are met witn in several places. In a brick-yard, 
 a mile to the south of Brantford, there is exposed a section of twenty-four 
 feet of blue clay, beautifully stratified in horizontal bands of a few inches, 
 with grey layers. These are less tenacious than the rest, and present various 
 corrugations and contortions, which are subordinate to even beds compos- 
 ing the mass. This clay, which is used for the manufacture of white 
 bricks, abounds in pebbles and rounded boulSers, which latter appear to be 
 chiefly of northern metamorphic rocks. From the aspect, of the bank 
 below the section, it is probable that the blue clay has here a thickness of 
 seventy or eighty feet. A similar clay has been met with in sinking wells 
 in several parts of the township of Seneca. Much' of the flat country 
 between the Niagara escarpment and the southern shore of Lake Ontario 
 appears to be underlaid by clay. In the township of Niagara, it is exposed 
 along the river and the lake, often covered with sand. At Thorold the 
 clays appear to belong partly to the upper, and partly to the lower division ; 
 while at St. Catherine's, a clay, which is supposed to belong for the. most 
 part to the former, has been penetrated to a depth of forty feet. At Jordan 
 in Louth, both clays are met with, and together form a bank of seventy 
 feet in height. From Grimsby westward, the upper clay diminishes in 
 thickness, and at Hamilton it entirely disappears. 
 
 The area between the Desjardins Canal and the limestone escarpment 
 which runs from Hamilton to the village of Ancaster, is underlaid by the 
 Erie clay ; which forms a raised plateau intersected by numerous hollows. 
 
CHAP. XXIL] SUPERFICIAL GEOLOGY. 903 
 
 The surface of the clay is here somewhat uneven, and the depressions are 
 filled with sand and gravel holding fragments of rocks from the Hudson 
 River formation, and pebbles of Laurentian gneiss ; the whole being some- 
 tunes overlaid by a thin stratum of fine sand. In the valley in which Dundas Dundas. 
 is situated, the blue clay has been penetrated to a depth of seventy-eight 
 feet, being about sixty feet below the level of Lake Ontario ; while on the 
 plateau to the south of the town, its height above the valley is probably 
 over one hundred feet ; so that if the clay of the valley runs under that of 
 the plateau, the entire ascertained thickness of the formation would be 
 about two hundred feei. An uneven covering of loamy gravel and rounded 
 fragments of limestone, with an occasional boulder of gneiss, is spread 
 over the blue clay at Dundas ; while to the westward, the valley is liter- 
 ally filled with irregular hillocks and broken ridges, composed of sand, 
 and blue and brown clays, which rise confusedly over one another to the 
 summit of the Niagara escarpment at Copetown, in the townships of 
 Ancaster and Beverley. 
 
 At Copetown station on the Great Western railway, near Dundas, eight- 
 een feet of brownish clay belonging to the upper division, are seen to rest 
 upon a considerable thickness of sand ; and farther to the westward, at Har- 
 risburg in South Dumfries, the. same clay has been ascertained to be at 
 least thirty feet thick. In sinking a well at Paris, one hundred feet of 
 clay holding boulders, and said to be for the most part brownish in color, 
 were met with. At Princeton, and at Ingersoll, twenty feet of this clay 
 were found resting on gravel ; and at Woodstock thirty feet of a similar clay 
 repose upon a clay belonging to the lower division. In sinking a well at the 
 Great Western railway station at London, Mr. Robb, on whose authority London, 
 the facts in the last four localities are stated, found a section in descending 
 order, of twenty-two feet of loam and sand, followed by sixty-eight feet of 
 hard-pan, with boulders, and two layers of four and five feet of soft sandy 
 clay; the whole underlaid by beds of sand and clay, with boulders, to a 
 depth of at least fifteen feet. The hard-pan, which, as already stated, is a 
 hard bluish-drab pebbly clay, may belong to the unstratified drift ; but in 
 another place near the town a section of fourteen feet of clay is exposed, 
 the upper part of which yields red bricks, while the lower portions burn 
 to a white or greenish-white color. 
 
 In the second range of York, in the rear of Toronto, the lower or Erie Toronto, 
 clay is extensively wrought for the manufacture of white bricks. It is 
 bluish when moist, but ash-colored when dry. It has a distinctly jointed 
 structure and contains pebbles and boulders sparingly distributed. Over 
 the irregular denuded surface of this horizontally stratified clay is spread 
 a coating of yellow clay and sand, which conforms to the undulations of 
 the surface of the soil. In two sections in a clay-pit here, the upper 
 stratum of yellow clay, which also holds pebbles and boulders, and burns 
 
904 GEOLOGY OP CANADA. [CHAP. XXII. 
 
 to red bricks, was three feet in thickness. Beneath this was found, in 
 the two sections, from five to nine feet of yellow sand, interstratified with 
 yellowish and bluish clays, both burning white. Under these was the 
 solid jointed blue clay ; which has been penetrated to the depth of sixty 
 feet, and in wells near by, to seventy or eighty feet, without any apparent 
 change in its characters. In digging wells in Toronto, according to 
 Prof. Hind, trunks and branches of trees have been found imbedded in 
 the overlying yellow clay at depths of from ten to twenty feet from 
 the surface. 
 
 To the east of Toronto, clays, generally overlaid by ^and, continue through 
 the southern parts of York and Scarborough. At Port Hope, and for a 
 few miles to the eastward, banks of stratified clay capped by sand, rise from 
 ten to forty feet above the level of Lake Ontario. Between Cobourg and 
 Napanee, the stratified clays are found in many localities, and are of two 
 colours, bluish below and yellowish above. These appear, as at Toronto, 
 BeJieviiie. to represent respectively the Erie and Saugeen divisions, In Belleville, 
 an excavation made near the court-house showed at the top four feet of 
 very fine yellow sand, followed by three feet of a mixture of brown clay 
 and sand, to which succeeded eight feet of stratified drab clay. This 
 rests upon the uneven surface of the boulder formation. 
 
 Near Kingston, between the city and the Grand Trunk railway station, 
 Kingston, a narrow belt of what appears to be the upper clay occurs along the west 
 side of the Cataraqui River. The railway cutting exposes a thickness of 
 about fifteen feet, which is in thin slightly undulating layers, and is thickly 
 studded with very rough irregular calcareous nodules, generally of small 
 size. In one of these, a valve of Cyclas was met with. Annular and tubular 
 concretions, from a quarter of an inch to an inch in diameter, are very 
 abundant in some parts of this deposit. In the townships in the rear of 
 Kingston, a similar brown clay often occupies the level portions between 
 the rocky ridges. Dr. Lawson has observed the leaves of a plant resem- 
 bling a Vaccinium in a laminated brownish clay at Newborough. He 
 also found near Frankville, in the township of Kitley, brown clay with 
 nodules, like that of Kingston, lying upon a blue clay, which yields white 
 bricks, and probably belongs to the lower division. At Easton's Corners, 
 in Wolford, also, a hard jointed clay, yielding white bricks, is said to be 
 unconformably overlaid by a soft drab clay, which becomes red by burn- 
 ing. In the cutting for the Brockville and Ottawa railway, at Brockville, 
 a bluish clay holding boulders is overlaid by several feet of brownish clay. 
 The plane of contact of these two clays slopes toward the St. Lawrence. 
 On the south side of Lake Ontario, in New York, clays belonging to the 
 two divisions are again met with. 
 
 In the metamorphic region north of Lakes Superior and Huron, and 
 between the latter lake and the Ottawa, thinly bedded clays have been 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 905 
 
 found in the valleys of many of the rivers. Between McKay's Mountain 
 and the Grand or Kakabeka Falls of the Kaministiquia, the banks of the Supen 
 river often consist of laminated buff-colored clays, covered by yellow sand, 
 which together attain the height of sixty feet. Nodules, which have been 
 washed from the clay, are found in abundance on the edge of the river. 
 Red clay is seen on the bank of the Batchehwahnung, under a high cliff of 
 sand and gravel, at the distance of a mile and a half in a straight line from 
 the mouth of the river. On the Schibwah River, red and drab clays, in 
 very thin alternating layers, are found about two miles from its mouth, in 
 a direct line from the bay. One bed contains an abundance of thin flat- 
 tened nodules ; and some of the clay at the surface was found to be thickly 
 perforated with small tubular holes filled with sand, which, though they 
 recall the Scolithus of the Potsdam formation, are probably the burrows of 
 the larva of some insect. At thirteen miles up the Goulais River, in a 
 straight line from its mouth, a deposit of similar clay, -resting on solid rock, 
 and running under a bed of sand, has a thickness of upward of sixty feet. 
 Numbers of large and curiously formed nodules were found in the clay at 
 this place, but none of them contained organic remains. 
 
 At the upper termination of the town plot, on the right bank of the G<miai 
 Goulais River, there is a deposit of the roots and limbs of trees, imbedded E 
 in a bluish scaly material, apparently a mass of compressed leaves and 
 moss, which rests upon a bed of clay, and is overlaid by a mixture of clay 
 and sand : the whole, with a stratum of sand at the top, constitutes a bank 
 of from twenty to twenty-four feet high. The bed of vegetable matter, Fossil wood, 
 which is from one to three feet thick, and about ten feet over the river at 
 the western end of the exposure, dips gently and evenly up the stream ; 
 while a thin bed of reddish clay, intervening between the overlying arena- 
 ceous clay and the stratum of sand which forms the surface, seems to be 
 perfectly horizontal. 
 
 On the south side of Lake Superior, between White-fish Point and the 
 Painted Rocks, a great deposit of sand, interstratified with gravel, is spread 
 over the surface of the country. At the Grand Sable, a short distance Grand sable, 
 west from the Grand Marais, it rises here and there almost vertically from 
 the lake to a height of 300 feet. At the parts most exposed to the winds 
 of the lake, such as at White-fish Point, the sand is piled up in dunes or 
 sub-conical hillocks ; but in more sheltered parts, where covered by vege- 
 tation, it is arranged in a series of terraces, which rise one above another 
 with considerable regularity, attaining in the highest terrace an elevation 
 of more than 150 feet above the water. Along the coast, a bluish-drab 
 clay occasionally crops out from ftelow the sand, which west from Two 
 Heart River is in several parts overlaid by an accumulation of roots and 
 limbs of trees, in various stages of decay, occurring at a variable height of 
 from twelve to twenty feet above the water, and in all respects resembling 
 
906 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 the bed on Goulais River, except that it sometimes presents a thickness of 
 twelve or fourteen feet. The bed of vegetable matter at the Grand Sable 
 is covered by a layer of mixed sand and clay, above, which the hill of 
 interstratified sand and gravel, which may belong to the Algoma division, 
 rises abruptly to the height already stated. The vegetable remains are 
 of recent species, among which are the stems and branches of what appear to 
 be the white cedar, Thuja occidentalism the white birch, Betula paperacea^ 
 and the balsam poplar, Populus lalsamifera, occur. The bark of the birch 
 is only partially decayed. 
 
 st. Mary Behind the Sault Ste. Marie, a terrace, varying in its height, but aver- 
 aging perhaps one hundred and fifty feet above Lake Superior, and often 
 composed of clay in red and drab layers, stretches from the Laurentide 
 hills southward toward the St. Mary River. About a mile below, and 
 again about four miles above the foot of the Sault, this terrace comes near, 
 the edge of the river, and recedes in sweeping curves in both directions 
 from each of these points. A bay, two miles and a half in depth, is thus 
 left between them, and is occupied by a barren plain of no great elevation 
 above the river, partly covered with coarse brown sand, and partly strewn 
 with boulders of northern metamorphic rocks, and angular fragments of 
 Silurian sandstone, which are sometimes arranged in small bare ridges 
 parallel to the present direction of the river. The surface has thus the 
 appearance of having formerly been covered with swiftly flowing water. 
 
 Thinly stratified red and drab clays, with beds containing nodules in great 
 numbers, occur in several places in the lower part of the Garden River. 
 Many of the nodules were broken, and found to be devoid of organic 
 remains. A considerable depth of brownish-drab thin bedded clay, holding 
 nodules, is also seen in the banks of the Thessalon and Mississagui Rivers. 
 The sections met with farthest up the Mississagui, and its tributary the 
 Little White River, exhibit near their summits thin seams of yellow sand 
 interstratified with the clay, and the whole deposit is overlaid by the same 
 kind of sand. On the Little White River, the clay is fifty feet thick ; and 
 at one place a bed was observed to be curiously contorted, while those 
 above and below it were even and undisturbed. A similar structure 
 occurring in the palaeozoic shales of Gaspe*, has been figured on page 392. 
 The clay deposits of the Mississagui and Little White Rivers do not attain 
 an elevation of more than 160 feet over Lake Huron, or 738 feet above the 
 sea. A similar clay is often seen under the sand in the banks of the Span- 
 ish River, below the White-fish branch ; and a portion of the same kind 
 of clay exists on a small island near the north shore, six and a half miles 
 east of the Hudson Bay Company's post at Lacloche, and directly opposite 
 the highest mountain in the neighborhood. At the elbow of the Nahma- 
 nitigon or Red Clay River, which enters the southeast corner of Lake 
 Nipissing, stratified red, blue, and buff clays, holding spherical nodules, 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 907 
 
 occur at an estimated elevation of 710 feet above the sea. Laminated 
 brownish-drab clay has been found in three places in the upper part of the 
 Meganatawan River. The highest of these has an elevation of about 1000 
 feet above the sea. Drab clay of the same character was found between 
 Ox-tongue Lake and the Lake of Bays, on the upper part of the Muskoka Muskoka. 
 River. Clay, probably similar to these just noticed, is also met with among 
 the hills in the townships between Georgian Bay and Lake Simcoe. 
 
 It will be perceived that the clays just described, in this northwestern 
 part of the province, although occurring in isolated patches of no great 
 extent, are all Of the same general character, and appear to belong to one 
 age, supposed to be that of the Saugeen clay ; with which, in the absence 
 of any evidence to the contrary, they may for the present be classed. 
 
 ALGOMA BAND. 
 
 To the north of Lake Huron, and between Georgian Bay and the Ottawa 
 River, part of the surface of the country consists of bare rock, but where 
 any superficial covering exists, it is almost invariably a yellow sand. This Yellow sand. 
 also overlies the clays of this region, which have just been described, and 
 are exposed only in river cuttings. This sand is most largely developed 
 along the principal rivers of the district, and it also covers St. Joseph's 
 Island, and part of the Grand Manitoulin ; while to the westward of Lake 
 Huron, the sands already alluded to on the south side of Lake Superior 
 probably belong to the formation. It is largely developed on the Dog and 
 Kamuiistiquia Rivers, and spreads over a considerable tract below the Great 
 Falls of the Michipicoten, as well as over a smaller area on the Batcheh- 
 wahnung River. The Goulais River, in its lower stretch, flows in a very 
 tortuous course between mountain ranges, through a wide and fertile valley, 
 which has yellow sand as a subsoil over a great part of its area. This yel- 
 low sand also extends far and wide over the higher table-lands of the Thes- ihessaion. 
 salon and Mississagui Rivers. On either side of the Spanish River, below the 
 great bend, it forms an extensive plain, bearing a heavy growth of pines, 
 and it is also found in large patches north of that part of the coast lying 
 between the mouths of the Mississagui and Spanish Rivers. About 
 Grand Portage on the Mississagui, gravel takes the place of the clay and 
 sand which are found farther down in the valley, and becomes coarser and 
 more prevalent in ascending the river. At its intersection with Salter's 
 base line, the Mississagui is 830 feet over the level of the sea ; and farther 
 up, the banks and flats of the river are covered with coarse shingle and 
 boulders. The sand is widely spread almost all along the valleys of the 
 White-fish and Sturgeon Rivers, the upper reach of the Wahnapitae, and 
 the head branches of the Meganatawan. Similar sands extend from the 
 Muskoka Lake, up the river of the same name, into the Lake of Bays. The 
 
908 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. XXII. 
 
 Lake deposit surrounds Lake Nipissing, with a varying breadth, on all sides 
 smg< except the south, and appears to be extensively developed between this 
 lake and the Ottawa. It is reported to be pretty continuous over the whole 
 district between the line of the Mattawa and Lake Nipissing on the north, 
 and the head waters of the Meganatawan and Muskoka to the south. Below 
 Cedar Lake the Petewahweh is flanked on either side by a wide plateau 
 formed of yellow sand, which is again largely developed on the Bonne- 
 chSre, above the third chute, and covers much of the country between this 
 river and the Madawaska. It likewise occupies a considerable area around 
 Lake Kamaniskaik, and between Muskrat Lake and the Bonnechere. 
 
 Much of the region thus covered, lies within the district of Algoma, and 
 this great arenaceous deposit may hence be conveniently designated as the 
 Algoma sand. It has hitherto proved unfossiliferous, and it is uncertain 
 what relation it bears to the fossiliferous sands farther down the Ottawa, 
 which will be described in the sequel. 
 
 Algoma 
 sand. 
 
 ARTEMISIA GRAVEL. 
 
 Gravel. 
 
 A belt of loose gravel, remarkable for its great extent, stretches in a 
 southward direction across the peninsula of western Canada, from near 
 Owen Sound to Brantford, a distance of 100 miles. Its average breadth, 
 not including that of the extreme points, is twenty-three miles, and its 
 total area more than 2,000 square miles. The limits of this great gravel 
 deposit are approximately as follows. Its northern extremity is in the 
 southwest corner of Sydenham, and from this point its western boundary 
 runs nearly straight to the west side of Bentinck. Proceeding thence with 
 a slight curve to the eastward, it intersects the east half of the south line 
 of Normanby. The curve is now reversed, and takes in the northeast 
 corner of Minto, and the northern half of Arthur. Entering Luther, it 
 again curves to the east, and includes the southwest part of that town- 
 ship. From the centre of the south line of Luther it proceeds in a direct 
 course to the north side of Wilmot, thence to the northern part of East 
 Oxford, where it turns eastward, and comes to the Grand River near 
 Brantford. 
 
 Again, starting from the southwest corner of Sydenham, its eastern boun- 
 dary is traced across Holland to about the centre of the west line of Eu- 
 phrasia, and, after forming a northward spur in that township, it reaches 
 the Beaver River in the north of Artemisia. From this point, it proceeds 
 northeastward, and curves round, making a promontory which includes a 
 small portion of Collingwood, and the greater part of Osprey. It forms a 
 westward sinus in Melancthon, continues thence into Mono, and runs out in 
 a long spur between Albion and Ajala, in the direction of the Oak Ridge. 
 Leaving the south side of this spur, it continues from the southwest line of 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 909 
 
 Caledon, with a gentle curve to the eastward, till it reaches the centre of 
 Puslinch ; bisects the north line of Beverley, and after forming a spur in 
 that township, returns nearly to its northwest angle, and follows its west- 
 ern line for several miles, and then crosses the southeast corner of South 
 Dumfries, and reaches the Grand River just below Brantford. Within 
 the above limits the gravel is continuous over almost the whole surface. 
 
 This great belt of gravel has a general parallelism with the Niagara 
 escarpment, and follows the highest ground of the peninsula. The mate- source of the 
 rials composing it consist principally of the ruins of the Guelph formation, gra 
 on which the greater part of it lies, except toward the southern extremity, 
 where the Niagara formation is largely represented. Pebbles of Lauren- 
 tian and Huronian rocks are everywhere mixed with the others, and some- 
 times form a considerable proportion, while rounded fragments from the 
 harder beds of the Hudson River formation occur locally in some abun- 
 dance. The gravel is all well rounded, and generally coarse ; it often 
 Constitutes what might properly be called shingle, being loose and free from 
 any admixture of clay; and it is distinctly stratified. Well worn boulders 
 of Guelph, Laurentian, and Huronian rocks are disseminated through the 
 whole mass, and wherever the gravel has been dug for road-making, there 
 may be found heaps of these, which have been thrown aside. 
 
 An extensive spur of gravel runs from this area to the northeast, con- The oak 
 stituting what is called the Oak Ridge, which has been described by Mr. Ridge - 
 T. C. Keefer. It leaves the great Middle Silurian escarpment in the 
 northern part of Albion, and runs eastward as far as Darlington, where it 
 curves southward into Clarke. It thence runs almost straight to the great 
 bend of the Trent in Sidney, and continues in the same course a short 
 distance beyond it. The general course of the ridge thus presents a 
 southward convexity, while the north shore of Lake Ontario curves in the 
 opposite direction. The ridge appears to be composed wholly of sand and 
 gravel ; and -its greatest elevation behind Toronto, where it is probably 
 higher than at any other part, is 720 feet over Lake Ontario, or 950 feet 
 above the sea. Near the summit of the ridge, in Sidney, there is a lake 
 which has no visible inlet, but gives rise to a mill-stream. A similar lake 
 is situated on the continuation of the ridge near the Pinnacle House, on 
 Yonge Street, and not far from the summit of the water-shed. 
 
 The relations of this Artemisia gravel to the Algoma sand, and to the 
 sands and clays of the upper or Saugeen division, have not yet been fully 
 determined. Near Brantford, however, it is seen to overlie a blue 
 clay, which belongs to the Erie division ; and in the village of Mount 
 Forest, as already stated, it rests unconfonnably upon a fine blue clay. 
 
910 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 ANCIENT BEACHES, TERRACES, AND RIDGES. 
 
 Lacustrine Besides the upper clays and sands already described in western Canada, 
 there are several local accumulations of sands, often marked by fresh- 
 water shells. These, together with various ridges and terraces, which are con- 
 spicuous features in the surface geology of this region, appear for the most 
 part to have been formed by the waters of the great lakes, when their 
 extent was much greater than at present. The most considerable deposit 
 of this kind is probably the sandy tract in the county of Simcoe, which 
 extends southeastward from the head of Nottawasaga Bay, and has an area 
 of rather more than 300 square miles. It has been described by Mr. 
 Sanford Fleming, and may be said to cover the whole of Sunnidale, the 
 greater part of Vespra, the western quarter of Flos, the northeastern third 
 of Nottawasaga, the northern half of Tossorontio, and the northern half 
 of Essa. The sand, which is of a yellowish-grey color, appears to be of 
 considerable depth. In Flos and Sunnidale, the Nottawasaga River flows 
 for some distance between banks of sand, from seventy to eighty feet in 
 height, holding fresh-water shells. These are also found in the sand all 
 along the Nottawasaga River, from four miles south of its intersection 
 
 Fresh-water with the Northern railway, to its mouth. At Angus station in Essa, 
 on the west bank of this river, Professor Chapman collected the following 
 species, which were in fine sand underlaid by gravel, and were met with 
 from near the surface to a depth of eighteen feet : Unio complanatus 
 (very abundant), Cydas similis, 0. dubia, Amnicola porata, Valvata 
 tricarinata, V. piscinalis, PlanorUs trivolvis, P. campanulatus, P. bicari- 
 natus, Limncea palustris, and Physa ancillaria. The general level at 
 which these shells occur may be taken at from thirty to forty feet above 
 Lake Huron, and the locality is distant above twenty miles in a straight 
 
 Nottawa- j me f r0 m the mouth of the river. Farther down the Nottawasaga, about 
 twelve miles from its mouth, and at nineteen feet over Lake Huron, 
 Dr. Bigsby found in the bank of the river two horizontal layers filled with 
 shells of Unio. The layers are each from four to six inches thick, and 
 from one to two feet apart, and are beneath from eighty to one hundred 
 feet of sand. The shells are closely packed together, and some of them 
 have their valves in contact. Shells of the genera PlanorUs, Physa, 
 Limncea, Melania and Paludina are also met with in the same layers. 
 All of the species found here are now living in great numbers in the 
 Nottawasaga. The two layers above mentioned are continuous for three 
 miles down the river, and are occasionally seen all the way to the lake, 
 while numbers of shells are scattered through the sandy layers above them. 
 The sand, which is uniformly stratified, holds occasional portions of gravel, 
 and at one place three continuous layers of small pebbles occur half way 
 up the bank. It is underlaid by clay, which is often seen in the bed of 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 
 
 the river, and sometimes rises twenty feet above it. The Nottawasaga 
 River, before entering Lake Huron, runs for several miles parallel to the 
 shore, being separated from it by a narrow peninsula of sand. Behind 
 this, according to Mr. Sanford Fleming, a ridge of sand parallel to the 
 present shore, rises to a height of about eighty feet above the lake, and 
 appears to have formed a narrow neck of land reaching across the former 
 extension of the Nottawasaga Bay. Melania conica and M. Niagarensis 
 have been found in the sand, in a railway cutting near Collingwood, but 
 at no great elevation above Lake Huron. Planorbis trivolvis, with three 
 species of Helix, was found in sand and fine gravel in a road-cutting 
 through a little ridge between seventy-five and seventy-eight feet above 
 Lake. Huron, about a mile south of Collingwood harbor. In the .northern 
 part of Collingwood, at the base of the Blue Mountains, there is another 
 ridge of sand, the summit of which at Craigleith is not far from eighty feet 
 above the lake. ' A beach-mark at about the same height is seen running 
 from the northern extremity of Nottawasaga Bay into Essa, and another 
 one at Penetanguishine. Near Meaford, at the mouth of the Bighead Meaford 
 River, a succession of ridges and terraces of sand and gravel rise above 
 one another to about 150 feet above Lake Huron, and, winding along the 
 bank of the river, come upon the shore three miles to the north of Meaford. 
 Thence they are continued to Cape Rich. Fresh-water shells are found 
 in one of these terraces at a height of seventeen feet above the lake, and 
 are said to occur in another ridge at fifty feet. In sinking a well in 
 Meaford, so many prostrate trunks of trees were met with, about ten feet 
 under the surface, and about the same height over the lake, that the 
 digging was abandoned. Trunks of cedar and other trees are found 
 beneath about forty feet of sand near the river's mouth. Two miles to the 
 west of Cape Rich worn fragments of bark and wood are said to have 
 been met with in digging a cellar on a terrace 155 feet above the lake. 
 One of the principal ridges leaves the Silurian escarpment, with a height 
 of 160 feet, and, after running east for two miles nearly to Cape Rich and 
 gradually losing its elevation, ourves round and runs southward, parallel 
 to the shore, with a height of only forty-five feet. In its east and west 
 extension the ridge is very abrupt on the lake side, with a gentle fall to 
 the south ; but after rounding the cape it becomes steep on the landward 
 side, and presents a gradual slope of 300 yards to the lake. This slope 
 is thrown up into no fewer than fifteen regular parallel ridges of small 
 flattened shingle, the summit of each rising three feet higher than that of 
 the next below, or from four to five feet above the intervening depression. 
 Still smaller secondary ridges frequently lie between these, and join them 
 obliquely ; in exactly the same manner as the little ridges of shingle, which 
 are washed up by every storm, repose upon the slope of the lowest of the 
 series. The contours of these clearly show that forces similar to those 
 
912 GEOLOGY OF CANADA. [CHAP. XXII, 
 
 now in operation were acting at the time of their formation, and that the 
 prevailing direction of the winds was the same then as now. This curved 
 ridge encloses a marshy flat with a clay bottom, half a mile in breadth and 
 thirty feet above the lake. After crossing this flat, on the road leading 
 southwest from the cape, two other gravel ridges rise to sixty and eighty 
 feet, respectively, above the lake. The higher of these ridges curves in the 
 same manner as the ridge first described, and the other has probably a 
 similar form. A terrace covered with large rounded gneiss boulders comes 
 between the high Silurian escarpment and the highest ridge, 
 owon Another deposit of sand and gravel extends, with a gradual rise, from 
 
 the head of Owen Sound up the valley of the Sydenham River, for a dis- 
 tance of about three miles. In the town of Owen Sound, which stands upon 
 this deposit, twelve species of recent fresh-water shells were collected in the 
 sand, at elevations varying from nine to about fifteen feet above Lake 
 Huron. They consist of Limncea umbrosa, Planorbis campanulatus, 
 P. bicarinatus, P. parvus, Melania acuta y M. Niagarensis, M. conica, 
 Paludina decisa, Valvata sincera, V. tricarinata, Amnicola porata, and 
 Cyclas similis. About a mile south of the mouth of the Sydenham River, 
 some of the same species were found in the sand at forty feet above the 
 lake. On the west side of this sandy plain, trunks of trees are seen at 
 the edge of the river, projecting from the foot of a bank of gravel and 
 sand about thirty-five feet in height ; but their occurrence in this position 
 may be accidental. Besides this lacustrine deposit on the shores of Owen 
 Sound, there are several terraces of sand and gravel which occur at 
 much higher levels, and correspond to ancient water-margins about 120, 
 150, and 200 feet above the present level of Lake Huron. Some of the 
 higher terraces continue with great regularity several miles along the east 
 side of the Sound. At Piette's Harbor, on the west side of the Sound, 
 two ancient beaches are found ; one at 149 feet, and another about 175 
 feet above the lake ; besides others at lower levels. 
 
 isthmus i n Isthmus Bay, a set of small parallel ridges, composed of the debris 
 
 of the Niagara dolomite, rises from thev water's edge to a height of 
 about twenty feet above it. Behind these, ridges of the same material 
 succeed one another, attaining sixty or seventy feet above the lake. 
 Human bones, much decayed and broken, are found in great numbers in 
 one of these ridges between twenty-five and thirty feet over the water. 
 cast's Wingfield Basin at Cabot's Head, is partly surrounded by ridges of shin- 
 Hoad< gle about twenty feet above the lake ; but steps indicating former water- 
 margins are found at greater elevations between the basin and the high 
 cliffs in the rear. Dr. Bigsby notes the occurrence of a beach of rolled 
 pebbles at about 100 feet above the lake, on a small island near St. Joseph's 
 Lake Island. Terraces and ancient beaches are found in many places upon Lake 
 superior. Superior, but no recent fossils have as yet been found in them. Three 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 913 
 
 miles below the Petits Ecrits, seven terraces of sand and gravel rise above petit* 
 one another to a height of 931 feet above the sea-level. Their eleva- Ecnt *- 
 tions are respectively 30, 40, 90, 224, 259, 267, and 331 feet above the 
 lake. The third and fourth beaches are the best marked, and a marsh 
 500 yards in the rear, is on the same level as the fourth. Those 
 already alluded to in the sands on the south side of the lake probably 
 correspond with some of these. A few miles to the east of Black Black Hirer 
 River (opposite the Slate Islands), four successive steps rise to a height 
 of twenty feet over the lake, and are succeeded by another, twenty-five 
 feet higher ; while the sixth or uppermost is forty feet above this, making 
 its elevation above the lake eighty-five feet. In the bays between the 
 rocky points from the Montreal River to the Sault Ste. Marie, banks of 
 sand and gravel are found at various heights, from the level of the lake up 
 to thirty feet above it. On the north side of the lake, the ancient water- 
 margins are frequently marked by the wearing of the solid rock (page 
 701), as well as of the loose materials. The latter sometimes hold peb- 
 bles, which contain organic remains belonging to rocks newer than the 
 Niagara formation. 
 
 In the state of Ohio Mr. C. Whittlesey mentions a series of gravel Lake Erie, 
 ridges, rudely parallel with the southern shore of Lake Erie. The one 
 nearest to the lake extends for a distance of 120 miles, and has an average 
 height of 112 feet above the lake. The second, which is less continuous, 
 has an average elevation of 145, and the third 186 feet above Lake Erie. 
 The first and second of these are said to contain fresh-water shells. Similar 
 ridges doubtless occur along the northern shores of this lake, but have not 
 been much examined. A remarkable ridge of this kind is found in Raleigh. 
 
 The sandy flats which are met with in many places along the river Thames, 
 from St. Mary's to Chatham, contain land and river shells in great abun- 
 dance. At London the fine fluviatile sand rests upon a mixture of coarse London, 
 clay with sand and pebbles. Both the land and fresh-water shells, which 
 comprise many species, are disseminated throughout the deposit, to a depth 
 of seven feet, and perhaps more, but are most abundant in certain beds. It 
 is observed that the proportion of land shells greatly increases toward the 
 surface. Land and fresh-water shells are also abundant in the sandy 
 alluvions along the Grand River, between Brantford and Dunville ; and 
 similar flats, full of the same kind of shells, occur at some of the bends of 
 the Saugeen below Hanover. At the Falls of Niagara strata of fresh- Niagara 
 water sand are found on Goat Island, where they rest upon the boulder Falls - 
 formation, and in the ancient bed of the river, on each side of the gorge 
 below the Falls. On the Canadian side, sixteen species of common fresh- 
 water mollusca are found imbedded in the sand, evidently in the position 
 in which they had lived. They are Planorbis bicarinatus, Physa heteros- 
 tropha, Limncea caperata, L. stagnates, Melania Niagarensis, M. conica, 
 
 H* 
 
914 GEOLOGY OF CANADA. [CHAP. XXII 
 
 M. acuta, Paludina decisa, Amnicola porata, Unio gibbosus^ U.compla- 
 natus, U. ellipsis, U. rectus, Margaritana marginata, Cyclas similis, 
 and Pisidium dubium f , with one land species, Helix albolabris ? Prof. 
 Hall states the occurrence of a mastodon's tooth in a similar deposit on 
 the opposite side of the river. Fresh-water shells have also been met 
 with in the bank of loose material on the north side of the whirlpool. 
 
 Burlington Burlington Bay is separated from the western part of Lake Ontario by 
 a low sandy beach running northwesterly ; and five miles to the west of 
 this is a nearly parallel ridge, which stretches with a westwardly curve 
 across the marshes at the head of the bay, and constitutes Burlington 
 Heights, which have an elevation of 107 feet above the lake. This ridge, 
 which consists of alternate beds of sand, and of coarse and fine gravel, 
 overlies the Medina formation in its continuation through the western 
 part of the city of Hamilton. To the northward it terminates abruptly, 
 and is separated from the escarpment of this formation by a deep and 
 narrow ravine, which, until filled up by a railway embankment, served as 
 the outlet of the streams which enter the Dundas valley from the west- 
 ward. In making an excavation for the Desjardins Canal, the ridge was 
 found to be underlaid by the Erie clay, near the level of the lake. Toward 
 the top, many of the beds are cemented into a hard rock by infiltrated 
 carbonate of lime. At a height of seventy feet above the lake were 
 
 Mammoth's found several of the bones of the mammoth or fossil elephant, Eueleplias 
 Jacksoni, and in the same excavation, seven feet higher, the horns of the 
 wapiti, Cervus Canadensis, and the jaw of a beaver, Castor fiber, were met 
 with. To the west of the town of Dundas is an old water-margin, at an 
 elevation which seems to coincide with that of Burlington Heights ; while 
 on the north side of the town another ridge of sand and gravel, attaining 
 a height of 318 feet above the lake, occurs just under the escarpment of 
 the Niagara formation, which is about 100 feet higher. In its eastward 
 extension it recedes from the cliff, and, diminishing in height, disappears 
 at the end of a mile. It approaches the face of the escarpment on the 
 east side of Spencer's ravine, on the other side of which a still higher bank 
 of sand and gravel conceals the escarpment ; and was probably at one 
 time connected with the gravel ridge, which would thus have formed a bar 
 between the former outlet of Flamborough Creek and the waters which then 
 filled the Dundas valley. This creek has now excavated the solid rock 
 to a distance of half a mile back from the general line of the escarpment, 
 and cut the bar of sand and gravel at the mouth of the gorge to its base. 
 
 On the north side of Lake Ontario fresh-water shells .are found in the 
 banks of the Don, beneath a considerable thickness of sand, at about thirty 
 feet above the level of the lake. They also occur around Lake Simcoe, 
 imbedded in sands from eighteen to thirty feet above the lake. Toronto 
 Island,which is being constantly modified by the action of the lake, has 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 915 
 
 been shown by Mr. Sandford Fleming to have resulted from the westward Toronto 
 drifting of the materials derived from the wearing down of the Scarborough 8 
 Heights, 320 feet high ; and Long Point, in Lake Erie, appears to have 
 been formed in the same way, by the gradual drifting of sand and gravel to 
 the eastward. An exact counterpart of Toronto Island is presented by 
 the Davenport ridge, described by Mr. Fleming. This ridge, which con- 
 sists of fine rounded gravel, runs to the westward from the high ground 
 behind Toronto, which is from 250 to 300 feet above Lake Ontario, in the 
 same manner as Toronto Island extends from the Scarborough Heights. 
 The gravel beds of this ridge all dip to the southward, and rounded lumps 
 of fine clay are of common occurrence among them. Their presence is 
 accounted for by supposing them to have been rolled, perhaps when in a 
 frozen state, by the waves of the ancient lake. This ridge, the summit of 
 which is about 170 feet above Lake Ontario, is about seven miles to the 
 northwest of Toronto Island. In a paper presented to the Geological 
 Society of London, in 1837, Mr. Thomas Roy states the occurrence of 
 thirteen ancient water-margins between Toronto and Lake Simcoe, at the 
 respective heights over the sea of 342, 442, 514, 542, 578, 634, 654, 
 734, 790, 858, 914, 966, and 996 feet. It is stated by Prof. Hall that 
 on the south side of Lake Ontario, a conspicuous ridge runs eastward Wayne 
 from Lewiston into Wayne County, a distance of 100 miles, with a general Count y- 
 parallelism to the shore of the lake. The elevation of its summit varies 
 a few feet, but it is supposed to have been thrown up when the water stood 
 about 175 feet higher than the present surface of Lake Ontario, and in its 
 elevation corresponds very well with the Davenport ridge. It holds no 
 marine shells, but species of Unio are said to have been discovered in it. 
 
 STRATIFIED CLAYS AND SAND Off EASTERN CANADA. 
 
 The valleys of the St. Lawrence and the Richelieu, in Canada East, and 
 a considerable portion of the region between the St. Lawrence and the 
 Ottawa, to the east of the meridian of Kingston, are occupied by stratified 
 clays ; which, unlike those of western Canada, contain abundance of marine 
 shells, for the most part identical with species now living in the lower St. 
 Lawrence and the gulf. These clays are in many cases overlaid by sands, 
 occasionally interstratified with clay, which also contain marine remains. 
 The two are regarded as forming parts of one formation, and as corre- 
 sponding to the upper and lower divisions of the Champlain clay of the Champiam 
 Vermont geologists. Dr. J. W. Dawson, who has carefully studied these c] * y ' 
 deposits in Canada, distinguishes the lower as the Leda clay, from one of Leda clay, 
 its characteristic shells ; and the upper, for a similar reason, as the Saxi- 
 cava sand. He considers the one as having been formed in shallow waters, 
 and the other as a deep-water deposit, and conceives that portions of the 
 
916 GEOLOGY OF CANADA. [!HAP. XXII. 
 
 two divisions may have been contemporaneous. In some places, as at Beau- 
 port, the clay appears to be wanting, and a layer of sand contains the 
 fossils of the lower division, which is, in its turn, covered by the Saxicava 
 sand. In other parts, as in Vermont, considerable portions of brownish 
 clay are interstratified with this upper sand. 
 
 Distribution. If a i me be drawn from the outlet of Lake Champlain to Ottawa, and 
 from the extremities of this, as a base, two others be carried to Quebec, 
 there will be included a very level triangular area of about 9,000 square 
 miles, for the greater part covered by the Champlain clays and sands. 
 The plains on either side of the St. Lawrence below* Quebec are occupied 
 by the same formation, which is found at intervals as far down as 
 Matanne ; while on the north side, it covers an extensive area in the valley 
 of the Saguenay, and around lake St. John and its tributaries. The clay 
 itself in many cases forms the surface soil ; but in the higher portions of 
 the area it is very often overlaid by sands, which form a complete border 
 
 Lower clays, around the triangular district just indicated. Clays belonging to the 
 lower division are however found at various levels from the surface of 
 the sea to 600 feet above it, and in some cases they have been observed 
 some feet below the sea-level. The lower clay is ordinarily more or less 
 calcareous, and bluish. Occasionally, however, it is interstratified with 
 beds of grey, brown, and reddish colors, and it generally contains but few 
 pebbles or boulders. The sands of this formation are silicious, and appa- 
 rently derived from the Laurentian rocks. They frequently contain grains 
 of magnetic iron ore and of garnet. 
 
 Ottawa. Along the south bank of the Ottawa River, from the city of Ottawa 
 
 to Hawkesbury, and again from Point Fortune to its junction with the 
 St. Lawrence, the lower clay is seen in banks of from twenty to forty feet 
 in height. The river is 118 feet above the sea at Ottawa, and about sixty 
 feet lower in its eastern part ; so that the clays, from Point Fortune down- 
 ward, although precisely similar in character to those farther up the river, 
 are at a lower level. The overlying sand generally approaches to within 
 a short distance of the river, concealing the clay, except along the streams. 
 The greatest breadth of the level clay surface which has been observed 
 here is in the township of L'Orignal, where it extends about fifteen miles 
 back from the river. Small numbers of the shells of Saxicava rugosa and 
 Tellina Grroenlandica are found wherever these clays have been recognized 
 
 Green'* along the Ottawa. About the mouth of Green's Creek, in Gloucester, a 
 bed in the clay, near high-water mark, abounds in nodular masses, which 
 are strewn along the shore of the Ottawa for two miles to the eastward. 
 These seem to have been formed by a process of concretion around various 
 organic remains, which are found on breaking open the nodules. Among 
 the fossils imbedded in these are fishes, of which the most abundant is the 
 Mallotw villosuS) or capeling of the lower St. Lawrence. A single speci- 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 917 
 
 men each of the Cydopterus lumpus, or lump-sucker, and of a species of Fossa fiehos. 
 Coitus, has been found here. Several specimens of a common star-fish, 
 and numbers of marine shells, including Tellina G-rcenlandica and Saxicava 
 rugosa, are also met with here ; besides which are a species of fresh- 
 water shell, and various land-plants. Among the latter, Dr. Dawson has Land plants, 
 recognized the following species : Drosera rotundifolia, Trifolium repens, 
 Potentilla Norvegica, P. tridentata , P. Canadensis, Arctostaphylos uva- 
 ursi, Populus balsamifera, Potamogeton perfoliata, and P. natam ; 
 besides grasses, carices, mosses, and algae. The height of this deposit is 
 118 feet above the sea. The capeling is also found in nodules in clay on 
 the Chaudidre Lake, at 183 feet ; on the Madawaska, at 206 feet ; and at 
 Fort Coulonge Lake, at 365 feet above the sea. 
 
 The clays of this series are well seen along the tributaries of the Ottawa, 
 in the seigniories of Vaudreuil, Soulange, and Rigaud, and also on the 
 South Petite Nation River. On the Riviere a la Graisse, in Rigaud, the Rigaud. 
 inferior parts of the section exhibit an exceedingly fine bluish or greyish 
 calcareous clay, free from pebbles, overlaid by a similar clay, brownish in 
 color, in which is interstratified a band of reddish clay from one to two feet 
 in thickness. Analyses of these clays will be found on page 641. Very 
 similar sections occur on the same river, in Hawkesbury and Lochiel, and 
 also on the Rivieres de File and Baudette. Clays of this series are 
 observed on the St. Lawrence as far up as Dickinson's Landing, where a fine 
 brownish calcareous variety is overlaid by a coarser clay holding pebbles 
 and boulders derived from the Calciferous formation, with others of Lau- 
 rentian origin. These clays occupy the banks of the river, for the most 
 part, down to the Cascades. 
 
 On the north side of the Ottawa, from Hull to Isle Jesus, the clay often 
 covers a considerable breadth between the river and the Laurentian hills, 
 and extends among these for several miles up the larger tributaries. The Hirer Rouge, 
 river Rouge enters the Ottawa between hills of bare rock ; but on its 
 western side, in the fourth range of Grenville, a bank of clay 125 feet in 
 thickness occurs, the summit of which is 405 feet above the sea. Again, 
 not far east of this river, in the rear of Grenville and in the front of Har- 
 rington, is an area of several hundred acres underlaid by stratified blue 
 clay, the surface of which is about 500 feet above the sea. Several similar 
 portions of clay are found in this vicinity. These higher clays have as yet 
 yielded no fossils ; but Tellina G-roenlandica, Saxicava rugosa, Balanus 
 Hameri, and B. crenatus are found in a clay 120 feet above the sea in 
 the bank of the Ottawa, in Grenville. 
 
 The superficial deposits in the vicinity of Montreal have been more care- Montreal, 
 fully studied than those of any other part of Lower Canada; and Dr. Dawson, 
 who has devoted much time to their examination, has published hi The Ca- 
 nadian Naturalist a description from which the following details are taken. 
 
918 GEOLOGY OF CANADA, [CHAP. XXIL 
 
 The isolated mass of intrusive rock which rises about 750 feet above the 
 sea, and forms the mountain of Montreal, exhibits upon its sides a series of 
 ancient beaches, serving to mark the stages by which the land rose to its 
 present level > after the tertiary period. The most strongly marked of these 
 ancient sea-margins are at heights of 470, 440, 386, and 220 feet over 
 the sea-level, the St. Lawrence at Montreal being considered as twenty feet 
 above the sea.* The highest of these beaches is on the property of Mr. D. 
 
 cdtedes Davidson, above C6te des Neiges. A section of it exhibits, in descending 
 order : I. Eight feet of angular stones and sand. II. Five and a half 
 feet of fine gravel, with inclined layers of shells, chiefly Saxicava rugosa. 
 III. Six feet of stratified sand, with a few shells. These beds are of very 
 limited breadth, and rest against the steep side of the mountain, fronting 
 the mouth of the Ottawa. They are evidently the remains of a beach thrown 
 up in a little cove or strait between the two summits of the then partially 
 submerged hill, and are the highest recent fossiJiferous deposits known 
 in Canada. 
 
 sherbrooke Below the lowest terrace, and about 100 feet above the St. Lawrence, in 
 the plateau along Sherbrooke Street, the stratified deposits consist of fine 
 grained sand, in some places underlaid or replaced by stratified gravel, and 
 holding shells in its lower portion. This sand is underlaid by an unctuous 
 calcareous clay, w T hich is grey, occasionally with brown and reddish colors, 
 and also holds marine shells. This rests upon the clay of the boulder 
 
 Boulder formation, which is filled with rounded and striated fragments of various 
 
 formation. rQckg> T ke total thickness of these deposits is at least 100 feet, of which 
 the boulder formation forms the greater part. The sand however often 
 attains a thickness of ten feet, and the fine clay occasionally amounts to 
 twenty feet. These stratified deposits also sometimes contain boulders 
 
 Mount both of Laurentian rocks, and of the dolerite of the mountain. Dr. Bigsby 
 long since observed that the boulders derived from the latter source have 
 been drifted principally to the southwestward ; in which direction they are 
 said to have been traced for a distance of 270 miles, to the south shore of 
 Lake Ontario, marking the direction of the ancient currents or glaciers as 
 having been from the northeast. It is to be remarked that the northeast side 
 of the mountain is bare and abrupt, and it is there that the successive ter- 
 races may be best observed. On this side as elsewhere, the rocks beneath 
 the boulder formation are polished and grooved. The directions of the striae 
 are there from 40 to 70 degrees east of north. In many places, the 
 surface of the boulder formation, beneath the stratified clay, has been deeply 
 
 * In the report of the Board of Works for 1845, it is stated by the Hon. H. H. Killaly, 
 then President of the Board, that the summer level of the St. Lawrence in the harbor of 
 Montreal, is 12-& feet over the summer level of Lake St. Peter, and the level of this 
 lake is the datum (see page 109) from which the heights of the great lakes, and of other 
 elevations in the interior of Canada, are usually estimated. 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 919 
 
 furrowed, as if by currents ; and in like manner, the surface of this clay is 
 sometimes cut into trenches, which are filled by the overlying sand. On 
 the other hand, in places more sheltered, the boulder formation passes into 
 the fine clay, or into gravel, and the latter into sand. It is in such local- 
 ities, where evidences of denudation are absent, that marine fossils most 
 abound. 
 
 Th# city of Montreal is built upon the deposits just described. Near 
 the base of the mountain, at about 100 feet above the river, a fine yellow- 
 ish sand is seen in many places. Excavations near McGrill College MCGHI college 
 showed this sand resting upon a very fine unctuous grey clay, both con- 
 taining a few boulders, and underlaid by the boulder formation, which comes 
 to the surface toward the foot of the mountain. In some places the sur- 
 face of the clay is cut into furrows, which are filled with sand ; but in others 
 the sand rests upon an unbroken surface, and a layer of greyish sandy clay 
 forms a transition between them. The sand here contains no shells, but 
 the intermediate bed of sandy clay holds ten species, chiefly of common 
 American littoral shells. Among these Saxicava and Tellina predomi- 
 nate. The clay beneath contains but few shells, and these are of two species, 
 the so-called Leda Portlandica, which is now identified with the living 
 arctic species L. truncata, and Astarte Laurentina. Of the species 
 observed in these deposits, the latter is the only one which has not yet been 
 found living in the present seas. Both of these shells occur chiefly in the 
 upper layers of the clay, and they haye their valves attached. In a continua- 
 tion of these beds, an excavation below Sherbrooke Street discloses twelve 
 feet of the Leda clay, in layers of from half an inch to three inches, 
 separated by very thin partings of sandy clay containing small shells and 
 fragments. Near the bottom is a thicker sandy layer holding numerous 
 shells of mollusca, together with foraminifera. 
 
 At the Mile-end quarries, upon a slight ridge, are found stratified sand Mile-end, 
 and gravel, holding boulders and shells in the lower part. The deposit 
 sometimes rests directly upon the limestone rock, which is at other times 
 covered with a thin layer of the boulder formation. The lower clay is here 
 wanting, having perhaps been removed by denudation. A thick deposit 
 of this clay is however seen at the brick-yard of Messrs. Peel & Comte 
 near by, where it is overlaid by the Saxicava sand, and has furnished 
 one of the pelvic bones of a seal, and several of the caudal vertebrae of Bones of 
 a cetacean, Beluga Verrnqntana; besides fragments of the white cedar, thewha! <- 
 Thuja occidentalis. 
 
 Between the little ridge at the quarries and another caused by a trap Logan'* 
 dyke near the house of Mr. James Logan, is a slight depression holding farm- 
 an accumulation of beds rich in fossils, which present the following section. 
 Beneath about two feet of soil and sand, underlaid by a very thin stratum 
 of clay, are found eight inches of grey sand, holding in small numbers, 
 
920 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXII. 
 
 Bones of 
 *eaJs and 
 birds. 
 
 J^achine 
 road. 
 
 Victoria 
 Bridge. 
 
 Saxicava, Mytilus, Tellina, and Mya; the valves generally united. Then, 
 after about a foot of tough reddish clay, containing a few specimens of 
 Astarte and Leda, succeeds another layer of grey sand, of the same 
 thickness as the former, and holding the same fossils, besides Balanus and 
 Trichotropis ; the shells being in three thin layers. Below this are fifteen 
 inches of sand or clay holding Saxicava, and resting upon a layer of three 
 inches of sandy clay, which is rich in deep-sea shells, foraminifera, and 
 sponges. The white silicious spiculse of the latter {Tethea Logani of 
 Dawson) resemble tufts of asbestus. Two feet of sand and clay, with a 
 few fossils, including foraminifera and algae, with Lepralia attached, con- 
 clude this section of about eight feet ; which rests upon a stony clay 
 belonging .to the boulder formation. In a thick deposit of clay about three 
 quarters of a mile to the east of this, and about forty feet lower, in Messrs. 
 Peel & Comte's clay-pit in St. Mary's suburbs, there have been obtained, 
 in addition to several species of marine shells and the spiculse of sponges, 
 the skeleton of a seal, Phoca Groenlandica. At Messrs. Buhner & Shep- 
 herd's brick-yard, close by, several of the bones of a young seal were met 
 with, and a few of those of other animals, including one or two which 
 appear to be the bones of a bird. The brick-yard at the Tanneries 
 exhibits many of the above enumerated marine shells at the summit of 
 the lower clay, and in the overlying sands. 
 
 Besides the localities already mentioned, the boulder formation is seen 
 in excavations in Dorchester and LagauchetiSre Streets, and in the gravel 
 pits on the Lachine railway. The steep descent at Beaver Hall, and 
 farther on, along the Lachine road, marks the limit of the cutting formerly 
 made by the St. Lawrence in these superficial deposits. In the ancient 
 river-bed in Craig Street, and near the Tanneries, the river gravel is met 
 with, occasionally with fresh-water shells. In some parts the action of 
 the river has laid bare the grooved surfaces of rocks beneath. Far out in 
 the river, in sinking for some of the piers of the Victoria Bridge, a great 
 thickness of the boulder formation was met with ; and in dredging in 
 the current immediately below the city, the material brought up was 
 apparently the ancient marine clay, and it contained the shells of Tellina. 
 Similar clays are found by dredging in Lake St. Peter. 
 
 Clays which belong to the lower division, and are employed for the manu- 
 facture of bricks and coarse pottery, are found in very many localities 
 along the valleys of the Richelieu, and on both sides of the St. Lawrence 
 as far as Quebec. In many places bands of a brownish-red color are 
 interstratified with the bluish or ash-grey clay, and exhibit a jointed 
 structure, which causes them to split into thin vertical plates and prisms. 
 A good example of this interstratification is seen in a cliff of clay eighty- 
 five feet in height, in the Little RiviSre du ChSne, in the seigniory of Des- 
 chaillons. Near this is Cap a la Roche, which rises 155 feet above the St. 
 
CHAP. X^II.] SUPERFICIAL GEOLOGY. 921 
 
 Lawrence ; being the highest land in that vicinity. It presents the following 
 section in ascending order. After five feet concealed at the water's edge, 
 are twenty feet of yellowish-grey sand, with layers of black magnetic iron 
 sand ; the deposit being coarser and less yellow toward the base. To this 
 succeed ninety feet of bluish impalpable clay, with grey and brown bands ; 
 above which is a narrow terrace, strewn with gneiss boulders, where the 
 strata are concealed. Then follow five feet of ochreous sand, forming a 
 broader terrace ; beyond which is the third and highest step of thirty feet, 
 which is supposed to be partly of yellow and partly of grey sand, and is 
 strewn both at the base and summit with gneiss boulders. This overlying 
 sand is wanting a little farther down the river ; where the high banks in 
 Lotbmie^re appear to be in many parts composed of clay to the summit, 
 although in other parts capped by sand. At St. Jean-Deschaillons red bricks 
 are extensively manufactured from the clay ; which is said to be upward 
 of 100 feet in thickness, and to repose upon a bed of twelve feet of sand. 
 These sections are interesting as showing stratified sands beneath a great 
 thickness of the lower clay. At St. Nicholas numerous fossil shells have st. Nicholas. 
 been found in a sandy clay, 180 feet above the sea, and at the head of 
 a rocky ravine about 400 yards south of the St. Lawrence. On the north 
 shore, about twelve miles up the Jacques Cartier River, the lower clay is 
 again met with, holding shells of Tellina and Astarte, and overlaid by 
 twelve feet of sand. 
 
 Below Quebec, the lower clay extends in a nearly continuous belt from 
 Point LeVis to Matanne. Marine shells are found in clay at the sea-level 
 on the east side of the bay at the mouth of Riviere du Loup, but from this Riviere du 
 locality to Cacouna, the surface of the clay slopes up to a height of more Loup ' 
 than a hundred feet. At Rivi&re du Loup, the shells of Mya and Tdlina 
 are found imbedded in the sand and disintegrated shale of an ancient 
 beach, only a few feet above the present sea level. Similar beaches, which 
 seldom attain more than fifteen feet above high-water mark, are met with 
 in many localities along this southern shore, from Riviere du Loup to the 
 Magdalen River. A low terrace, about five feet above the highest tides, 
 and averaging about 100 yards in breadth, extends, with a few interrup- 
 tions, from Rimouski to Whale Cape, a distance of seventy-five miles. It 
 is composed of sand, gravel, and broken shells, and makes a good roadway, 
 as well as a productive soil. The shells in this terrace are of the same species 
 as now inhabit the adjacent waters. Besides these, bones of the whale and Bones of the 
 the morse have been found partially imbedded in this deposit, in several ^ hale and 
 places between Bic and Matanne. At Ste. Anne des Monts, five or six 
 terraces rise one above another to a height of about twenty-five feet above 
 the sea. All of them abound in fragments of shells, belonging to the 
 common littoral species. Shells ofNatica, Saxicava, and Balanus are found 
 in sand upon the Metis River, 245 feet above the sea. Near the mouth Metis. 
 
922 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 of this river is a terrace fifty feet in height ; and in a similar terrace, at 
 
 Matanne. the mouth of the Matanne River, a layer of shells is found at forty-four 
 feet, resting on blue clay, and overlaid by six feet of sand. Portions of 
 clay are also met with in some of the bays on the north coast of Gaspe*. 
 One of these, holding marine shells, forms a plateau of ninety feet in height 
 on the west side of the Magdalen River, stretching for two or three miles 
 along the coast, with a breadth of about a mile on the Magdalen. In 
 the interior, stratified clays occur at the head of Lake Matapedia, at a 
 height of 480 feet, and near the outlet of the 'same lake, at 530 feet 
 above the sea ; but in neither locality have they been observed to contain 
 fossils. No stratified clay has yet been observed on or near the eastern 
 coast of the peninsula of Gaspe* ; but a considerable area of it occurs on 
 
 ra.-'tapedia. the south side, at the mouth of the Great Cascapedia River. It extends 
 along the coast for three and a half miles to the east, and eleven miles to 
 the west. of the mouth of the river, and to a variable distance back. In 
 this clay, Mya and Saxicava are found in a great number of successive 
 beds to a height of seventeen feet over high-water mark, in the position 
 which the shells occupied when in life. Each bed is separated from the 
 one below it by a thin layer of sand, which also fills the cylindrical open- 
 ings through which the inhabitants of the shells once .communicated with 
 the surface. 
 
 Uaspg. In the Gaspe* peninsula thick beds of gravel and sand are spread over 
 
 the boulder formation in the valleys of the rivers and brooks, particularly in 
 their lower portions. On the Magdalen River, these have been observed up 
 to a height of about 1600 feet above the sea. Near the coast also, deposits 
 of gravel and sand are found around many of the bays and coves, and like 
 those on the rivers they are often worn into terraces. On the south side of 
 the Northwest Arm of Gaspe Bay, an ancient beach, 154 feet above the sea, 
 is marked by a sudden step along a hill-side, and traces of other beaches 
 are found at lower levels in the neighborhood. A terrace varying from 
 thirty-five to forty-three feet in height, begins on the north side of -the 
 
 Yoji; River. York River, six miles from its source, and continues regularly for about 
 three miles, cutting off the bends of the stream. Two miles and a half 
 west of the long sand beach in Mai-bay, well marked terraces occur not 
 far from the Malbay River, at the estimated elevations of eight, fifteen, 
 and fifty feet above the sea. Mya arenaria, M. truncata, Oardium 
 G-roenlandwum, and Tellina proximo, are found at about fifteeen feet 
 above high-water mark, in a deposit of sand, covering several hundred 
 acres, at Anse aux Gascons in Port Daniel Bay. 
 
 Murray Bay. On the northern side of the St. Lawrence, stratified clays occur in 
 the valleys of Murray Bay and Bay St. Paul. At Murray Bay the lower 
 clay, containing fossils, is seen exposed along the shore at low tide. Far- 
 ther up is a flat of sand and gravel, about thirty feet over the sea, con- 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY, 923 
 
 taining shells of Tellina. Above this is a well marked terrace 100 feet 
 high, which presents a steep bank of clay, and is surmounted by another 
 less distinct, at 182 feet. Beyond this the ground rises in a steep slope, 
 on which the highest observed shore-mark is a narrow beach of rounded 
 pebbles at 326 feet: this becomes a wide terrace farther to the north, 
 and on the opposite side of the bay. Clays are not however confined to 
 the lower levels, but occur regularly stratified throughout the terraces, 
 and in some places present sections of sixty and eighty feet in height. At 
 Bay St. Paul similar terraces were observed ; the heights of the two best Bay st. Paul, 
 marked of these were found to be approximately 130 and 360 feet 
 above high- water mark. Marine fossils occur throughout the strata 
 in which these terraces are worn, and still higher, at 390 feet above the 
 sea-level. The numerous land-slips, which are so common here, and else- 
 where throughout these clay deposits, seem to be due to the presence of 
 arenaceous beds near the base, which permit the percolation of water ; 
 while the unsupported nearly vertical cliffs allow movements to occur, 
 causing fissures, down which surface-waters flow, until, reaching the sandy 
 layer, they undermine the mass. The weight of this then causes the base Land-slips. 
 to slide outward, until at last a vertical section of the cliff lies nearly 
 horizontally in the valley below. In this, among other ways, the successive 
 terraces have doubtless been formed in the clays which once filled these 
 valleys. The lower levels, both at Bay St. Paul and Murray Bay, are 
 in many places strewn with masses of clay, detached by land-slips from the 
 heights around. These have been rounded, either by the subsequent 
 action of the receding waters, or by the weather, and now present hillocks 
 and conical mounds, often of singular regularity. 
 
 In the valley of the Saguenay, marine clays, generally overlaid by sand Saguenay. 
 and gravel, are found almost everywhere between Ha-ha Bay and the west 
 side of Lake St. John ; as well as between that bay and Chicoutimi, and on 
 both sides of the Saguenay River above and below the latter place. Be- 
 tween Chicoutimi and Ha-ha Bay, the clay is sometimes 600 feet in thick- 
 ness, and is subject to immense land-slips, by which areas of many acres 
 are sometimes removed from their original place. Between Lake Keno- 
 gami and Belle Riviere, the clay has a thickness of 100 feet ; and about 
 half a mile below the falls of the latter river, at a height of about 400 feet 
 above the sea, it contains the shells of Saxicava. The same species was 
 found on the Alphonse River, at a height of about 150 feet ; and it was 
 also found associated with several other marine species at a much lower 
 level, in a bed of sand near Chicoutimi church. 
 
 On the island of Anticosti bluish-grey clays occur on the Becscie and Anticosti. 
 Otter Rivers ; and clay cliffs from sixty to seventy feet high extend for 
 about five miles along the coast near the St. Mary's River. These clays 
 are frequently calcareous, and contain numerous pebbles of limestone. 
 
924 
 
 GEOLOGY OP CANADA. 
 
 [CHAP. XXII. 
 
 Labrador. 
 
 Mingan 
 Islands. 
 
 Flower-pot 
 rocks. 
 
 Upper 
 
 sands. 
 
 St. Maurice. 
 
 Ottawa. 
 
 Pakenham 
 mills. 
 
 On the coast of Labrador clays occur containing many species of marine 
 fossils, which have been collected by Captain Orlebar, R.N., and Mr. J. 
 S. Packard of Brunswick, Maine. They are found in Tertiary Bay, 
 and some other localities, in deposits but little above high-water mark. 
 
 On Large Island, one of the Mingans, there occurs a succession of 
 ancient beaches, which are composed of small limestone pebbles. Except 
 where covered by moss, but little difference is perceptible between these 
 and the beach at present washed by the sea. They form successive terraces 
 rising one above another from five to thirty feet, the highest attaining 
 about 100 feet above high-water mark. Another feature strongly marking 
 the change in the relative levels of sea and land is the presence on this 
 island of what from their shape have been termed flower-pot rocks. They 
 are composed of horizontal layers of limestone piled on one another, and 
 are the remains of stratified masses that were once united, but have been 
 gradually worn away by the destructive action of the sea. Many of these 
 standing out of the water at various heights, according to the state of the 
 tide, show the waves still at work on them, while some are seen high up 
 on the island, demonstrating a similar action when the land was from 
 fifty to sixty feet below its present level. 
 
 The sand which has been noticed as overlying the clays in most of their 
 localities, is in some parts of the country developed to such an extent as 
 to require a more special mention. This is particularly the case on the 
 north side of the St. Lawrence, where it forms a belt at the base of the 
 Laurentide hills, from the Ottawa to Cape Tourmente. This belt ex- 
 pands to a breadth of thirty miles on the St. Maurice River, where it 
 reaches to the St. Lawrence, and stretches several miles along the shore. 
 To the westward it covers much of the surface in the triangular area 
 between the St. Lawrence and the Ottawa, east of- the meridian of 
 Kingston. The whole of the higher lands in the townships of Edwards- 
 burgh, Augusta, and the south part of Oxford, are covered by a fine 
 yellow sand, which is frequently blown up into dunes. The same appears 
 to be the case with the sand between Ottawa and Prescott. These sands 
 cover the valleys of the South Petite Nation River, and are largely 
 developed in West Hawkesbury, Lochiel, Kenyon, Nepean, Fitzroy, 
 and Pakenham. Fossil shells, chiefly Saxicava rugosa and Tellina 
 Grrcenlandica, are found in many places in the sands of this district. 
 The highest observed locality of these shells is in Nepean, at 410 feet 
 above the sea. They are also found in Kenyon, at 335 feet ; in Fitzroy, 
 at 330 feet ; and in Winchester at 300 feet. A mixture of marine and fresh- 
 water shells occurs in a sandy clay near Pakenham mills, at a height of 
 266 feet. The bed, which is four and a half feet thick, is overlaid by ten 
 feet of clay, surmounted by ten feet of sand and surface soil. 
 
 These sands are also met with in that part of the province south of the 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY, 925 
 
 St. Lawrence, along the boundary of New York. From the east side of 
 Missisquoi Bay another belt of sand extends between the clay plains of 
 the south shore of the St. Lawrence, which it partially overlies, and the more 
 elevated region to the southeast, as far as Metis. A considerable develop- 
 ment of the sand is also seen on the west side of the Richelieu at Sorel, sorei. 
 and thence stretching southward. Near Clarence ville, shells of Tellina are 
 found associated with Limnea, and three species of Unio, in a sandy clay clarence- 
 ninety-eight feet above the level of the sea, and about ten feet above the Tllle ' 
 level of Lake Champlain, in what may have been the site of an ancient 
 estuary. At the Wallbridge mills, in Stanbridge, Saxicava and other marine 
 shells occur in sand at a height of about 160 feet. Near the Upton Upton, 
 station on the Grand Trunk railway, the shells of Saxicava, Tellina, said. 
 My a are found with comminuted fragments of Mytilm, occupying a cleft 
 in the limestone at a height of 300 feet above the sea-level ; the presence 
 of these littoral shells marking a former sea-beach. 
 
 A remarkable locality of fossil shells occurs near Beauport, about two Beauport. 
 and a half miles northeast of Quebec, and a quarter of a mile from the St. 
 Lawrence. The deposit is exposed on the side of a ravine 110 feet deep, 
 and the bank, whose summit is about 150 feet above the sea, consists of 
 stratified sand and gravel, resting upon the unstratified boulder forma- 
 tion, which, as usual, is without fossils. About twenty feet from the top is 
 a bed twelve feet in thickness, composed almost wholly of the shells of Saxi- 
 cava, Tellina, etc. Between this deposit of littoral shells and the boulder 
 clay, Dr. Dawson has observed a sandy layer of about three inches, filled 
 with deep-water shells, such as Fusus, Pecten, and RhyncJionella. In this 
 layer, as well as beneath it, resting upon, or partially imbedded in the 
 boulder clay, and adhering to stones, which are often smoothed or striated, as 
 if by glacial action, are found numerous species of Balanus, of Spirorbis, 
 and of several genera of bryozoa. This lower stratum of sand represents the 
 Leda clay of Montreal, and is rich in the fossils which are usually found at 
 the surface of that deposit. It will be observed however that the Leda, which 
 characterizes it in so many other localities, and which inhabited only a 
 clayey bottom, is here wanting. Foraminifera, which abound in the clays 
 of Montreal, are also comparatively rare in the lower sand of Beauport. 
 Shells of Saxicava and Tellina occur in horizontal beds of sand and clay, 
 about a quarter of a mile from the locality just described, and at a height 
 of 200 feet. They also occur in a bed of sand near the bridge above the 
 Falls of Montmorenci. Similar deposits, but without shells, have been 
 observed farther inland, several miles to the northwest, and at heights 
 between 300 and 400 feet above the sea. In this connection may be 
 mentioned an interesting deposit of very fine silicious sand, which occurs 
 at Laval, on the right bank of the Bras, just at its junction with the 
 Montmorenci River. Here, in a cliff which is about 150 feet in height 
 
926 
 
 GEOLOGY OF CANADA, 
 
 [CHAP. XXIL 
 
 Laval, above the river, beneath about fifty feet of yellowish sand mixed with 
 boulders of gneiss, is exposed a thickness of fifteen feet of the silicious 
 earth. It is of two colors, yellow and grey, which are somewhat irregu- 
 larly interstratified. The materials of the lower part of the escarpment are 
 concealed. This earth, from its fineness, has been used at Quebec as a 
 plate powder, and was supposed to be of infusorial origin. A microscopic 
 examination, however, shows it to be nothing more than a fine quartz 
 sand. The fossiliferous. sands occurring at the lower levels along the 
 borders of the lower St. Lawrence, contain an assemblage of fossils some- 
 what different from those of the higher levels, approaching more nearly to 
 the present fauna of the Gulf. These sands are no doubt more recent 
 than those of the higher levels. 
 
 The following is a list of the invertebrate animals which have been found 
 in a fossil state in the post-tertiary deposits of Eastern Canada ; without 
 however including the numerous species of foraminifera, many of them 
 new, which have been described by Dr. Dawson ( Canadian Naturalist, 
 vol. iv, page 26). In the left-hand column the number prefixed to certain 
 species denotes the page of this volume on which they will be found 
 figured ; and in tho right-hand columns, stars indicate eight of the more 
 important localities in which the fossils have been observed. Of these 
 numbered columns 1 is for Pakenham mills, and the next four are in the 
 vicinity of Montreal ; 2 being Logan's farm, 3 Coteau Baron, 4 the Mile- 
 end quarries, and 5 the grounds of McGill College. 6 is St. Nicholas, 
 7 Beauport, and 8 Tertiary Bay, Labrador. 
 
 LIST OF INVERTEBRATE FOSSIL ANIMALS IN THE POST-TERTIARY DEPOSITS. 
 
 Page 
 
 RADIATA. 
 
 1 
 
 2 
 
 3 
 
 4 
 
 5 
 
 G 
 
 7 
 
 8 
 
 
 PROTOZOA. . 
 
 
 .v. 
 
 
 
 
 
 
 
 
 ECHINODKRMATA. 
 
 
 
 
 
 
 
 -V- 
 
 
 
 
 
 
 
 
 
 
 .". 
 
 -X- 
 
 
 
 
 -'. 
 
 
 
 
 
 
 
 
 MOLLUSCA. 
 BRYOZOA. 
 
 
 
 
 
 
 
 -V- 
 
 -X- 
 
 
 
 
 
 
 
 
 
 ' 
 
 
 
 
 
 
 
 
 
 
 .-'- 
 
 
 
 
 
 
 
 
 
 
 .V. 
 
 
 
 
 
 
 
 
 
 
 ,v 
 
 -x- 
 
 
 
 
 .". 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
CHAP. XXII.] 
 
 SUPERFICIAL GEOLOGY. 
 
 927 
 
 POSTVTEKTIARY FOSSILS. Continued. 
 
 Page 1 2 1 3 4 5 6 7 8 
 
 BRACHIOPODA. 
 
 963 Rhynchonella (Hypothyris) psittacea, Gmelin -"- -* * 
 
 LAMELLIBRANCHIATA 
 963 Pecten Islandicus, Chemnitz 
 
 963 Leda truncata, Wood. (L. Portlandica.) * . . . . % 
 
 " pygmasa, Miinster. 1 
 
 " caudata, Donovan. (L. minuta, Fabricius.) 
 
 Crenella glandula, Totten. (C. decussata, Montague.) * 
 
 " nigra, Gray * * 
 
 963 Mytilus edulis, Linnaeus * * * * & * 
 
 Unio cardium, Rafinesque. 2 (U. ventricosus, Barnes.) 
 " rectus, Lamarck. 
 
 Sphasrium (Cyclas) ? 
 
 Cardium Islandicum, Linnasus 
 
 " (Serripes) Groenlandicum, Chemnitz * 
 
 963 Astarte Laurentiana, Lyell . . 1 . -x- * -x- -* * * 
 
 " elliptica, Brown 
 Mesodesma deaurata, Hanley. 3 (M. Jauresii, De Joannis.) 
 
 964 Tellina Groenlandica, Beck * -x- * * * * * 
 
 964 " proxima, Brown ' -x- . . -x- * -x- -& * 
 
 Macoma inflata * 
 
 963 Mya truncata, Linnaus -x- 
 
 963 " arenaria, Linnaeus -x- -x- -A -x- . . ;<- 
 
 964 Saxicava rugosa, Linnaaus -x- -x- . . -x- -x- -* 
 
 " arctica, Linn. (var. of S. rugosa) -x- * 
 
 " distorta, Say. (var. of S. rugosa) -x- 
 
 GASTEROPODA. 
 Opisthobranchiata. 
 
 Cylichna oryza, Totten. (C. cylindracea?) -v_ . . % %. 
 
 Bulla (Diaphana) debilis, Gould 
 
 Prosobranchiata. 
 
 Amicula vestita, Gray # 
 
 964 Acmoea (Lepeta) coeca, Miiller 
 
 Puncturella (Cemoria) Noachina, Linnajus * * 
 
 Margarita helicina, Fabricius -x- 
 
 Lacuna neritoidea, Gould 
 
 Littorina palliata, Say , x . 
 
 Rissoa- obsoleta ? Searles Wood . x . 
 
 Paludina decisa, Say -x- 
 
 Val vata tricarinata, Say % 
 
 Amnicola porata, Say _x- 
 
 964 Scalaria Groanlandica, Perry ^ 
 
 Turritella erosa, Couthouy .^ ^. 
 
 costulata, Mighels * 
 
 Aporrhais occidentalis, Beck _* 
 
 Aclis (Alvania) ascaris, Searles Wood -x- 
 
 Menestho albula, Miiller. .% 
 
928 
 
 GEOLOGY OF CANADA. 
 
 [CHAP. XXII. 
 
 POST-TERTIAY FO88IL8. Concluded. 
 
 Page 
 
 Prosobranchiata. Continued. 
 
 1 
 
 2 
 
 3 
 
 4 
 
 5 
 
 G 
 
 7 
 
 8 
 
 
 
 
 
 
 
 
 
 
 
 964 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 964 
 
 " " Groenlandica Miiller (N pusilla Say ) . 
 
 
 
 
 
 
 
 
 
 964 
 
 
 
 _-'. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 4;- 
 
 
 " " rufa, Gould 
 
 
 
 
 
 
 
 
 -V. 
 
 964 
 
 
 
 -;;- 
 
 -'- 
 
 
 
 }$ 
 
 ,'- 
 
 -X- 
 
 
 
 
 
 
 
 
 
 -"- 
 
 
 
 
 
 .-. 
 
 
 
 
 
 
 
 964 
 
 Fusus tornatus, Gould 
 
 
 * 
 
 
 
 -- 
 
 * 
 
 -*'- 
 
 -( 
 
 964 
 
 
 
 -'- 
 
 
 
 
 
 
 
 964 
 
 
 
 % 
 
 
 
 -- 
 
 -V- 
 
 -"- 
 
 X. 
 
 
 " arctica, Middendorff. 
 
 
 -' 
 
 
 
 
 
 
 
 
 Pulmonata. 
 
 ( 
 
 
 
 
 
 
 
 
 
 
 
 --'- 
 
 -"- 
 
 
 
 
 
 
 
 
 
 
 --- 
 
 
 
 
 
 
 
 " elodes, Say 
 
 .". 
 
 
 
 
 
 
 
 
 
 
 .-'- 
 
 
 
 
 
 
 
 
 
 
 .V. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 ARTICULATA. 
 ANNULATA. 
 
 
 
 
 
 
 
 
 
 
 
 
 -V. 
 
 
 -"- 
 
 
 
 
 .V. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 -v- 
 
 .Y. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 -'- 
 
 
 
 
 
 
 
 964 
 
 CIRRIPBDA. 
 
 
 
 
 
 
 -- 
 
 
 
 
 
 
 
 
 
 
 
 .-'. 
 
 
 
 " porcatus Da Costa 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 1 Leda pygmaa has only been observed at Green's Creek in Gloucester, where it is 
 found adhering to a sea-weed, and associated with Tellina Gr&nlandica, Saxicava rugosa, 
 and the fossil fishes already mentioned on page 916. . 
 
 * Unio cardium and U. rectus have been observed only in one locality, near Clarence- 
 yille, where they are associated with a Limncea, and with Tellina Groenlandica and Mya are- 
 naria, in a bed of sandy clay about ten feet above the level of Lake Champlain. 
 
 3 Mesodesma deaurata has been found at the mouth of the Matanne River, where it is 
 associated with Mytilus edulis, Tellina Grcenlandica, Mya arenaria, Saxicava rugosa, Natica 
 dausa, Balanu* Hameri, and B. crenatus ; and in the lower terraces along the coast. 
 
CHAP. XXII.] SUPERFICIAL GEOLOGY. 929 
 
 The superficial deposits of the higher portions of south-eastern Canada, Gold-bearing 
 embracing the Notre Dame Mountains, and the country to the southeast of 
 them, have been but partially examined. The unmodified drift, which 
 contains the gold of that region, is derived from the disintegration of the 
 rocks of the region, but contains a few boulders derived from the 
 Laurentide hills. It has however been in great part re-arranged by the 
 action of water ; and stratified deposits of clay sand and gravel are found 
 at various heights throughout the region, but they have hitherto been 
 very little studied. At the southern extremity of Lake Memphramagog, Lake Mem- 
 which, according to the Vermont surveyors, is only 685 feet above the sea, pl 
 a terrace of clay is met with at an elevation of ninety-three feet above the 
 lake, or 778 feet above the sea-level. This is the highest deposit of clay 
 which has been observed in Vermont ; but stratified sand and gravel are 
 found above it, arranged in successive terraces, to a height of 579 feet 
 over the la*ke, or 1264 feet above the sea ; and similar stratified deposits 
 form a regular terrace-like beach in Ripton on the Green Mountains 
 at a height of 2196 feet (Geology of Vermont, 1862). Ancient beaches Ancient 
 are described by Dr. Hitchcock as existing in the White Mountains, at b< 
 elevations of 2449 feet and 2665 feet above the sea. If, as is probable, 
 the superficial materials of this portion of the continent were re-arranged 
 and stratified during the slow elevation of the submerged land, it would 
 follow that the higher stratified deposits are of a greater antiquity than 
 the clays and sand of the St. Lawrence and Champlain valleys. In the 
 Gaspe* peninsula no foreign boulders have as yet been observed in the 
 boulder formation ; which there appears to be altogether composed of the Boulder 
 debris of the rocks of the country. It is exposed in the valleys of rivers formation - 
 and brooks, sometimes to a depth of a hundred feet. As in other regions 
 of the province, the boulders and pebbles are frequently grooved and 
 striated, and are thrown together in great confusion in a tough mixture of 
 sand and clay. 
 
 The boulder formation, or glacial drift, both in the British Islands and Ag e of the 
 North America, is by Lyell referred to the age of the newer pliocene, drift - 
 or most recent division of the tertiary series, of which it marks the close ; 
 while the stratified deposits which overlie it, and consist in part of the mate- 
 rials of the boulder formation re-arranged by the agency of water, are by 
 the same authority classed among post-tertiary strata. Although no ter- 
 tiary deposits older than the boulder formation -have yet been recognized 
 in Canada, they are met with in various parts of the United States. 
 
 At the western base of the Green Mountains, at Brandon in Vermont, 
 there is found beneath the unstratified boulder formation, and reposing 
 upon the older rocks, a deposit of tertiary strata, which are of great sci- 
 entific as well as economic interest. This locality is about 520 feet above 
 the sea, and presents beds of gravel and sand, with kaolin or porcelain 
 
 I* 
 
930 GEOLOGY OF CANADA. [CHAP. XXII. 
 
 Miocene of clay, yellow ochre, limonite or brown hematite, oxyd of manganese, and 
 )nt ' lignite or fossil wood. The latter is obtained in sufficient quantities to be 
 employed as fuel, and contains many fossil fruits, from the examination of 
 which Mr. Lesquereux is led to refer this deposit to the age of the mio- 
 cene, or the middle division of the tertiary period. The ores of iron and 
 manganese of this deposit, as well as the ochres and kaolin, are advanta- 
 geously wrought ; and are to be distinguished from the deposits of ores 
 and ochres which have been described as occurring in Canada, and which 
 belong to a more recent period. The oxyd of manganese, which belongs to 
 the species psilomelane and pyrolusite, is pure, and often crystalline ; and 
 the limonite is much less impure than that of the St. Lawrence valley. 
 Deposits of this ore, often with manganese., and with kaolin, are found in 
 many localities along the west side of the. Green Mountains, arid at various 
 levels up to more than 1000 feet. On the east side of these mountains, 
 similar deposits also occur in several places, as at Plymouth, where iron 
 and manganese ores, with clays, are met with upon a terrace 1168 feet 
 above the sea. These deposits, although regarded as similar to that of 
 Brandon, are probably of a different age. None of them have yet been 
 found along the extension of the Green Mountains into Canada ; but the 
 possibility of their occurrence in the Eastern Townships should be kept 
 in mind, inasmuch as both the ores and clays are of considerable economic 
 importance. 
 
 Kecent The deposits of bog manganese and of bog iron ores and ochres which 
 
 deposits. are f ounc [ m various parts of Canada, overlying the stratified clays and 
 sands, have already been described with considerable detail under their 
 respective heads in the twenty-first chapter. They are all of recent origin, 
 and, like the peat and fresh-water shell marl with which they are associated, 
 are still in many cases in the process of formation. The history of the peat 
 bogs and marl beds has also been given in the same chapter. Deposits of 
 silicious infusorial earth, which are frequent in Nova Scotia and in Vermont, 
 appear to be comparatively rare in Canada. The only locality of this kind 
 as yet known is in the valley of the Petewahweh River, about thirty-five 
 miles from its mouth ; where a fine white infusorial silica, which is made up 
 of the shields of the most common species of protophytes, is said to occur in 
 considerable quantities. 
 
APPENDIX: 
 
 COJFTAINI^G, 
 
 I. 
 
 A TABULAR VIEW OF THE ROCKS OF GREAT BRITAIN AND NORTH 
 AMERICA ; WITH NOTES ; 
 
 II. 
 
 A CATALOGUE OF THE LOWER SILURIAN FOSSILS OF CANADA; 
 
 III. 
 
 ADDITIONAL FIGURES OF PALAEOZOIC FOSSILS, AND FIGURES OF SOME 
 FROM THE RECENT DEPOSITS. 
 
932 
 
 GEOLOGY OF CANADA. 
 
 
 
 1 5 
 
 O S 03 
 kj iJ i-I 
 
 
 -5 S 
 
 52 3 -3 
 o* w '-5 S 
 
 
 
 * 
 
 
 8 
 
 ii 
 
 
 
 l! 
 
 02 P 
 
 g "3 
 
 I 5 ^ 
 
 O ai 
 
 SH > O 
 
 I 
 
 P4 
 
 
 I 
 
 
 . 
 
 H 7 
 
 o o 
 
 S 
 
 P.-S o 
 
 4> 3 73 
 
 2 
 
 - 60 g 
 
 HCIl" 
 
 a -a P * 
 
 s-s-s 
 
 PH a 
 
 11 I 
 ^O !?5 
 
 II 
 
 uogpnn 
 
 .is 
 - 
 
 OP* 
 
 I 
 
 O 
 
 CM 0> 
 
 I 
 
 iUw 
 
 l 
 
 ^ 
 
 
 * 
 
 . 8 
 
 a ^3 
 
 "2 o 
 
 53 fl . B 
 
 o go B'* 
 
 
 
 Q 
 
 'dnojS | 
 
 uospnn uojuiuj. oo Pi 
 
 111 
 
 o o o 
 
 g-a 73 
 
 5 B S 
 
 =33 
 
 O *, h 
 
 III 
 
 t> ^ 
 
 J3A 
 
 * !! 
 
 2 : s . 
 
 So -OT3 op 
 
 T K S ^ 
 
 I S3 
 
APPENDIX. 933 
 
 KOTES TO THB PRECEDING TABLE. 
 
 In this table are shown in parallel columns the various sub-divisions of the palaeozoic 
 formations which have been recognized in different parts of North America, with their 
 probable equivalents in Great Britain. It will be seen that in Canada a portion of the Up- 
 per Silurian series has been made a separate division, under the name of Middle Silurian. 
 The Oriskany formation is assumed to be the base of the Devonian system, in accord- Devonian. 
 *nce with the synchronism of De Verneuii ; but the fauna of the Gaspe limestones, at 
 present under examination, seems to indicate that it would be more proper to place 
 that limit farther down in the series. At Cape Gaspe", the upper eight hundred 
 feet of these limestones (p. 393) hold an intimate association of Lower Helderberg and 
 Devonian species, and the Psilophyton princeps of the sandstones (page 397) has been 
 found in the upper part of the limestones. There is no palaeontological break between 
 these limestones, and the Oriskany sandstone which overlies them, of sufficient impor- 
 tance to constitute a dividing line between two great systems. At this locality the 
 difference between the upper limestones and the Oriskany formation is not greater, 
 so far as regards the fossils by which they are characterized, than that between the 
 Trenton formation and the Hudson River group. But if, guided by these considera- 
 tions, we should place the upper limestones of Cape Gaspe" in the Devonian, then the Upper 
 whole of the Lower Helderberg, down to the Water limestone, would follow ; and the Silurian. 
 Upper Silurian would be represented, in Eastern Canada, only by the series of fossilif- 
 rous rocks on the Bay of Chaleurs, of which a descriptive section is given at page 
 443. These rocks contain a fauna, which is, upon the whole, distinct from that of the 
 Niagara and Guelph formations on the one hand, and from that of the Lower Helder- 
 berg on the other ; while at the same time it is more closely allied to the fauna of the 
 Ludlow group of England than any other yet discovered in the Silurian rocks of America. 
 It seems to occupy a position between the Niagara and the Lower Helderberg, but to be 
 more intimately connected with the former than with the latter. The Middle Silurian 
 of Canada, as limited in the above table, appears to represent very nearly the Wenlock 
 iimestone, and the Llandovery rocks of England. In both countries this part of the 
 series is strongly characterized by immense numbers of large Pentameri, with numerous 
 corals and crinoids. 
 
 The Lower Silurian rocks may be separated, on palaeontological grounds, into two Lower 
 divisions, an upper and a lower. The former includes all the formations from the base Silurian, 
 of the Birdseye and Black River to the top of the Hudson River group. The fossils of 
 this division constitute a single large but compact fauna, having its greatest development 
 in the Birdseye and Black River, and Trenton formations, and declining upwards to the Upper 
 top of the Hudson River formation. At certain horizons we find peculiar groups of division, 
 species which have a wide geographical distribution, but, so far as is at present known, 
 only a limited vertical range. Among these may be mentioned the peculiar corals and 
 cephalopods of the Black River, the several species of the genus Triarthrus in the Utica 
 formation, and the large orthides of the Hudson River. The most abundant and charac- 
 teristic species, however, range through the whole division. A very large proportion 
 of the Trenton species (excepting the crinoids and cystideans,) appeared suddenly in 
 the seas, in the region of western Canada, just at the commencement of the period of 
 the deposition of the lower strata of the Birdseye and Black River formation. 
 
 The lower division, consisting of the Chazy, Calciferous, and Potsdam formations, Lower 
 including the Quebec group, holds a large fauna, which is, upon the whole, specifically 
 distinct from that of the upper division. This fauna flourished most vigorously during 
 the period of the deposition of the Quebec group, and the upper part of the Calciferous 
 formation. About twenty of the Chazy species pass upward into the Black River and 
 Trenton formations, while the Chazy is connected with the Calciferous by the Quebec 
 group. Owing to the difficulty in collecting the fossils, our knowledge of this lower 
 fauna is evidently far from being complete. But we at least know this much, that it 
 
934 
 
 GEOLOGY OF CANADA. 
 
 British 
 equivalents 
 
 Western 
 Canada. 
 
 Eastern 
 Canada. 
 
 Taconic 
 system. 
 
 New York. 
 
 consists of a large number of peculiar genera and species, and that, viewed in a general 
 way, it is different from the great fauna of the upper division of the Lower Silurian 
 rocks. The upper fauna is considered to be the palseontological equivalent of that of the 
 Bala or Caradoc formation of Britain, while the lower represents that of the Llandeilo. 
 Nearly all of the species which are common to the Lower Silurian of England and Canada 
 occur only in the Bala in the former country, and only in the rocks lying above the 
 base of the Chazy in Canada. The great zones of cystideae are also found in the same 
 horizon in both countries. On the other hand the peculiar aspect of the trilobites, and 
 the great number of graptolites in the lower fauna of Canada, indicate a parallelism with 
 the Llandeilo. It is impossible to show the exact horizon of the line between the Bala 
 and Llandeilo, in Canada, but for the present it is assumed to be in the break between 
 the Chazy and Black River formations. On account of the abundance of cystideae in 
 the Chazy, it may however be hereafter found advisable to add this formation to the 
 Bala rocks, as suggested in CANADIAN ORGANIC REMAINS, Decade iii, page 12. 
 
 The succession of the North American rocks given in the columns of the table will 
 now be noticed. 
 
 II. WESTERN CANADA. This district includes all that portion of the province north 
 and west of the great dislocation, including the north side of the St. Lawrence to the 
 Gulf, and the Island of Anticosti. The succession and the nomenclature of its formations 
 as already given on page 20, differ but little from that of the New York rocks. The 
 Oneida or Shawangunk conglomerate, the Schoharie and Cauda-galli grits, and the 
 Genessee slates of New York, are however local formations, not yet recognized in West- 
 ern Canada. If, with Mr. Hall, the magnesian beds of the Water-lime, containing 
 Eurypterus, be regarded as subordinate to the Onondaga salt group, the Lower Hel- 
 derberg group will have no representative in the western division of Canada, if we 
 except the masses of fossiliferous limestone in the conglomerates of St. Helen's Island, 
 (page 356). This group is also absent from western New York. The highest palaeozoic 
 strata of southwestern Canada, which are the black shales of Bosanquet, include only 
 the base of the Portage group. The Guelph formation of western Canada is not known 
 in the state of New York. 
 
 III. EASTERN CANADA. By this designation is meant that portion of the province lying 
 to the south and east of the great break, whose course has been described in this volume 
 on pages 233 and 709. This region includes the greater part of Lower Canada south of 
 the St. Lawrence ; and the rocks of the strait of Belle Isle and of the adjacent parts of 
 Newfoundland belong to the same area. In this region, the Potsdam group, as already 
 shown (pages 283, 288 and 879), appears as a great accumulation of limestones, sand- 
 stones, and shales, several thousand feet in thickness. The Quebec group, consisting of 
 the Phillipsburgh, Lvis, and Sillery divisions, is another similar series of strata, not less 
 in amount. The Calciferous and Chazy formations are shown by their organic remains 
 to be representatives of portions of this great group ; and the Potsdam formation in 
 like manner represents a part of the Potsdam group. The Taconic system of Emmons, 
 which he supposed to be a distinct series of rocks more ancient than the Potsdam, 
 appears to consist, for the greater part at least, of the strata of the Potsdam and Que- 
 bec groups. The Upper Copper-bearing rocks of Lake Superior are regarded as occu- 
 pying the position of the Quebec group, to which they bear some resemblance in litho- 
 logical and mineralogical characters. They may perhaps include the Potsdam group. 
 The higher members of the Silurian and the Devonian rocks, so far as yet recognized in 
 this region, have been noticed on the preceding page, and are described in this volume 
 under the title of the Gaspe series. 
 
 IV. NEW YORK. The divisions of the rocks adopted by the geologists of this state, 
 and since recognized by Mr. Hall in his Palaeontology, are too well known to require 
 further notice. They have been made the basis of the nomenclature adopted for the 
 corresponding rocks of Canada. 
 
APPENDIX. 935 
 
 V. PENNSYLVANIA. The Roman numerals given under this head correspond to the Pennsylvania, 
 thirteen divisions adopted by Rogers in 1836, in his first Report on the geology of the 
 
 state. la the names in the adjoining column, which were subsequently given by him, 
 the palaeozoic period is supposed to represent a day, the divisions of which are named 
 from the sun's apparent course in the heavens. (Report on the Geology of Pennsyl- 
 vania, 1857, vol. I, p. 105). The base of the Primal series of Pennsylvania, according to 
 Rogers, consists of a conglomerate, more largely developed in Virginia and Tennessee, 
 and having in the first-mentioned state a thickness of 150 feet. This is followed by 1200 
 feet of brownish and greenish-grey shales, overlaid by 300 feet of sandstone with 
 Scolithus, and succeeded by 700 feet of shales, often talcose, which form the summit of 
 the Primal division. The Auroral division in Pennsylvania is said to consist chiefly 
 of magnesian limestones, which vary from 2500 feet to more than 5000 feet in thickness, 
 and are by Rogers supposed to correspond to the Calciferous, Chazy, and Black River 
 formations. These two divisions of Rogers may probably represent the Potsdam and 
 Quebec groups of Eastern Canada. 
 
 VI. TENNESSEE. The succession here given is taken from Safford's Report, published Tennessee, 
 in 1856. The lowef members of the series appear in the eastern part of the state, where 
 
 the group III consists of several thousand feet of sandstones and shales, including near 
 the top a white sandstone with Scolithus. The group IV in like manner consists of several 
 thousand feet of sandstones and shales, with limestones, often magnesian. These two 
 groups, which are regarded by Safford as equivalent to the Potsdam and Calciferous 
 formations, resemble the Potsdam and Quebec groups of Eastern Canada, and the Primal 
 and Auroral divisions of Pennsylvania. The groups I and II appear to be like the 
 altered strata of the Quebec group in eastern Canada, and are perhaps repetitions of 
 III and IV, in a disturbed and metamorphosed condition. The group V in Eastern 
 Tennessee includes in its upper part a large mass of sandy shales, and has a total thick- 
 ness of about 2000 feet, but thins out to the westward. The great accumulation of 
 sandstones, shales, and limestones, which make up the Potsdam and Quebec groups of 
 Eastern Canada, Pennsylvania, and Tennessee, is represented in the Mississippi valley 
 by a few hundred feet of sandstones and limestones. These constitute what has been Missouri, 
 called the Magnesian Limestone series of Missouri, which is divided into four parts by 
 three intervening sandstones. It has a total thickness of about 1300 feet, and is followed 
 by the Trenton and Hudson River groups, and by the Upper Silurian and Devonian series, 
 the whole represented by a few hundred feet of strata, chiefly calcareous. The Lower 
 Magnesian limestone, and the St. Peter's sandstone of Owen, which in Iowa underlie the 
 Trenton group, have a thickness of about 800 feet. Above the latter group is the 
 Galena or lead-bearing limestone of Iowa and Illinois. This constitutes the Upper Iowa. 
 Magnesian limestone of Owen, formerly known as the Cliff limestone of the west, which 
 however included the strata up to the base of the Devonian. The great mass of Upper 
 Devonian and Carboniferous sandstones and shales of Eastern Canada, New York, 
 and Pennsylvania, is represented in the Mississippi valley by a few hundred feet 
 of strata, chiefly calcareous. The whole Devonian series in Iowa and Illinois is only 
 about 200 feet iu thickness, and is directly succeeded by the Carboniferous limestones, 
 which are in their turn overlaid by the Coal measures. These limestones are by Hall 
 divided into the Burlington, Keokuk, and Warsaw limestones, the latter two being the 
 Archimedes limestone of Owen. To this succeed the St. Louis limestones, which in Iowa 
 support the Coal measures; while in Missouri about 200 feet of sandstone intervene, 
 followed in some parts by an overlying member, called the Kaskaskia or Upper Archi- 
 medes limestone. The total thickness of this Carboniferous limestone group in Iowa 
 is less than 400 feet, but it increases to more than 1200 feet in Missouri and Tennessee. 
 
936 GEOLOGY OF CANADA. 
 
 CATALOGUE OP LOWER SILURIAN FOSSILS. 
 
 The following catalogue contains a list of all the hitherto described species of Lower 
 Silurian fossils from Canadian localities, with the exception of the fossils from the 
 Quebec group. There are a few other species, mostly orthoceratites, yet to be deter- 
 mined. The study of the Middle Silurian, Upper Silurian, and Devonian fossils of 
 Canada, is not yet sufficiently advanced to render practicable the preparation of a cata- 
 logue of them approaching to completeness; and the same may be said of those of the 
 Quebec group. The described fossils from this group, however, are figured in the 
 eleventh chapter, and a list of these found at Point Le>is is given on page 862, with 
 the exception of the graptolitidse, of which a complete list is placed at the end of this 
 catalogue. 
 
 In the succeeding pages, the columns to the right hand side, indicate by asterisks the 
 vertical range of the species through the divisions of the Lower Silurian series ; and 
 in the last column will be seen what species pass upwards into 'the Middle Silurian 
 rocks. The abbreviations at the head of these columns have the following significations : 
 P. G., Potsdam group ; Cal., Calciferous formation; Ch., Chazy; B. B., Birdseye and Black 
 River ; Tr., Trenton ; Ut., Utica ; H. R., Hudson River formation ; and M. S., Middle Silurian 
 series. The abbreviations used in the list of authorities and references, are as follows 
 with their explanations : 
 
 AM. JOUR. Sci American Journal of Science and Arts (Silliman's Journal) ; 
 
 New Haven, Conn. 
 
 ANN. NAT. HIST Annals and Magazine of Natural History ; London. 
 
 ANN. REP. N. Y Annual Reports of the Geological Survey of New York. 
 
 BR. PAL. Foss British Palaeozoic Fossils, by Sedgwick and McCoy. 
 
 CAN. JODR Canadian Journal of Industry, Science, and Art; Toronto. 
 
 CAN. NAT. GEOL Canadian Naturalist and Geologist ; Montreal. 
 
 DEC Decades of the Geological Survey of Canada. 
 
 GEOL. REP. N. Y Final Reports of the Geological Survey of New York. 
 
 GEOL. TRANS Transactions of the Geological Society of London. 
 
 JOUR. A. N. S Journal of the Academy of Nat. Sciences of Philadelphia. 
 
 JOUR. GEOL. Soc Journal of the Geological Society of London. 
 
 MEM. GEOL. SUR Memoirs of the Geological Survey of Great Britain. 
 
 PAL. Foss Palaeozoic Fossils of Canada ; published by the Geological 
 
 Survey as " New Species of Lower Silurian Fossils." 
 
 PAL. N. Y Palaeontology of New York. James Hall. 
 
 POLYP. Foss Polypiers Fossiles. Edwards and Haime ; Paris. 
 
 PROC. A. N. S Proc. of the Academy of Nat. Sciences of Philadelphia. 
 
 PROG. AM. Assoc Proceedings of the American Association for the Advance- 
 ment of Science. 
 
 REG. REP Annual Reports, Regents of the University of New York. 
 
 REP Reports of the Geological Survey of Canada. 
 
 REP. BRIT. Assoc Reports, British Association for the Advancement of Science. 
 
 REP. GEOL. Wis Report on the Geology of Wisconsin. D. D. Owen. 
 
 SIL. FAUN. W. TENN Die Silurische Fauna des West. Tennessee. Dr. Ferd. Roemer. 
 
 SUP. MON. LIM Supplement to No. 1 of a Monograph of the Limniades, etc., 
 
 Haldeman, 1840. 
 
 URWELT Urwelr, Russlands. Eichwald. 
 
 ZOOL. JOUR Journal of the Zoological Society of London. 
 
APPENDIX. 
 
 93T 
 
 CATALOGUE OF THE LOWER SILURIAN FOSSILS OF CANADA, NOT INCLUDING THOSE 
 
 OF THE QUEBEC GROUP. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 6 
 P-' 
 
 i. 
 
 J= 
 
 
 CQ 
 23 
 
 L- 
 
 H 
 
 -j' 
 
 P 
 
 ft! 
 
 ft 
 
 72 
 
 ^ 
 
 
 PLANTS. 
 
 
 
 
 
 
 
 
 
 
 
 PAL.EOPHYCUS. 
 
 Hall, Pal. N. Y., i, 7, 1847. 
 
 
 
 
 
 
 
 
 
 
 P. irregularis. 
 
 " " " pi. 2, fig. 3. 
 
 . . 
 
 -X- 
 
 
 
 
 
 
 
 
 tubularis. 
 
 " " "figs. 1,2, 4, 5. 
 
 , . 
 
 -X- 
 
 
 
 
 
 
 
 
 Beauharnoisensis. 
 
 Billings, Pal. Foss., 98. 
 
 
 X- 
 
 
 
 
 
 
 
 
 Beverleyensis. 
 
 " " 97. 
 
 * 
 
 -X- 
 
 
 
 
 
 
 
 
 congregatus. 
 
 <( o 
 
 -X- 
 
 
 
 
 
 
 
 
 
 funiculus. 
 
 " " 98. 
 
 . . 
 
 -X- 
 
 
 
 
 
 
 
 
 incipiens. 
 
 " " 2. 
 
 -X- 
 
 
 
 
 
 
 
 
 
 obscurus. 
 
 " " 98. 
 
 
 
 
 
 -X* 
 
 
 
 
 
 BUTHOTREPHIS. 
 
 Hall, Pal. N. Y., i, 8, 1847. 
 
 
 
 
 
 
 
 
 
 
 B. gracilis. 
 
 " " " pi. 21, fig. 1. 
 
 
 
 
 
 -X- 
 
 
 
 
 
 
 
 
 
 LICROPHYCUS. 
 
 Billings, Pal. Foss., 99, June, 1862. 
 
 
 
 
 
 
 
 
 
 
 LFTiltnnpncia 
 
 ini 
 
 
 
 
 .. 
 
 */' 
 
 
 
 
 
 11 LI LUIIL Ilblo. 
 
 Hudsonicus 
 
 1U 1. 
 
 U 11 It 
 
 
 
 
 
 
 
 5C" 
 
 
 
 minor. 
 
 " " 100, fig. 88. 
 
 
 
 
 
 -X- 
 
 
 
 
 
 
 
 
 
 Ottawaensis. 
 
 " " 99, " 87. 
 
 
 
 
 
 -;:- 
 
 
 
 
 
 
 
 
 
 succulens. 
 
 Buthotrephis succulens, Hall, Pal. N.Y., 
 
 
 
 
 
 
 
 
 
 
 
 i pi. 22 fig. 2. 
 
 
 
 
 
 *X" 
 
 
 
 
 
 RDSOPHYCUS. 
 
 Hall, Pal. N. Y., ii, 83, 1853. 
 
 
 
 
 
 
 
 
 
 
 R. Grenvillensis. 
 
 Billings, Pal. Foss., 101. 
 
 
 
 .. 
 
 -X- 
 
 
 
 
 
 
 
 BEATRICEA. 
 
 Billings, Rep. 1857, 343. 
 
 
 
 
 
 
 
 
 
 
 B. nodulosa. 
 
 tt ' 344 
 
 
 
 
 
 
 
 X" 
 
 
 
 undulata. 
 
 if ft ft 
 
 
 
 
 
 
 
 *X" 
 
 ~fc 
 
 
 PROTOZOA. 
 
 
 
 
 
 
 
 
 
 
 
 RECEPTACTJLITBS. 
 
 Defrance, 1827. 
 
 
 
 
 
 
 
 
 
 
 R. occidentalis. 
 
 Salter, Dec. i, 45, = R. Neptuni, Hall, 
 
 
 
 
 
 
 
 
 
 
 
 Pal. N. Y., i, 68, pi. 24, fig. 3. 
 
 .. 
 
 
 .. 
 
 * 
 
 -x- 
 
 
 
 
 
 lowensis. 
 
 Owen, Rep. Geol. Wis., pi. 2, fig. 13. 
 
 
 
 
 
 -X- 
 
 
 
 
 
 
 
 
 
 calciferus. 
 
 Billings, Pal. Foss. 
 
 
 -X- 
 
 
 
 
 
 
 
 
 AMORPHOZOA. 
 
 
 
 
 
 
 
 
 
 
 
 EOSPONGIA, 
 
 Billings, Pal. Foss., 18, Nov. 1861. 
 
 
 
 
 
 
 
 
 
 
 E. Roemeri. 
 
 1Q 
 
 .. 
 
 
 ft 
 
 
 
 
 
 
 
 varians. 
 
 It (t (( ft 
 
 .. 
 
 
 -X- 
 
 
 
 
 
 
 
 ASTYLOSPONGIA. 
 
 Roemer, Sil. Faun. W. Tenn., 1860. 
 
 
 
 
 
 
 
 
 
 
 A. parvula. 
 
 Billings, Pal. Foss., 20. [1847. 
 
 
 
 ' 
 
 
 
 
 * 
 
 
 
 
 
 STROMATOPORA. 
 
 Goldfuss, 1830. Stromat ocerium, Hall, 
 
 
 
 
 
 
 
 
 
 140 
 
 S. rugosa. 
 
 Stromatocerium rugosum, Hall, 
 
 
 
 
 
 
 
 
 
 
 
 P.al. N.Y., i, pi. 12. 
 
 . 
 
 * 
 
 -X- 
 
 -X- 
 
 
 
 
 
 
 compacta. 
 
 Billings, Pal. Foss., 55. 
 
 . 
 
 
 * 
 
 -X- 
 
 
 
 
 
 
 Canadensis. 
 
 a 
 
 
 
 
 
 
 
 -K- 
 
 
 
 
 
 
 
 
938 
 
 GEOLOGY OF CANADA. 
 
 CATALOGUE OF LOWER SILURIAN FOSSILS. Continued. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 3k < 
 
 r, * 
 D C 
 
 
 Q ! 
 -' 
 
 H 
 
 s i 
 
 5 ( 
 
 ri 
 
 ^ 
 
 
 ARCHEOCYATHUS. 1 
 
 Billings, Pal. Foss., 3, Nov. 1861. 
 
 
 
 
 
 
 
 
 
 283 
 
 A. Atlanticus. 
 
 " " 4. 
 
 # 
 
 
 
 
 
 
 
 
 
 Minganensis. 
 
 Petraia Minganensis, Billings, Can. 
 
 
 
 
 
 
 
 
 
 
 ZOOPHYTA. 
 
 Nat. Geol., iv, 346. 
 
 * 
 
 :> 
 
 
 
 
 
 
 
 
 PROTAR^A. 
 
 Edwards & Haime, Polyp. Foss., 208. 
 
 
 
 
 
 
 
 
 
 
 ?. vetusta. 
 
 Porites vetusta, Hall, Pal. N. Y., 
 
 
 
 
 
 
 
 
 
 
 
 i, pi. 25, fig. 5. 
 
 
 
 
 . 
 
 ::- 
 
 
 
 
 
 HELIOLITES. 
 
 Dana. Zooph., 541, 1846. 
 
 
 
 
 
 
 
 
 
 
 3. megastoma. 
 
 McCoy, Br. Pal. Foss., pi. 1 C. fig 4 
 
 
 
 
 
 
 
 .;;. 
 
 * 
 
 
 FAVOSITES. 
 
 Goldfuss. 
 
 
 
 
 
 
 
 
 
 
 P. Gothlandica. 
 
 u 
 
 
 
 
 
 
 
 # 
 
 * 
 
 
 STENOPORA. 
 
 Goldfuss. 
 
 
 
 
 
 
 
 
 
 156 
 
 S. fibrosa. 
 
 it 
 
 
 . 
 
 y. 
 
 5t 
 
 ;;. 
 
 * 
 
 .;;. 
 
 * 
 
 156 
 
 petropolitana. 
 
 Pander. 
 
 , , 
 
 
 K- 
 
 K- 
 
 -:;. 
 
 -:;- 
 
 * 
 
 
 
 patula. 
 
 Billings, Can. Nat. Geol., iv, 427. 
 
 1 1 
 
 . 
 
 ;;- 
 
 
 
 
 
 
 
 adhasrens. 
 
 it a it it 
 
 
 
 -,:- 
 
 
 
 
 
 
 
 BOLBOPORITES. 
 
 Pander. 
 
 
 
 
 
 
 
 
 
 
 B. Americanus. 
 
 Billings, Can. Nat. Geol., iv, 429'. 
 
 . 
 
 
 -:,- 
 
 
 
 
 
 
 
 HALYSITES. 
 
 Fischer, 
 
 
 
 
 
 
 
 
 
 
 H. catenulatus. 
 
 Linnaeus. 
 
 . 
 
 . . 
 
 . 
 
 * 
 
 -;:- 
 
 
 * 
 
 * 
 
 
 TETRADIUM. 
 
 Dana. 
 
 
 
 
 
 
 
 
 
 139 
 
 T fibratum 
 
 Safford Am Jour Sci [21 xxii 237 
 
 
 
 
 -f 
 
 
 
 -V. 
 
 
 
 COLUMNARIA. 
 
 Goldfuss. 
 
 
 
 
 
 
 
 
 
 139 
 
 C. alveolata. 
 
 
 
 . . 
 
 .. 
 
 
 -::- 
 
 
 
 
 
 
 parva. 
 
 Billings, Can. Nat. Geol., iv, 428. 
 
 
 
 * 
 
 
 
 
 
 
 124 
 
 incerta. 
 
 it it tt it 
 
 .. 
 
 
 * 
 
 
 
 
 
 
 
 Goldfussi. 
 
 11 Rep. 1858, 166. 
 
 
 .. 
 
 
 
 .. 
 
 
 -X 
 
 
 
 Blainvilli. 
 
 tt tt tt tt 
 
 . . 
 
 
 
 
 
 . 
 
 -X 
 
 
 
 rio-ida 
 
 it n it 167. 
 
 
 
 
 
 
 
 -V 
 
 
 
 erratica. 
 
 it it tt it 
 
 t . 
 
 
 
 
 -;.: 
 
 
 
 
 
 PALJSOPHYLLUM. 
 
 Billings, 1858. 
 
 
 
 
 
 
 
 
 
 
 P. rugosum. 
 
 " Rep. 1858, 168. 
 
 
 
 
 
 
 
 
 * 
 
 
 
 
 
 FAVISTELLA. 2 
 
 Dana, Zooph., 538, 1846. 
 
 
 
 
 
 
 
 
 
 206 
 
 F. stellata. 
 
 Hall, Pal. N. Y., i, pi. 75, fig. 1. 
 
 .. 
 
 
 . 
 
 . 
 
 
 
 
 * 
 
 
 
 PETRAIA. 
 
 Lonsdale. Streptelasma or Strepto- 
 
 
 
 
 
 
 
 
 
 
 
 plasma. Hall. 
 
 
 
 
 
 
 
 
 
 
 P. profunda. 
 
 Hall. Streptoplasma profunda. Pal. 
 
 
 
 
 
 
 
 
 
 
 
 N. Y., i, pi. 12, fig. 4. 
 
 
 
 
 -;: 
 
 
 
 
 
 156 
 
 corniculum. 
 
 Hall . Streptelasma corniculum -f- crassa 
 
 
 
 
 
 
 
 
 
 
 
 -\-multilamellosa-\-parva. Pal. N.Y., i, 
 
 
 
 
 
 
 
 
 
 
 
 pi. 25, fig. 1-4. 
 
 . 
 
 
 . 
 
 -:: 
 
 -::- 
 
 
 
 
 
 aperta. 
 
 Billings, Pal. Foss., 102. 
 
 . 
 
 
 . 
 
 -;: 
 
 
 
 
 
 
 j 
 
 " Rep. 1858, 168. 
 
 
 
 
 
 
 
 X, 
 
 
 
 ZAPHRENTIS. 
 
 Rafinesque, 1820. 
 
 
 
 
 
 
 
 
 
 208 
 
 Z. Canadensis. 
 
 Billings, Pal. Foss., 105. 
 
 
 
 
 
 
 
 .... 
 
 
 
 
 
 
 
 
 
 
 
 
 
APPENDIX. 
 
 939 
 
 CATALOGUE OF LOWER SILURIAN FOSSILS. Continued. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND KEFERENCES. 
 
 O 
 
 ^ 
 
 r. 
 
 o 
 
 ' 
 
 o 
 
 - 
 
 30 
 
 ^ 
 
 5 
 
 j 
 
 ^ 
 
 n 
 
 2, 
 
 CRINOIDE^E. 
 BLASTOIDOCRINUS. 
 B. carcharieedens. 
 CARABOCRINUS. 
 C. radiatus. 
 tuberculatus. 
 Vancortlandtii. 
 CLEIOCRINUS. 
 C. regius. 
 grandis. 
 ihagnificus. 
 DENDROCRINUS. 
 D. acutidactylus. 
 conjugans. 
 cylindricus. 
 gregarius. 
 humilis. 
 Jewettii. 
 latibrachiatus. 
 proboscidiatus. 
 rusticus. 
 similis. 
 GLYPTOCRINUS. 
 G. lacunosus. 
 marginatus. 
 ornatus. 
 priscus. 
 quinquepartitus. 
 ramulosus. 
 
 HETEROCRINUS. 
 H. articulosus. 
 Canadensia. 
 inaequalis. 
 tenuis. 
 HYBOCRINUS. 
 H. conicus. 
 tumidus. 
 pristinus. 
 LECANOCRINUS. 
 L. elegans. 
 Isevis. 
 PACHYOCRINUS. 
 P. crassibasalis. 
 PAL^EOCRINUS. 
 P. angulatus. 
 
 Billings, 1859. 
 Dec. iv, 18. 
 Billings, 1857. 
 " Rep. 1857,276. Dec. iv, 31. 
 " Dec. iv, 33. 
 " " " 32. 
 
 Billings, 1857. 
 " Rep. 1857, 277. Dec. iv, 53. 
 
 " Dec. iv, 54. 
 <( a it il 
 
 Hall, 1852. 
 Billings, Rep. 1857, 266. Dec. iv, 37. 
 " " 268. " " 41. 
 a tt 44. 
 
 " " 265. " " 36. 
 " 270. " " 39. 
 <( n it tt it tt 43. 
 u tt tt it it it 39. 
 " " 267. " " 38. 
 " " " 270. " " 41. 
 " " " 267. " " 40. 
 Hall, 1847. 
 Billings, Rep. 1857, 261. Dec.iv, 61. 
 " " " 260.' " " 59. 
 
 (( it It It It It gO. 
 
 " " " 257. " " 56. 
 11 Dec. pi. 8, fig. 4. 
 Can. Nat. Geol., i, 54. 
 Rep. 1857, 258. Dec. iv, 57. 
 Hall, 1847. 
 
 Billings, Dec. iv, 51. 
 it tt tt 4g t 
 
 " " " 51. 
 " " " 50. Rep. 1857, 273. 
 Billings, 1857. 
 " Rep. 1857, 274. Dec. iv, 29. 
 " " " 275. " " 28. 
 " Dec. iv, 23. 
 Hall, 1856. 
 Billings, Rep. 1857, 278. Dec. iv, 47. 
 
 (C (( tt tt It It 
 
 Billings, 1859. 
 " Dec. iv, 22. 
 
 Billings, 1859. 
 " Dendrocrinus angulatus. Rep. 
 1857. 269. Dec. iv. 45. 
 
 
 
 
 
 * 
 
 
 -X- 
 
 
 -;;- 
 
 % 
 
 
 
 
 
 
 -;: 
 -::- 
 -;;- 
 
 * 
 * 
 
 -;:- 
 -:;- 
 -;:- 
 * 
 
 * 
 
 -:;- 
 -;;- 
 
 -;:- 
 * 
 
 -;;- 
 -;:- 
 -;:- 
 
 -;;- 
 -;;- 
 
 -;:- 
 
 -:;- 
 -;:- 
 
 -'- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 .<. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 -;;- 
 
 
 
 
 
 
 
 -;:- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 -::- 
 
 
 
 
 
 
 
 
 -. 
 
 >:- 
 
 
940 
 
 GEOLOGY OF CANADA. 
 
 CATALOGUE OF LOWER SILURIAN FOSSILS. Continued. 
 
 Page 
 
 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 6 
 
 Cu 
 
 c3 
 
 
 _c 
 
 
 cc 
 ' 
 
 C 
 
 a 
 
 f 
 
 
 
 W 
 
 QQ 
 
 S 
 
 PAL^EOCRINUS. Con. 
 P. pulchellus. 
 rhombiferus. 
 striatus. 
 
 POROCRINUS. 
 
 P. conicus. 
 
 RETEOCRINUS. 
 R. fimbriatus. 
 stellaris. 
 
 RHODOCRINUS. 
 R. asperatus. 
 pyriformis. 
 microbasalis. 
 
 SYRINGOCRINUS. 
 S. paradoxicus. 
 
 CYSTIDE^). 
 AMYGDALOCYSTITES. 
 A. florealis. 
 
 radiatus. 
 tenuistriatus. 
 
 ATELEOCYSTITES. 
 A. Huxleyi. 
 
 COMAROCYSTITES. 
 
 C. punctatus. 
 GLYPTOCYSTITES. 
 G. Forbesi. 
 gracilis. 
 Logani. 
 multiporus. 
 
 MALOCYSTITES. 
 M. Barrandei. 
 Murchisoni. 
 . PAL.EOCYSTITES. 
 P. Chapmani. 
 Dawsoni. 
 pulcher. 
 tcnuiradiatus. 
 
 Tlillmcrq T?pr Ifi^ 1 ? 2fiQ Dec iv 46 
 
 
 
 
 -X- 
 -X- 
 
 -X- 
 
 
 * 
 
 
 n n it n it n 45 
 
 
 
 
 
 ct u it it it tt 25. 
 
 Billings, 1857. 
 " Rep. 1857, 279. Dec. iv, 34. 
 Billings, 1859. 
 " Dec. iv, 65. 
 " " " 64. 
 Miller, 1821, = Thysanocrinus, Hall. 
 Billings, Dec. iv, 27. 
 " " " 61. 
 Thysanocrinus, (Rhodocrinus) microba- 
 salis. Billings, Rep. 1857, 264. 
 Dec. iv, 63. 
 Billings, 1859. 
 " Dec. iv, 65. 
 
 Billings, 1854. 
 11 Can. Jour. [1], ii, 270. Rep. 
 1857,289. Dec. iii, 63. 
 Billings, 1854._ Can. Jour. [1], ii, 271. 
 Rep. 1857, 289. Dec. iii, 65. 
 Billings, 1854. Can. Jour. [1], ii, 271. 
 Rep. 1857, 289. Dec. iv,64. 
 
 Billings, 1858. 
 " Dec. iii, 72. 
 Billings, 1854. 
 " Dec. iii. 61. 
 Billings, 1854. 
 " Rep. 1857, 283. Dec. iii, 59. 
 " " " 283. " " 59. 
 " " " 282. " " 57. 
 " Can. Jour. [1], ii, 215. Rep. 
 1857,281. Dec. iii, 54. 
 Billings, 1858. 
 " Dec. iv, 67. 
 " " " 66. 
 Billings, 1858. 
 Dec. iii, 71. 
 tt it it 1^0. 
 
 " Can. Nat. Geol., iv, 430. 
 jictinocrinus tenuiradiatus, Hall. Pal. 
 N. Y., i, -18, pi. 4, figs. 8, 9. Bil- 
 lings, Dec. iii, 69. 
 
 
 
 
 
 K 
 
 
 
 
 
 
 
 
 
 
 -X- 
 
 -X- 
 
 -X- 
 X- 
 
 -X- 
 -X- 
 -X- 
 -X- 
 -X- 
 
 -X- 
 -X- 
 
 -X- 
 
 
 .. 
 
 .. 
 
 -x- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 .. 
 
 
 -X- 
 
 
 
 
 
 
 
 
 
 
 -X- 
 
 
 
 * 
 
 -x- 
 
 -X- 
 
 -X- 
 -X- 
 
 
APPENDIX. 
 
 941 
 
 CATALOGUE OP LOWER SILURIAN FOSSILS continued. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 6 
 3-' 
 
 " 
 
 Q 
 
 . PQ 
 
 5;pq 
 
 
 
 } 
 
 P4 
 
 E5 
 
 m 
 
 -2, 
 * 
 
 158 
 158 
 158 
 
 PLECROCYSTITES. 
 P. Anticostiensis. 
 elegans. 
 filitextus. 
 
 exornatus. 
 robustus. 
 squamosus. 
 CYCLOCYSTOIDES. 
 C. Halli. 
 
 ASTERIAD^J. 
 PALASTERINA. 
 P. rugosa. 
 stellata. 
 PETRASTER. 
 P. rigidus. 
 
 STENASTER. 
 S. Salteri. 
 pulchellus. 
 
 T^NIASTER. 
 
 T. cylindricus. 
 spinosus. 
 EDRIOASTERID^). 
 
 AOELACRINITES. 
 
 A. Billingsii. 
 Dicksoni. 
 EDRIOASTBR. 
 
 E. Bigsbyi. 
 
 BRYOZOA. 
 PTILODICTYA. 
 P. acuta. 
 fenestrata. 
 labyrinthica. 
 recta. 
 
 COSCINIUM. 
 
 C. proavium. 
 INTRICARIA. 
 I. ? reticulata. 
 
 Billings, 1854. 
 " Rep. 1857, 288. Dec. iii, 52. 
 " " " 287. " " 51. 
 " Can. Jour. [1], ii, 252, Rep. 
 1857, 286. Dec. iii, 50. 
 Billings, Dec. iii, 52. 
 " " " 49. 
 it it 
 
 Billings and Salter, 1858. 
 " " Dec. iii, 86. 
 
 McCoy, 1851. 
 Billings, Rep. 1857, 291. Dec. iii, 77. 
 " " " 290. " " 76. 
 Billings, 1858. 
 Palasterina rigidus. Billings, Rep. 
 1857, 291. Dec. iii, 80. 
 Billings, 1858. 
 " Dec. iii, 78. 
 Pal&aster pulchella, Billings, Rep. 
 1857, 292. Dec. iii. 79. 
 Billings, 1858. 
 Palceocoma cylindrica, Billings. Rep. 
 1857, 292. Dec. iii, 81. 
 Billings, Dec. iii, 81. 
 
 Vanuxem. 
 Chapman, Can. Jour. [2], v, 358. 
 Billings, Dec. iii, 84. 
 Billings, 1858. Cyclaster, Billings, 1857, 
 not Cyclaster of Leymerie and 
 Cotteau. 
 Cyclaster Eigsbyi, Billings, Rep. 1857, 
 293. Dec. iii, 82. 
 
 Lonsdale, 1839, = Stictopora, Hall; 
 Hall, Pal. N. Y., i. pi. 26, fig. 3. 
 it 4 4^ 
 
 " " 12, " 8. 
 Escharopora recta, Hall, pi. 26, fig. 1, 
 
 Keyserling, 1846, =Clatkropora } Hall, 
 1852. 
 Eichwald, Urwelt., ii, pi. 1, fig. 5. 
 Defrance, 1826. 
 Hall, Pal. N.Y., pi. 26, fig. 8. 
 
 
 
 
 
 
 
 -X- 
 -X- 
 
 * 
 
 
 
 
 
 * 
 
 -;;- 
 
 * 
 
 * 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 -. 
 
 
 
 
 
 
 
 
 
 
 
 
 
 -A- 
 
 -;: 
 -;:- 
 * 
 
 * 
 
 -X- 
 
 -X- 
 
 * 
 
 * 
 
 -X- 
 
 * 
 * 
 
 * 
 
 -X- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 -X- 
 
 * 
 
 -X- 
 
 * 
 
 
 
 
 
 -X- 
 
 
 
 
 .. 
 
 
 
 -;<- 
 
 
 
 
 
942 
 
 GEOLOGY OP CANADA. 
 
 CATALOGUE OF LOWER SILURIAN FOSSILS. Continued. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 6 
 P^ 
 
 08 
 
 
 
 .=. 
 o 
 
 cz 
 
 L, 
 
 u 
 
 
 
 K 
 
 CQ 
 
 s 
 
 157 
 
 POLYPORA. 
 P. gracilis ? 
 
 ARTHROCLEMA. 
 A. pulchella. 
 
 McCoy, 1844. 
 Retepora incepta, and R. gracilis, Hall, 
 Pal. N. Y., i, pi. 4, fig. 1, 2. 
 Billings, 1862. 
 " Pal. Poss 54 
 
 
 
 - 
 
 -,( 
 
 
 
 
 
 
 
 GRAPTOLITHUS. 
 G. amplexicaule. 
 
 Linnaeus. 
 Hall, Pal NY i pi 26 fig 11 
 
 
 
 
 
 
 
 
 
 200 
 
 bicornis. 
 
 it u tt 173 it 2 
 
 
 
 
 
 
 
 ' 
 
 
 
 mucronatus. 
 
 tt tt u 170 tt i 
 
 
 
 
 
 
 
 
 
 200 
 
 ramosus. 
 
 3 
 
 
 
 
 
 
 
 -V- 
 
 
 200 
 
 pristis. 
 
 Hisinger. 
 
 
 
 
 
 
 ^ 
 
 
 
 102 
 
 BRACHIOPODA. 
 
 LlNGULA. 
 
 L. acuminata. 
 
 _ crassa 
 
 Bruguiere, 1789. 
 Conrad, Ann. Rep. N.Y., 1839, 64,= 
 L. antiqua^ Hall, pars. 
 Hall, Pal. N. Y., i, pi. 30, fig. 8. 
 
 ;;- 
 
 V 
 
 
 
 
 
 
 
 161 
 
 curta. 
 
 (( It 11 It (I Q 
 
 
 
 
 
 
 
 
 
 161 
 
 elongata. 
 
 it tt ti it 5 
 
 
 
 
 
 
 
 
 
 
 equalis. 
 
 tt ii tt tt 3 
 
 
 
 
 
 
 
 
 
 161 
 
 obtusa. 
 
 tt it it tt tt it 17 
 
 
 
 
 
 
 
 
 
 
 riciniformis. 
 
 tt it it it tt tt 2 
 
 
 
 
 
 
 
 
 
 161 
 
 quadrata. 
 
 Eichwald. 
 
 
 
 
 
 
 
 
 
 124 
 141 
 
 Belli. 
 Eva. 
 
 Billings, Can. Nat. Geol., iv, 431. 
 " " vi, 150. 
 
 
 
 
 
 * 
 
 
 
 
 
 
 124 
 124 
 113 
 161 
 
 Huronensis. 
 Lyelli. 
 Mantelli. 
 Briseis. 
 
 " " iv, 433. 
 " " " 348. 
 " " " 349. 
 " Pal. Foss., 48. 
 
 
 
 -; 
 
 -;;- 
 * 
 
 ::- 
 
 
 
 
 
 210 
 
 Canadensis. 
 
 " 114. 
 
 
 
 
 
 
 
 -V- 
 
 
 161 
 
 Cobourgensis. 
 
 " " 48. 
 
 
 
 
 
 
 
 
 
 
 Daphne 
 
 Lingula attenuata, Hall, not Sowerby. 
 
 
 
 
 
 
 
 
 
 
 Forbesi. 
 
 Billings, Pal. Foss., 115. 
 
 
 
 
 
 
 
 
 
 141 
 
 Kingstonensis. 
 
 " " 48. 
 
 
 
 
 -- 
 
 
 
 
 
 
 Parryi. 
 
 " " 20. 
 
 
 
 
 
 -". 
 
 
 
 
 
 Philomela. 
 
 " " 49. 
 
 
 
 
 
 jj 
 
 
 
 
 161 
 
 Progne. 
 
 " " 47. 
 
 
 
 
 
 -- 
 
 
 
 
 142 
 
 OBOLUS. 
 0. Canadensis. 
 
 Eichwald, 1829. 
 Billings, Rep. 1858, 189. 
 
 
 
 
 .-'- 
 
 
 
 
 
 284 
 284 
 
 142 
 
 Labradoricus. 
 OBOLELLA. 
 0. chromatica. 
 cingulata. 
 
 ElCHWALDIA. 
 
 E. subtrigonalis. 
 
 " Pal. Foss., 5. 
 Billings, 1861. 
 " Pal. Foss., 7. 
 a it tt g 
 
 Billings, 1858. 
 " Rep. 1858, 192. 
 
 vc 
 
 * 
 
 -;:- 
 
 
 
 - 
 
 
 
 
 
 
 Anticostiensis. 
 
 Pal. Foss. 
 
 
 
 
 
 
 
 ,v- 
 
 
 159 
 159 
 
 DlSCINA. 
 
 D. Circe. 
 Pelopea. 
 
 Lamarck, 1817. 
 Billings, Pal. Foss., 51. 
 " 52. 
 
 
 
 
 
 
 
 
 
 -:;- 
 
 X- 
 
 
 
 
APPENDIX. 
 
 943 
 
 CATALOGUE OF LOWER SILURIAN FOSSILS. Continued. 
 
 
 
 '^ . :d 
 
 | PH CQ 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 . P rfJ . 
 
 IH p aq E 
 
 s'pria 
 
 
 TREMATIS. 
 
 harpe. 
 
 
 
 159 
 
 '. Huronensis. 
 
 illings, Pal. Foss., 53. 
 
 
 * 
 
 159 
 
 Montrealensis. 
 
 " " 52. 
 
 
 : k 
 
 159 
 
 Ottawaensis. 
 
 " 53. 
 
 
 ->5- 
 
 
 cancellata. 
 
 G. B. Sowerby, Zool. Jour., ii, pi. 11, 
 
 
 
 
 
 fig. 6. 
 
 
 -X- 
 
 159 
 
 terminalis. 
 
 Emmons, Geol. Rep. N.Y., 395, fig. 4. 
 
 
 -k 
 
 159 
 
 filosa. 
 
 Orbicula filosa, Hall, Pal. N. Y., i, pi. 
 
 
 
 
 
 30, fig. 9. 
 
 
 
 * 
 
 
 LEPT^ENA. 
 
 )alraan, 1827. 
 
 
 
 163 
 
 j. Sericea. 
 
 Sowerby. 
 
 
 
 -X- >! -X- : !< 
 
 
 STROPHOMENA. 
 
 lafinesque. 
 
 
 
 163 
 
 S. alternata. 
 
 Conrad, Ann. Rep. N. Y., 1838, 115. 
 
 . . . -;< -x- 
 
 -X- -X- -55- * 
 
 
 Camerata. 
 
 " Jour. A. N. S., viii, 5, pi. 14. 
 
 
 
 -X- 
 
 
 Ceres. 
 
 Billings, Can. Nat. Geol., v, 54. 
 
 
 
 ....* 
 
 163 
 
 deltoidea. 
 
 Conrad, Ann. Rep. N. Y., 1838, 115. 
 
 
 
 -X- 
 
 
 recta. 3 
 
 " Proc. A. N. S., i, 332. 
 
 # 
 
 * 
 
 
 subtenta. 
 
 <( 
 
 
 . . . & 
 
 
 incrassata. 
 
 Hall, Pal. N. Y., i, pi. 4, 1. 
 
 .... -:< -x- 
 
 ?:- . . ->{ 
 
 164 
 
 filitexta. 
 
 " " " " 31, fig. 3. 
 
 -;:- 
 
 A . . * 
 
 
 planumbona. 
 
 It (( U <! A 
 
 
 
 % . . * 
 
 209 
 
 Hecuba. 
 
 Billings, Can. Nat. Geol., v. 60. 
 
 
 
 . . . . * 
 
 209 
 
 fluctuosa. 
 
 " " " 58. 
 
 
 
 . . . . % 
 
 209 
 
 nitens. 
 
 " " " 53. 
 
 
 
 . . . . -X- 
 
 164 
 
 Thalia, 
 
 u ic it 59 
 
 
 
 -X- 
 
 
 Arethusa. 
 
 " Pal. Foss., 132. [fig . 4> 
 
 
 
 .... -rS- 
 
 
 tenuistriata. 
 
 Sowerby, Hall, Pal. N. Y., i, pi. 31 A, 
 
 
 
 5l< 
 
 
 imbrex? 
 
 Pander. 
 
 . . . . . . . 
 
 . . . . * 
 
 311 
 
 pecten. 3 
 
 Linnaeus. 
 
 
 
 .... -X- * 
 
 
 ORTHIS. 
 
 Dalman, 1827. 
 
 
 
 
 0. deflecta. 
 
 Strophomena deflecta, Conrad. Proc. 
 
 
 
 
 
 A. N. S., i, 332. Leptana deflecta, 
 
 
 
 
 
 Hall, Pal. N. Y., i, 113. pi. 31, B. fig. 
 
 
 
 
 
 5, O. deflecta, Safford. Am. Jour. 
 
 
 
 
 
 Sci. [2], xii, 355. 
 
 -::- 
 
 -X- 
 
 130 
 
 disparalis. 
 
 Conrad, Proc. A. N. S., i, 333. 
 
 .... 45- -X- 
 
 
 130 
 
 perveta. 
 
 u a 
 
 .... * * 
 
 
 
 subaequata. 
 
 (( a 
 
 . . . . * -X- 
 
 -X- 
 
 167 
 
 tricenaria. 
 
 
 
 .... % X 
 
 -X- -X- * 
 
 165 
 
 pectinella. 
 
 " Ann. Rep N. Y. 1840, 201. 
 
 -X* 
 
 * 
 
 167 
 
 lynx. 
 
 Eichwald. 
 
 
 
 -X- * * * 
 
 165 
 
 testudinaria. 
 
 Dalman. 
 
 % 
 
 -X- -X- -X- * 
 
 167 
 
 insculpta. 
 
 Hall, Pal. N. Y., i, pi. 32, fig. 12. 
 
 -X- 
 
 * -X- 
 
 91 A 
 
 occidentalis. 
 
 " " " " 32 A fie- 2 
 
 
 
 A\.\) 
 
 165 
 
 plicatella. 
 
 O J\ j Alg . t* 
 
 " " " 32, fig. 9. - 
 
 
 
 -x- ;<- 
 
 165 
 
 subquadrata. 
 
 " " " " 32 A, fig. 1. 
 
 
 
 x- * * 
 
 010 
 
 porcata. 
 
 McCoy, Br Pal Foss., pl.l H, fio-,41,42 
 
 
 4^. .. ^ ^ 
 
 OH 
 
 retrosa. 
 
 9 
 
 Salter, Mem. Geol. Sur., ii, pi. 27, figs. 
 
 
 
 
 
 3,4. 
 
 
 
 % * 
 
 
 gibbosa. 
 
 Billings, Rep. 1857, 296. 
 
 -;t 
 
 -X- 
 
944 
 
 GEOLOGY OP CANADA, 
 
 CATALOGUE OP LOWER SILURIAN FOSSILS Continued. , 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 O 
 
 3n' 
 
 "5 
 
 
 
 g 
 
 cq 
 
 
 ^ 
 
 ^ 
 
 X 
 
 i 
 
 OQ 
 
 s 
 
 
 Oaf HIS.- Con, 
 
 
 
 
 
 
 
 
 
 
 130 
 
 0. acuminata. 
 
 Billings, Can. Nat. Geol., iv, 440. 
 
 
 
 41 
 
 
 
 
 
 
 129 
 
 borealis. 
 
 " " " 436. 
 
 . . 
 
 , 
 
 It 
 
 
 ft 
 
 
 
 
 129 
 
 imperator. 
 
 " " " 435. 
 
 . 
 
 , 
 
 ft 
 
 
 
 
 
 
 
 piger. 
 
 c it a 442. 
 
 
 , 
 
 41 
 
 
 
 
 
 
 129 
 
 platys. 
 
 " " " 438. 
 
 
 
 -X- 
 
 
 
 
 
 
 
 Porcia. 
 
 " " " 439, 
 
 . . 
 
 . . 
 
 "- 
 
 
 
 
 
 
 
 ORTHISINA. 
 
 D'Orbigny, 1849. 
 
 
 
 
 -/;- 
 
 ft 
 
 
 
 
 * 
 
 
 O. Verneuili. 
 
 Eichwald. 
 
 
 
 
 
 
 
 
 
 113 
 
 grandseva. 
 
 Billings, Can. Nat. Geol., iv, 349. 
 
 
 -;<- 
 
 
 
 
 
 
 
 284 
 
 festiaata. 
 
 " Pal. Foss., 9. 
 
 ft 
 
 
 
 
 
 
 
 
 
 PORAMBONITES. 
 
 Pander, 1830. 
 
 
 
 
 
 
 
 
 
 
 P. Ottawaensis. 
 
 Billings, Pal. Foss., 140. 
 
 
 
 
 
 
 
 
 
 
 RHYNCHONELLA, 
 
 Fischer, 1809. Mrypa, pars, Pal. N. Y 
 
 
 
 
 vv 
 
 
 
 
 
 211 
 
 R. capax. 
 
 Jltrypa capax, Conrad, Jour. A.N.S. 
 
 
 
 
 
 
 
 
 
 
 
 viii, 264., pi. 14, fig. 21. Atrypa. in- 
 
 
 
 
 
 
 
 
 
 
 
 crebescens, pars. 
 
 
 
 
 
 
 
 
 
 211 
 
 modesta. 
 
 Say, dtrypa modesta, Hall, Pal. N. Y., 
 
 
 
 
 
 
 
 '/\ 
 
 
 
 
 i, pi. 33, fig. 15. 
 
 
 
 
 
 
 
 /(' 
 
 
 168 
 
 increbescens. 
 
 Hall, pars. Pal. N. Y., pi. 33. 
 
 .. 
 
 .. 
 
 .. 
 
 # 
 
 ft 
 
 
 
 
 168 
 
 recurvirostra. 
 
 " " " " fig. 5. 
 
 
 
 
 X- 
 
 '& 
 
 "X* 
 
 - 
 
 
 126 
 
 plena. 
 
 l( (( U A 11 7 
 
 4, <. 
 
 .. 
 
 
 4> 
 
 
 
 
 TT 
 
 
 211 
 
 Anticostiensis. 
 
 Billings, Pal. Foss., 142. 
 
 
 
 
 
 
 
 'X" 
 
 
 126 
 
 orientalis. 
 
 " Can. Nat. Geol., iv, 443. 
 
 . . 
 
 , . 
 
 -X- 
 
 
 
 
 
 
 
 GAMERELLA. 
 
 Billings, August, 1859. Triplesia, 
 
 
 
 
 
 
 
 
 
 
 
 Hall, October, 1859. 
 
 
 
 
 
 
 
 
 
 231 
 
 C. calcifera. 
 
 Billings, Can. Nat. Geol., vi, 318. 
 
 . . 
 
 -A* 
 
 
 
 
 
 
 
 127 
 
 longirostra. 
 
 " " iv, 302. 
 
 . , 
 
 . . 
 
 
 
 
 
 
 
 
 143 
 
 Panderi. 
 
 (( l( (( (C 
 
 . , 
 
 . . 
 
 . . 
 
 * 
 
 
 
 
 
 127 
 
 varians. 
 
 ti u u 445. 
 
 . 
 
 .. 
 
 -X- 
 
 
 
 
 
 
 143 
 
 Volborthi. 
 
 11 " 301. [H all. 
 
 
 
 
 ft 
 
 
 
 
 
 
 extans. 
 
 Jttrpyaextans,Gonra.<l. Triplesia extans, 
 
 
 
 
 
 ft 
 
 
 
 
 
 nucleus. 
 
 Atrypa nucleus, Hall, Pal. N. Y., i, 
 
 
 
 
 
 
 
 
 
 
 
 pi. 33, fig. 2. [i. p l. 33, fig. 10. 
 
 . 
 
 
 . . 
 
 , 
 
 ft 
 
 
 
 
 168 
 
 hemiplicata. 
 
 Atrypa hemiplicata, Hall, Pal. N. Y., 
 
 . 
 
 , 
 
 
 . 
 
 ft 
 
 
 
 
 
 antiquata. 
 
 Billings, Pal. Foss., 10. 
 
 * 
 
 
 
 
 
 
 
 
 
 ATHYRIS. 
 
 McCoy, 1844. 
 
 
 
 
 
 
 
 
 
 212 
 
 A. Headi. 
 
 Billings, Pal. Foss., 147. 
 
 
 
 
 
 
 
 X- 
 
 
 212 
 
 borealis. 
 
 Variety from Lake St. John. 
 
 
 
 
 
 
 
 -X" 
 
 
 212 
 
 Anticostiensis. 
 
 " from Anticosti. 
 
 . 
 
 
 . 
 
 
 
 
 
 ft 
 
 
 
 LAMELLIBRANCHI- 
 
 
 
 
 
 
 
 
 
 
 
 ATA. 
 
 
 
 
 
 
 
 
 
 
 
 AVICULA. 
 
 Klein, 1753. 
 
 
 
 
 
 
 
 
 
 215 
 
 A. demissa. 
 
 Conrad, Jour. A.N.S.,viii, pl.13, fig. 3. 
 
 . 
 
 . 
 
 . 
 
 , 
 
 . 
 
 .. 
 
 ft 
 
 
 170 
 
 elliptica. 
 
 Hall, Pal. N. Y., i, pl. 36, fig. 3. 
 
 . 
 
 , 
 
 . 
 
 . 
 
 X- 
 
 
 
 
 170 
 
 Hermione. 
 
 Billings, Pal. Foss., 40. 
 
 . 
 
 . 
 
 . 
 
 . 
 
 ft 
 
 
 
 
 
 Trentonensis. 
 
 Conrad, Jour.A.N.S., viii, pl.12.fig.10. 
 
 . 
 
 . 
 
 . 
 
 
 
 X- 
 
 
 
 
APPENDIX. 
 
 945 
 
 CATALOGUE OF LOWEE SII^UKIAN FOSSILS. Omtinued. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 d 
 
 S- 
 
 "5 
 D 
 
 .d 
 
 o 
 
 2:' 
 
 23 
 
 J 
 
 JH 
 
 i 
 
 d 
 
 S 
 
 
 
 * 
 
 * 
 
 X- 
 
 * 
 
 -X- 
 
 -X- 
 
 -X- 
 
 * 
 
 5Q 
 
 ^ 
 
 215 
 
 131 
 
 147 
 
 148 
 147 
 147 
 148 
 
 148 
 
 151 
 
 175 
 176 
 175 
 176 
 175 
 175 
 
 143 
 216 
 
 175 
 213 
 
 172 
 143 
 
 AMBONYCHIA. 
 A. amygdalina. 
 orbicuiaris. 
 radiata. 
 undata. 
 
 VANUXEMIA. 
 V. inconstans. 
 - Bayfieldii. 
 Moatrealensis. 
 CYRTODONTA. 
 C. obtusa. 
 
 subangulata. 
 
 subtruncata. 
 Canadensis. 
 cordiformis. 
 Huronensis. 
 rugosa. 
 spinifera. 
 - subcarinata. 
 sigmoidea. 
 breviuscula, 
 Emma. 
 Harrietta. 
 Hindi. 
 Leucothea. 
 poaderosa. 
 CTENODONTA, 
 0. dubia. 
 gibbosa. 
 levata. 
 nasuta. 
 astartaeformis. 
 - contracta. 
 gibberula. 
 Logani. 
 abrupta. 
 Iphigenia. 
 
 MODIOLOPSIS. 
 11. carinata. 
 faba. 
 modiolaris. 
 mytiloides. 
 subspatulata. 
 Gesneri. 
 Maia. 
 
 Hall, 1847. 
 
 Hall, Pal. N. Y. 7 i, pL 36, fig. 6. 
 
 it u u it u it 5 
 
 It 11 11 U gQ It 4. 
 
 it tt u tt 36> u tj m 
 
 Billings, 1858. 
 " Can, Geol. Nat., in, 433. 
 tt it 439 
 
 " " iv, 444. 
 Billings, 1858. 
 dmbonychia obtusa, Hall, Pal. N.Y., i, 
 pi. 36, fig. 8. 
 Edmondia subangulata, Hall,Pal.N.Y., 
 i, pi. 35, fig. 2. 
 E. subtruncata, Hall, pi. 35, fig. 3. 
 
 Billings, Can. Nat. Geol., iii, 434. 
 u u tt 437. 
 
 " " 432. 
 " " " 432. 
 " " " 435. 
 " " " 433. 
 " " " 438. 
 " " iv, 446. 
 " Pal. Foss., 150. 
 " " 149. 
 " " 151. 
 " " 46. 
 " " 150. 
 Sailer, 1851. Tellinomya, Hall. 
 Hall, Pal. N. Y., i, pi. 34, fig. 6. 
 
 U tt It It It U K 
 it It It It 11 tt I 
 
 tt it tt it it it 3 
 
 Salter, Dec., i, pi. 8, fig. 7. 
 a it it it it it 45 
 
 U It tl tl tt It Q 
 
 tt it n it it tt 3^ 
 
 Billings, Pal. Foss., 46. 
 " 152. 
 Hall, 1847. 
 " Pal. N. Y., i, pi. 35, fig. 11. 
 
 
 
 
 -X- 
 
 "r 
 * 
 * 
 
 w 
 
 * 
 
 
 
 
 
 ..- 
 
 * 
 
 
 
 * * 
 
 " * 
 
 * 
 
 v- 
 
 # 
 
 -X- 
 * 
 * 
 * 
 v- 
 * 
 - 
 * 
 
 * 
 
 * 
 * 
 * 
 * 
 * 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 ;:- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 X 
 
 
 
 
 
 
 
 
 
 
 * 
 * 
 * 
 * 
 * 
 * 
 * 
 * 
 
 ft 
 
 ;:- 
 * 
 * 
 
 * 
 * 
 * 
 * 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 # 
 
 * 
 
 - 
 
 Conrad, " " " " " 6. 
 it it u tt 81j 82. 
 
 Hall, " 35, fig. 4. 
 
 (1 (( ti It it g 
 
 Billings, Pal. Foss., 35, 43. 
 " 44. 
 
 
 
 
 * 
 
 
 
 
 
 
 
 -;:- 
 
 *' 
 
 %:- 
 
 * 
 * 
 
 41- 
 
 
 
 
 
 
 
 
 
 
 
 
 
946 
 
 GEOLOGY OF CANADA. 
 
 CATALOGUE OF LOWER SILURIAN FOSSILS. Continued. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 6 
 
 In' 
 
 i 
 
 ^ 
 
 J3 
 
 
 zi 
 
 S3 
 
 H 
 
 S 
 
 d 
 
 n 
 
 3 
 
 
 MODIOLOPSIS. Con. 
 
 
 
 
 
 
 
 
 
 
 173 
 
 tf. Meyeri. 
 
 Billings, Pal. Foss., 42. 
 
 
 
 
 
 
 
 ;:- 
 
 
 
 
 
 
 143 
 
 Nais. 
 
 " " 45. 
 
 
 
 
 
 
 ::- 
 
 
 
 
 
 
 Adrastia. 
 
 " " 45. 
 
 
 
 
 
 
 
 ;:- 
 
 -,'f 
 
 
 
 
 
 parviuscula. 
 
 " Can. Nat. Geol., iv, 446. 
 
 
 
 
 
 * 
 
 
 
 
 
 
 
 MATHERIA. 
 
 Billings, 1858. 
 
 
 
 
 
 
 
 
 
 147 
 
 H. tener. , 
 
 " Can. Nat. Geol., iii, 440. 
 
 
 
 
 
 
 
 
 
 -;:- 
 
 
 
 
 
 ORTHONOTA. 
 
 Conrad, 1841. 
 
 
 
 
 
 
 
 
 
 
 0. pholadis. 
 
 " Ann. Rep. N. Y. 1838, 118. 
 
 
 
 
 
 
 
 . 
 
 
 
 
 -;:- 
 
 
 
 A n 4-Q 
 
 Hall Pal NY i pi 82 fig 8 
 
 
 
 
 
 
 
 -;:- 
 
 
 216 
 
 1 COH trctC LI 
 
 parallela. 
 
 tt u it it n Y 
 
 
 
 
 
 
 
 -;;- 
 
 
 
 
 
 
 
 
 
 LYRODESMA. 
 
 Conrad, 1841. 
 
 
 
 
 
 
 
 
 
 176 
 
 L. postriata. 
 
 Emmons, Geol. Rep. N. Y., 399. 
 
 
 
 
 
 
 
 -;c- 
 
 -;:- 
 
 -;:- 
 
 -::- 
 
 
 
 CLEIDOPHORUS. 
 
 Hall, 1847. 
 
 
 
 
 
 
 
 
 
 
 ^GVGr&l sin fill SDGcics. 
 
 
 
 
 
 
 
 
 .;;- 
 
 
 
 CONOCARDIUM. 
 
 Bronn, 1835. 
 
 
 
 
 
 
 
 
 
 113 
 
 C. Blumenbachium. 
 
 Billings, Can. Nat. Geol., ir, 350. 
 
 .. 
 
 -::- 
 
 
 
 
 
 
 
 143 
 
 imraaturum. 
 
 " Pal. Foss., 41. 
 
 
 
 
 
 
 
 -;;- 
 
 
 
 
 
 
 GASTEROPODA. 
 
 
 
 
 
 
 
 
 
 
 
 HOLOPEA. 
 
 Hall, 1847. 
 
 
 
 
 
 
 
 
 
 
 H. dilucula. 
 
 " Pal. N. Y., i, pi. 3, fig. 7. 
 
 
 
 * 
 
 
 
 
 
 
 
 
 obliqua. 
 
 " " " " 37, fig. 2. 
 
 
 
 
 
 * 
 
 
 
 
 
 
 
 
 
 paludiuiformis. 
 
 it it n u it u 3 
 
 
 
 
 
 
 * 
 
 
 
 
 
 
 
 
 symmetrica. 
 
 It U It 11 11 It j_ 
 
 .. 
 
 
 .. 
 
 # 
 
 
 
 
 
 
 turgida. 
 
 " " " 3, " 9, 10. 
 
 .. 
 
 -X- 
 
 
 
 
 
 
 
 
 Lavinia. 
 
 Billings, Pal. Foss., 28. 
 
 . 
 
 .. 
 
 .. 
 
 .. 
 
 -;- 
 
 
 
 
 
 Nereis. 
 
 " " 27. 
 
 . 
 
 
 
 # 
 
 -::- 
 
 
 
 
 
 Proserpina. 
 
 " " 28. 
 
 . 
 
 .. 
 
 -;:- 
 
 
 
 
 
 
 145 
 
 Pyrene. 
 
 " " 27. 
 
 
 
 .. 
 
 .. 
 
 -;c- 
 
 
 
 
 
 
 ovalis. 
 
 " Can. Nat. Geol., iv, 351. 
 
 
 -;:- 
 
 
 
 
 
 
 
 
 CYCLONEMA. 3 
 
 Hall, 1852. 
 
 
 
 
 
 
 
 
 
 217 
 
 C. bilix. 
 
 Pleurotomaria bilix, Conrad. Jour 
 
 . 
 
 .. 
 
 . 
 
 .. 
 
 -::- 
 
 .. 
 
 # 
 
 
 
 
 A. N. S., viii, pi. 16, fig. 10. 
 
 . 
 
 
 
 .. 
 
 -;;- 
 
 
 
 
 178 
 
 Hageri. 
 
 Billings, Pal. Foss., 29. 
 
 . 
 
 .. 
 
 .. 
 
 .. 
 
 -;;- 
 
 
 
 
 178 
 
 Montrealensis. 
 
 " " 30. 
 
 . 
 
 .. 
 
 . 
 
 # 
 
 # 
 
 
 
 
 178 
 
 Halliana. 
 
 Salter, Dec., i, pi. 6, fig. 1. 
 
 . 
 
 .. 
 
 . 
 
 -x- 
 
 
 
 
 
 
 semicarinata. 
 
 tt it tt tt tt tt o 
 
 
 
 
 
 
 
 
 
 
 SUBULITES. 
 
 Conrad. (Hall, 1847.) 
 
 
 
 
 
 
 
 
 
 120 
 
 S. calcifera. 
 
 Billings, Can. Nat. Geol., iv, 360. 
 
 . 
 
 * 
 
 
 
 
 
 
 
 183 
 
 elongatus. * 
 
 Conrad, M. S., Emmons. Geol. Rep 
 
 
 
 
 
 
 
 
 
 
 
 N. Y. 392, fig. 3. Hall, Pal. N. Y. 
 
 
 
 
 
 
 
 
 
 
 
 i, pi. 39, fig. 5. 
 
 . 
 
 
 .. 
 
 -::- 
 
 -;:- 
 
 
 
 
 
 parvulus. 
 
 Billings, Pal. Foss., 36. 
 
 . 
 
 
 
 .. 
 
 -;;- 
 
 
 
 
 
 Richardsoni. 
 
 " Rep. 1857, 306. 
 
 . 
 
 
 .. 
 
 
 
 . 
 
 X- 
 
 
 
 subfusiformis. 
 
 Murchisonia subfusiformis, Hall, 
 
 
 
 
 
 
 
 
 
 
 
 Pal. N. Y., i, pi. 39, tig. 2. 
 
 
 
 
 
 
 
 -X- 
 
 # 
 
 
 
 
APPENDIX. 
 
 947 
 
 CATALOGUE OF LOWER SILURIAN FOSSILS. Continued. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 6 
 
 al 
 
 "3 
 
 .d 
 
 
 3 
 23 
 
 ^ 
 
 f 
 
 ' 
 
 W 
 
 -X- 
 % 
 
 QQ 
 
 ^ 
 
 180 
 145 
 
 115 
 180 
 
 144 
 144 
 144 
 
 145 
 
 145 
 117 
 132 
 
 132 
 144 
 119 
 
 EUNEMA. 
 
 E. cerithioides. 
 Erigone. 
 pagoda. 
 strigillata. 
 prisca. 
 
 LOXONBMA. 
 L. Murrayana. 
 HELICOTOMA. 
 H. perstriata. 
 planulata. 
 larvata. 
 spinosa. 
 MACLUREA. 
 M. Atlantica. 
 magna. 
 
 matutina. 
 Logani. 
 
 OPHILETA. 
 0. compacta. 
 Ottawaensis. 
 STRAPAROLLUS. 
 S. asperostriatus. 
 Circe. 
 Eurydice. 
 
 ECCULIOMPHALUS. 
 
 E. Trentonensis. 
 TROCHONEMA. 
 T. tricarinata. 
 umbilicata. 
 PLEUROTOMARIA. 
 P. abrupta. 
 Americana. 
 
 Amphitrite. 
 aperta. 
 Arachne. 
 calcifera. 
 calyx. 
 Crevieri. 
 docens. 
 Eugenia. 
 gregaria. 
 Helena. 
 immatura. 
 
 Salter, 1859. 
 " Dec. i, 30. Billings, Pal.Foss., 35. 
 Billings, Pal. Foss., 35. 
 Salter, Dee. i, pi. 6, fig. 5. 
 
 U It 11 It Q It 4 
 
 Billings, Can. Nat. Geol., iv, 360. 
 Phillips, 1841. 
 Salter, Dec. i, pi. 6, fig. 6. 
 Salter, 1856. 
 Billings, Can. Nat. Geol., iv, 356. 
 Salter, Dec., i, pi. 2, figs. 5-7. 
 tt n n it n it U-14 
 n ii it it it n 9_io. 
 
 Lesueur, 1818. 
 Billings, Can. Nat. Geol., iv, 459. 
 Lesueur, Jour. A. N. S., i, pi. 13, 
 figs. 1, 2, 3. 
 Hall, Pal. N. Y., i, pi. 3, fig. 3. 
 Salter, Rep. Brit. Assoc. 1851. Trans. 
 Sec. 63. Dec. i, pi. 1. 
 
 Vanuxem, 1842. 
 Salter, Dec. i, pi. 3. 
 Billings, Can. Nat. Geol., v, 167. 
 Montfort, 1810. 
 Billings, Can. Nat. Geol., v, 162. 
 " " " 161. 
 " " " 162. 
 Portlock, 1843. 
 Conrad, Jour. A.N.S., viii, pi. 17, fig.4. 
 
 Salter, 1859. 
 Billings, Can. Nat. Geol., iv, 356. 
 Pleurotomaria umbilicata, Hall. 
 Defrance, 1825. 
 Billings, Can. Nat. Geol., iv, 354. 
 " " v, 164. 
 P. lenticularis, Hall, not Sowerby. 
 Billings, Pal. Foss., 32. 
 Salter, Dec. i, pi. 2, fig. 4. 
 Billings, Pal. Foss., 31. 
 " Can. Nat. Geol., iv, 352. 
 " 454. 
 " " 456. 
 " " " 452. 
 " Pal. Foss., 30. 
 " Can. Nat. Geol., iv, 355. 
 " " v, 165. 
 " iv, 454. 
 
 
 -X- 
 -X- 
 -X- 
 
 * 
 
 -X- 
 
 -X- 
 -X- 
 
 * 
 * 
 
 -X- 
 -X- 
 
 -X- 
 
 # 
 
 -X- 
 -X- 
 
 -;c- 
 
 -X- 
 
 -X- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 # 
 
 
 .. 
 
 -x- 
 
 
 
 
 
 
 
 
 
 
 -X- 
 
 -x- 
 
 --;- 
 
 -X- 
 
 
 
 
 * 
 
 -X- 
 
 -;:- 
 
 
 
 
 
 
 
 
 
 
 
 
 -X- 
 
 -x- 
 
 -X- 
 
 -X- 
 
 x- 
 
 -X- 
 -X- 
 
 x- 
 
 
 
 
 
 -X- 
 
 
 
 -X- 
 
 -X- 
 
 -x- 
 
 -X- 
 
 # 
 
 .. 
 
 -x- 
 
 
 
 
948 
 
 GEOLOGY OF CANADA. 
 
 CATALOGUE OF LOWER SILURIAN FOSSILS. Continued. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 d 
 ^ 
 
 5 
 
 
 
 ^ 
 
 
 . 
 
 P2 
 
 m 
 
 ^ 
 H 
 
 5 
 
 K 
 ffi 
 
 CQ 
 & 
 
 m 
 
 PLEUROTOMARIA. Con. 
 P. Laurentina. 
 lapicida. 
 miser. 
 nodulosa. 
 
 Billings, Can. Nat. Geol., iv, 354. 
 Salter, Dec. i, pi. 2, figs. 1-3. 
 Billings, Can. Nat. Geol., iv, 354. 
 Hall Pal NY i pi 10 fig 10 
 
 
 
 # 
 
 -;:- 
 
 -. 
 
 -;:- 
 
 -;;- 
 
 
 
 
 
 pauper. 
 Progne. 
 
 Billings, Can. Nat. Geol., iv, 457. 
 " " v 163 
 
 
 
 
 
 -;:- 
 
 
 
 
 
 
 117 
 
 Ramsayi. 
 rotuloides. 
 
 " " iv, 351. 
 Hall, Pal NY i pi 37 fig 7 
 
 
 
 -;;- 
 
 
 
 
 
 
 
 180 
 
 subconica. 
 
 11 It It It It It Q 
 
 
 
 
 
 
 
 ,-. 
 
 
 
 Circe. 
 
 Billings, Rep. 1857, 303. 
 
 
 
 
 
 
 
 -V. 
 
 
 181 
 
 supracingulata. 
 
 " " " 302. 
 
 
 
 
 
 
 
 
 
 119 
 120 
 
 183 
 183 
 
 MURCHISONIA. 
 M. Anna. 
 arenaria. 
 aspera. 
 bellicinta. 
 bicincta. 
 gracilis. 
 helicteres. 
 
 D'Archiac and De Verneuil, 1841. 
 Billings, Can. Nat. Geol., iv, 358. 
 " " " 359. 
 " " " 458. 
 Hall, Pal. N. Y., i, pi. 39, fig. 1. 
 " " " " 38, " 5. 
 39 it 4 
 
 Salter, Dec. i., pi. 4, fig. 4. 
 
 \ 
 
 -/:- 
 -;;- 
 
 -;:- 
 
 # 
 
 -;;- 
 
 -;;- 
 & 
 * 
 
 
 -;:- 
 
 
 
 Hermione. 
 
 Billings, Pal. Foss., 33. 
 
 
 
 
 
 
 
 
 
 119 
 
 infrequens. 
 linearis. 
 modesta. 
 
 " Can. Nat. Geol., iv, 457. 
 " " " 359. 
 " Rep. 1857, 299. 
 
 .. 
 
 -;:- 
 
 -;;- 
 
 
 
 
 
 
 
 multivolvis. 
 
 " " " 244. 
 
 
 
 
 
 
 
 
 
 
 perangulata. 
 Procris. 
 
 Hall, Pal. N. Y., i, pi. 10, fig. 4. 
 Billings, Pal. Foss., 35. 
 
 .. 
 
 
 
 
 
 
 -::- 
 
 
 
 
 
 rugosa. 
 
 " Rep. 1857, 299. 
 
 
 
 
 
 
 
 
 
 145 
 
 serrulata. 
 
 Salter, Dec. i, pi. 4, fig. 1. 
 
 
 
 
 
 
 
 
 
 
 
 teretiformis. 
 
 Billings, Rep. 1857, 298. 
 
 
 
 
 
 
 
 
 
 
 varians. 
 
 " " " 300. 
 
 
 
 
 
 
 
 
 
 
 ventricosa. 
 
 Hall, Pal. N. Y., i, pi. 10, fig. 3. 
 
 
 
 
 
 
 
 
 
 
 METOPTOMA. 
 M. dubia. 
 deformis. 
 patelliformis. 
 Alceste. 
 
 Phillips, 1836. 
 Hall, Pal. N. Y., i, pi. 4, fig. 11. 
 
 It 11 it K JQ 
 
 " " 40 " 2 
 Billings, Pal. Foss., 153. 
 
 
 
 ' 
 
 -;:- 
 -::- 
 
 
 -;;- 
 
 
 
 
 145 
 
 Erato. 
 Estella. 
 
 " " 39. 
 " " 153. 
 
 
 
 t f 
 
 
 
 -;:- 
 
 
 
 
 
 217 
 
 Nycteis. 
 Trentonensis. 
 
 HETEROPODA. 
 CYRTOLITES. 
 C. compressus. 
 
 ornatus. 
 
 " " 38. 
 " " 40. 
 
 Conrad, 1838. 
 Phragmolites compressus, Conrad, Ann. 
 Rep. N. Y. 1838, 119. C. compressus, 
 Hall, Pal. N. Y., i, pi. 40 A, fig. 2. 
 Conrad, Ann. Rep. N. Y. 1838, 118. 
 Hall, Pal. N. Y., pi. 84., fig. 1. 
 
 
 
 # 
 
 
 
 -;:- 
 
 -;:- 
 
 -X- 
 
 
 * 
 
 
APPENDIX. 
 
 949 
 
 CATALOGUE OF LOWER SILURIAN FOSSILS. Continued. 
 
 Pag 
 
 GENERA AND SPECIES 
 
 AUTHORS AND REFERENCES. 
 
 
 
 PH 
 
 "s 
 
 ~ 
 
 oc 
 
 05 
 
 ' *^ 
 H t> 
 
 ^ 
 Zl 
 
 cc 
 S 
 
 
 BELLEROPHON. 
 
 Montfort, 1810. Bucania, Hall, pars 
 
 
 
 
 
 
 
 
 146 
 
 B. Argo .* 
 
 Billings, Can. Nat. Geol., v, 167. 
 
 . 
 
 . 
 
 . 
 
 * 
 
 * 
 
 
 
 
 bidorsatus. 
 
 Hall, Pal. N. Y., i, pi. 40, fig. 8. 
 
 . 
 
 . 
 
 . 
 
 -X- 
 
 > 
 
 
 
 184 
 
 bilobatus. 
 
 Sowerby. 
 
 . 
 
 . 
 
 . 
 
 -* 
 
 * * 
 
 * 
 
 -X- 
 
 146 
 
 Charon. 
 
 Billings, Can. Nat. Geol., v, 169. 
 
 i. 
 
 
 . 
 
 * 
 
 * 
 
 
 
 146 
 
 disculus. 
 
 " " " 168. 
 
 . 
 
 . 
 
 . 
 
 * 
 
 * 
 
 
 
 
 expansus. 
 
 Hall, Pal. N. Y., i, pi. 40, fig. 7. 
 
 
 
 
 -X- 
 
 ;c- 
 
 
 
 
 punctifrons. 
 
 Conrad, Emmons, Hall, Pal. N. Y., i, 
 
 
 
 
 
 
 
 
 
 
 pi. 40, fig. 1. 
 
 
 
 .. 
 
 -* 
 
 * 
 
 
 
 146 
 
 sulcatinus. 
 
 Emmons, Geol. Rep. N. Y., 312. 
 
 
 
 
 % 
 
 A- 
 
 
 
 
 PTEROPODA. 
 
 
 
 
 
 
 
 
 
 
 PTEROTHECA. 
 
 Salter, 1852, = Clioderma, Hall, 14th 
 
 
 
 
 
 
 
 
 
 
 Reg. Rep., 98. 
 
 
 
 
 
 
 
 
 
 P. expansa. 
 
 Delthyris expansus, Emmons, Geol. 
 
 
 
 
 
 
 
 
 
 
 Rep. N. Y., 397. Clioderma expansa, 
 
 
 
 
 
 
 
 
 
 
 Hall, 14th Reg. Rep., 98. 
 
 . 
 
 
 
 , 
 
 - 
 
 '; 
 
 
 
 
 THECA. 
 
 Sowerby ; Morris, 1844. 
 
 
 
 
 
 
 
 
 
 T. (sps. undeser.) 
 
 x 
 
 < 
 
 . 
 
 p 
 
 . 
 
 5- 
 
 
 
 
 SALTERELLA. 
 
 Billings, 1861. 
 
 
 
 
 
 
 
 
 
 S. obtusa. 
 
 " Pal. Foss., 18. 
 
 X 
 
 
 
 
 
 
 
 
 pulchella. - 
 
 tl U 
 
 * 
 
 
 
 
 
 
 
 285 
 
 rugosa. 
 
 " " 17. 
 
 |^ 
 
 
 
 
 
 
 
 
 CEPHALOPODA. 
 
 
 
 
 
 
 
 
 
 
 ORTHOCBRAS. 
 
 Breyn, 1732. 
 
 
 
 
 
 
 
 
 
 (1) Species figured in 
 
 
 
 
 
 
 
 
 
 
 Pal. N. Y., vol. i. 
 
 
 
 
 
 
 
 
 
 
 0. amplieameratum. 
 
 Hall, Pal. N. Y., i, pi. 51, fig. 1. 
 
 , 
 
 , 
 
 t 
 
 & * 
 
 
 
 
 150 
 
 aneeps. 
 
 Gonioceras aneeps, Hall, Pal. N. Y., i, 
 
 
 
 
 
 
 
 
 
 
 pi. 14. ' 
 
 . 
 
 , 
 
 . 
 
 JJ, 
 
 
 
 
 
 anellum. 
 
 Conrad, Proc. A. N. S., i, 334. Hall, 
 
 
 
 
 
 
 
 
 
 
 Pal. N. Y., i, pi. 43, fig. 6. 
 
 . 
 
 . 
 
 . 
 
 ' -.' 
 
 1 
 
 
 
 
 atmulatum, 
 
 Hall, Pal. N. Y., i, pi. 44. 
 
 , 
 
 t 
 
 t 
 
 * -. 
 
 
 
 
 
 arcuoliratum. 
 
 " " " " 42, fig. 7. 
 
 
 
 t 
 
 . 
 
 * * 
 
 
 
 
 149 
 
 Bigsbyi. 
 
 Stores, Geol. Trans. [2], i, 195, pi. 25, 
 
 
 
 
 
 
 
 
 
 
 figs. 1-3, 1824. Ormoceras tenuifi- 
 
 
 
 
 
 
 
 
 
 
 lum, Hall, Pal. N.Y., i, pi. 15, 16,17. 
 
 , 
 
 . 
 
 
 . 
 
 
 
 
 
 bilineatum. 
 
 Hall, Pal. N. Y., i, pi. 43, figs. 2-3. 
 
 . 
 
 . 
 
 r 
 
 - 3 
 
 
 -::- 
 
 
 218 
 
 crebriseptum. 
 
 " " " " 86, fig. 2. 
 
 , 
 
 , 
 
 , 
 
 t 
 
 , . 
 
 -X- 
 
 
 
 fusiforme. 
 
 ' tt ti it it 20 
 
 , 
 
 t 
 
 t 
 
 % -X 
 
 
 
 
 
 juneeum. 
 
 " " " " 47, fig. 3. 
 
 , 
 
 
 
 
 . 
 
 
 
 
 
 laqueatum. 
 
 n n u tt 3 12 
 
 
 
 . 
 
 . 
 
 jj. 
 
 
 
 
 
 longissimum. 
 
 Zndoceras longissimum, and E. multi- 
 
 
 
 
 
 
 
 
 
 
 ; tubulatum, Hall, Pal.N.Y.^ i, pl.18. 
 
 . 
 
 . 
 
 . 
 
 * * 
 
 
 
 
 
 mul ticameratum. 
 
 Emmons, Geo. Rep. N. Y., 3/82. Hall, 
 
 
 
 
 
 
 
 
 
 
 Pal. N. Y.,i, pi. 11, fig. 1. 
 
 ; 
 
 
 
 -- 
 
 * -X 
 
 
 
 
950 
 
 GEOLOGY OF CANADA. 
 
 CATALOGUE OF LOWER SILURIAN FOSSILS. Continued. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 js 
 
 H B 
 
 c 
 
 1 
 
 Q 
 4 
 
 
 ORTHOCERAS. Con. 
 
 
 
 
 
 
 
 0, primigenium. 
 
 Vanuxem, Geol. Rep. N. Y., 36, fig. 4, 
 
 
 
 
 
 
 
 Hall, Pal. N. Y. ; i, pi. 3, fig. 11. 
 
 *''" * 
 
 
 
 
 
 proteiforme. 
 
 Endoceras proteiforme, Hall, Pal. N.Y., 
 
 
 
 
 
 
 
 i, pi. 46. 
 
 .... -x 
 
 * 
 
 
 
 
 recticameratum. 
 
 Hall, Pal. N.Y., i, pi. 11, Gg. 1 d. 
 
 .... -x 
 
 
 
 
 
 strangulatura. - 
 
 " 46, 4. 
 
 
 Ic 
 
 
 
 
 strigatum. 
 
 " " " " 56, " 1. 
 
 .... * 
 
 -X- 
 
 
 
 
 subarcuatum. 
 
 it it tt n 7 " 3 
 
 . . -X- 
 
 
 
 
 
 ^2) Species described 
 
 
 
 
 
 
 
 by E. B. in Canadian 
 
 
 
 
 
 
 
 publications. 
 
 
 
 
 
 
 
 3 \n tico^ ticnsc 
 
 Billings, Rep. 185 7, 316. 
 
 
 
 y f 
 
 
 
 Allumettense. 
 
 " " " 331. 
 
 . . -3C- -5 
 
 
 
 
 
 balteatum. 
 
 " " " 318. 
 
 
 
 
 * 
 
 
 
 cornuum. 
 
 " " " 329. 
 
 . . -55- 
 
 
 
 
 
 decrescens. 
 
 " " " 337. 
 
 . . . . -3 
 
 * 
 
 
 
 
 formosum. 
 
 " " " 317. 
 
 
 -;:- 
 
 # 
 
 
 
 hastatum. 
 
 " " " 333. 
 
 . . . . - 
 
 -X- 
 
 
 
 
 Huronense. 
 
 " " " 337. 
 
 
 
 55- 
 
 
 
 
 Lyelli. 
 
 " " " 320. 
 
 
 
 
 -X- 
 
 
 
 magnisulcatum. 
 
 " " " 330. 
 
 
 
 
 -x- 
 
 
 
 Minganense. 
 
 " " " 319. 
 
 . . -X- - 
 
 
 
 
 
 Murray!. 
 
 " " " 332. 
 
 
 -X- 
 
 
 
 
 Ottawaense. 
 
 " " " 331. 
 
 
 X- 
 
 
 
 
 perannulatum. 
 
 " " " 320. 
 
 
 . . . 
 
 -X 
 
 
 
 propinquum. 
 
 " " " 320. 
 
 
 
 .. . 
 
 -X 
 
 
 
 Python. 
 
 " " " 335. 
 
 
 
 -X- 
 
 
 
 
 Sedgwicki. 
 
 " " " 320. 
 
 
 
 4 
 
 
 
 vulgatum. 
 
 " " " 337. 
 
 
 * 
 
 
 
 
 xiphias. 
 
 " " " 318. 
 
 . . . . . 
 
 * 
 
 
 
 
 An tenor. 
 
 " Can. Nat..Geol., iv, 463. 
 
 . . -X- 
 
 
 
 
 121 
 
 Becki. 
 
 " " " 362. 
 
 -X- 
 
 
 
 
 121 
 
 deparcum. 
 
 " " " 363. 
 
 # 
 
 
 
 
 121 
 
 Lamarcki. 
 
 " " " 362. 
 
 *x* 
 
 
 
 
 
 Maro. 
 
 " " " 461. 
 
 
 
 
 
 121 
 
 Montrealensis. 
 
 " " " 363. 
 
 * 
 
 
 
 
 
 Shumardi. 
 
 " " " 460. 
 
 
 
 
 
 121 
 
 sordidum. 
 
 " " 363. 
 
 K- 
 
 
 
 
 
 pertinax. 
 
 " " v. 175. 
 
 
 
 
 
 
 rapax. 
 
 " " 176. 
 
 
 
 
 
 
 tener. 
 
 " " " 174. 
 
 
 
 
 
 
 Menelaus. 
 
 " Pal. Foss., 26. 
 
 
 
 
 
 
 perparvum. 
 
 " " 27. 
 
 
 
 
 
 
 CYRTOCERAS. 
 
 Goldfuss, 1833. 
 
 
 
 
 
 
 C. annulatum. 
 
 Hall, Pal. N. Y., i, pi. 41, fig. 4. 
 
 
 -X- 
 
 
 
 
 Billingsii. 
 
 Salter,Dec. i,pl. 7, figs. 5, 6. 
 
 .... 
 
 
 
 
APPENDIX. 
 
 951 
 
 CATALOGUE OF LOWER SILURIAN FOSSILS. Continued. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 6 
 
 * 
 
 le 
 
 
 .'" 
 
 J3 
 
 CJ ( CQ 
 
 il 
 
 ' 
 
 s; a - 
 
 OQ 
 
 a 
 
 
 CYBTOCEBAS. Con. 
 
 
 
 
 
 
 
 
 
 
 
 C. constrietum. 
 
 Oncoceras constrictum, Hall, Pal.N.Y., 
 
 
 
 
 
 
 
 
 
 
 
 i, pi. 41, fig. 6. 
 
 - 
 
 
 
 .. 
 
 -::- 
 
 -;: 
 
 
 
 
 
 exiguum. 
 
 Billings, Can. Nat. Geol., v, 172. 
 
 
 
 
 
 
 
 
 
 -;:- 
 
 
 
 
 
 falx. 
 
 " Rep. 1857, 314. 
 
 
 
 
 - 
 
 -::- 
 
 -;:- 
 
 
 
 
 
 Lysander. 
 
 Pal. Foss., 161. 
 
 .. 
 
 
 .. 
 
 .. 
 
 _ 
 
 
 
 -X- 
 
 
 
 macrostomum. 
 
 Hall r Pal. N. Y., i, pi. 42, fig. 1. 
 
 .. 
 
 -. 
 
 .. 
 
 -;:- 
 
 
 
 
 
 
 multicameratum. 
 
 n u u n 4 
 
 .. 
 
 
 .. 
 
 -;:- 
 
 
 
 
 
 
 McCoyi. 
 
 Billings, Can. Nat. Geol., iv, 467. 
 
 
 
 -. 
 
 -X- 
 
 
 
 
 
 
 
 regulare. 
 
 " Rep. 1857, 314. 
 
 
 
 
 
 
 
 # 
 
 * 
 
 
 
 
 
 simplex. 
 
 " " " 313. 
 
 .. 
 
 .. 
 
 .. 
 
 -;;- 
 
 * 
 
 
 
 
 
 sinuatum. 
 
 " 315. 
 
 ., 
 
 
 
 -X- 
 
 
 
 
 
 
 subturbinatum. 
 
 " " " 312. 
 
 . 
 
 
 
 * 
 
 # 
 
 
 
 
 
 
 GOMPHOCERAS. 
 
 Sowerby. 
 
 
 
 
 
 
 
 
 
 
 G. obesum. 
 
 Billings, Rep. 1857, 311. 
 
 
 
 
 
 
 
 -;; 
 
 
 
 
 
 
 
 
 
 PHBAMOCERAS. 
 
 Broderip, 1839. 
 
 
 
 
 
 
 
 
 
 
 P. praematurum. 
 
 Billings, Can. Nat. Geol., v, 173. 
 
 
 
 
 
 
 
 -;:- 
 
 # 
 
 
 
 
 
 LlTUITES. 
 
 Breyn, 1732. 
 
 
 
 
 
 
 
 
 
 
 L. magnifieum. 
 
 Gyroceras magnifieum^ Billings, Rep. 
 
 
 
 
 
 
 
 
 
 
 
 1857, 307. 
 
 
 
 
 
 
 
 -;:- 
 
 
 
 
 
 
 
 
 
 undatum. 
 
 Hall, Pal. N. Y., i, pi. 13. 
 
 
 
 . 
 
 -::- 
 
 
 
 
 
 
 vagrans. 
 
 Gyroceras vagrans, Billings, Rep. 1857, 
 
 
 
 
 
 
 
 
 
 
 
 308. 
 
 .. 
 
 
 . 
 
 -;:- 
 
 
 
 
 
 
 NAUTILUS. 
 
 Breyn, 1732. 
 
 
 
 
 
 
 
 
 
 
 N. Hercules. 
 
 Billings, Rep. 1857, 306. 
 
 
 
 
 
 
 
 -;:- 
 
 
 
 
 
 
 
 
 
 > Jason. 
 
 " Can. Nat. Geol., iv, 464. 
 
 
 
 
 * 
 
 
 
 
 
 
 
 natator. 
 
 " " 466. 
 
 
 
 
 # 
 
 
 
 
 
 
 
 tyrans. 
 
 " " " 465. 
 
 
 
 
 
 -:- 
 
 
 
 
 
 
 
 ASCOCERAS. 
 
 Barrande. 
 
 
 
 
 
 
 
 
 
 218 
 
 A. Canadense. 
 
 Billings, Rep. 1857, 310. 
 
 
 
 
 
 
 
 :'.= 
 
 
 
 
 
 
 
 
 
 NewberryL 
 
 " Pal. Foss., 163. 
 
 
 
 
 
 
 
 # 
 
 
 
 
 
 
 
 
 
 PlLOCEBAS. 
 
 Salter. 
 
 
 
 
 
 
 
 
 
 
 P. Canadense. 
 
 Billings, Can. Nat. Geol., v. 171. 
 
 
 
 * 
 
 
 
 
 
 
 
 
 CRUSTACEA. 
 
 
 
 
 
 
 
 
 
 
 
 ASAPHUS. 
 
 Brongniart, 1822 ; includes Isotelus of 
 
 
 
 
 
 
 
 
 
 
 
 DeKay. 
 
 
 
 
 
 
 
 
 
 204 
 
 A. Canadensig. 
 
 Chapman, Can. Jour. [2], i, 482 ; ii, 
 
 
 
 
 
 
 
 
 
 
 
 47 ; iii, 230. Ann. Nat. Hist. [3], 
 
 
 
 
 
 
 
 
 
 
 
 ii 9 fie- 1 
 
 
 
 
 
 
 ,;;. 
 
 
 
 
 Halli. 
 
 A1 "> "& * 
 Chapman, Can. Jour. [2], ii, 235. 
 
 
 
 
 
 
 
 
 
 
 
 " Ann Nat Hist [3] ii 14 fig 2 
 
 
 
 
 
 
 .x. 
 
 
 
 
 Kincksii.. 
 
 " " iv 2 
 
 
 
 
 
 
 M 
 
 
 
 184 
 
 megistos. 
 
 IT , U. 
 
 Locke, Proc. Am. Assoc. 1841,221. 
 
 
 . . 
 
 .. 
 
 -;: 
 
 * 
 
 
 * 
 
 * 
 
 184 
 
 platycephalus. 
 
 Stokes, 1822. Isotelus gigas, De Kay, 
 
 
 
 
 
 
 
 
 
 
 
 1824. 
 
 * * 
 
 
 
 * 
 
 -:;- 
 
 * 
 
 * 
 
 * 
 
 
952 
 
 GEOLOGY OF CANADA 
 
 CATALOGUE OF LOWER SILURIAN FOSSILS. Continatd. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 6 
 
 Pu 
 
 15 
 o 
 
 J3 
 
 Q 
 
 aq 
 
 25 
 
 tl 
 
 H 
 
 3 
 
 
 
 K 
 -.-- 
 
 '.: 
 
 M 
 
 CQ 
 
 3 
 
 190 
 133 
 
 122 
 133 
 122 
 
 122 
 153 
 
 153 
 188 
 
 188 
 
 1ST 
 1ST 
 
 133 
 151 
 
 ACIDASPIS. 
 A. Horani. 
 Trentonensis. 
 AMPHION. 
 A. Canadensis. 
 AMPYX. 
 A. Halli. 
 BATHYURUS. 
 B. amplimarginatus. 
 Angelini. 
 conicus. 
 Cordai, 
 CybeK 
 extans. 
 
 parvulus. 
 senectus. 
 Smithi. 
 spiniger. 
 
 BRONTBUS. 
 B. lunatus. 
 CALYMENE. 
 C. Blumenbachii. 6 
 CHEIRUBCS. 
 C . loams, 
 pleurexanthemus. 
 
 CONOCEPHALITES. 
 
 C. A dam si. 
 arenosus. 
 miser. 
 Teucer. 
 Vulcamas. 
 
 DAJ.MANITBS. 
 D. Achates. 
 Bebryx. 
 ENCRiNURUg. 
 E. vigilans. 
 
 HARPBS. 
 H. antiquatua^. 
 ~ Dentoni, 
 ILL^NUS. 
 I. Americanus. 
 angusticollis. 
 arcturus. 
 
 Murchison, 1839. 
 Billings, Rep. 185T, 341. 
 Hall, Pal. N. Y., i, pi. 64, fig. 4. 
 Pander, 1830. 
 Billings, Can. Nat. Geol., iv, 381. 
 Dalman, 1827. 
 Billings, Pal. Foss., 24. 
 Billings, 1859. 
 " Can. Nat. Geol., iv, 365. 
 " " " 468. 
 " " " 366. 
 " v, 321. 
 . " " iv, 366. 
 Asaphus ? extans, Hall, Pal. N. Y., i, 
 pi. 60, fig. 2. 
 Billings, Pal. Foss., 16. 
 " " 15. 
 " " 56. 
 Actdaspis spiniger, Hall, Pal. N.Y., i, 
 pi. 64, fig. 5. 
 Burmeister, 1843. 
 Billings, Rep. 1857, 338. 
 Brongniart, 1822. 
 " Crust. Foss., i; fig 1. 
 
 Beyrich, 1815, = Ceraurus, Pal. N. Y. 
 Billings, Can. Nat. Geol., Y, 67, 
 Cer&urus plewexanthemvs^ Green. 
 Zenker, 1833. 
 Billinga> Pal. Foss,, 11, 
 " " 15. 
 " 11. 
 " " 14. 
 " 15. 
 
 Emmerich, 1845. 
 Billings, Can. Nat. Geol., Y, 63. 
 <c it cc 61. 
 
 Emmrich, 1845. 
 Ceraurus vigilans, Hall, Pal. N. Y., i, 
 pi. 65, fig. a. 
 Goldfiiss, 1839. 
 Billings, Can. Nat. Gool., iv, 468. 
 " viii, 3G. 
 
 Dalman, 1826. 
 Billings, Can. Nat. Geol., iv, 371. 
 " " 376. 
 Hall, Pal. N. Y., i, pi. 4, fig. 12. 
 
 -X- 
 X- 
 
 -X- 
 
 x- 
 
 -X- 
 
 - 
 
 
 
 
 
 
 
 
 -;;- 
 
 -;:- 
 -x- 
 
 -X- 
 
 -X- 
 
 
 -X- 
 
 * 
 
 5C- 
 
 * 
 
 -X- 
 
 - 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 * 
 
 * 
 
 - 
 ft 
 
 * 
 
 * 
 * 
 
 -XJ 
 
 * 
 * 
 * 
 
 ?:- 
 
 X- 
 
 
 
 
 
 
 
 
 
 
 - 
 
 
 
 .. 
 
 - 
 
 
 
 
 
 
 
 
 - 
 -X- 
 
 
 
 
 
 * 
 
APPENDIX. 
 
 953 
 
 CATALOGUE OF LOWER SILURIAN FOSSILS. Continued. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 6 
 
 A.' 
 
 "03 
 U 
 
 ^ 
 
 o 
 
 M 
 
 
 ^ 
 
 H 
 
 i 
 
 
 a: 
 
 W 
 3 
 
 
 ILL.SNUS. Con. 
 
 
 
 
 
 
 
 
 
 
 133 
 
 I. Bayfieldi. 
 
 Billings, Can. Nat. Geol., iv, 369. 
 
 .. 
 
 . . 
 
 -X- 
 
 
 
 
 
 
 
 elavifrons. 
 
 (i u 379^ 
 
 .. 
 
 .. 
 
 -A- 
 
 * 
 
 
 
 
 
 151 
 
 conifrons. 
 
 " " " 378. 
 
 
 
 
 ^ 
 
 
 
 
 
 
 Conradi. 
 
 " cc u 372. 
 
 . . 
 
 . , 
 
 -:<- 
 
 
 
 
 
 
 133 
 
 globosus. 
 
 " " " 367. 
 
 .. 
 
 ... 
 
 K- 
 
 
 
 
 
 
 
 grandis. 
 
 " " " 380. 
 
 
 
 
 
 
 
 
 .V. 
 
 151 
 
 Milleri. 
 
 " " " 375. 
 
 
 
 
 .V, 
 
 yC* 
 
 
 v** 
 
 
 
 -i orbicaudatus. 
 
 n ti it 379^ 
 
 
 
 
 
 
 
 -5C- 
 
 -A* 
 
 
 -^ ovatus. 
 
 Conrad Proc. A. N. S. i 332. 
 
 
 
 
 J^ 
 
 
 
 
 A 
 
 
 
 
 
 
 
 
 
 
 
 
 
 LlCHAS. 
 
 Dalman, 1826. 
 
 
 
 
 
 
 
 
 
 
 L. Trentonensis. 
 
 Platynotus Trentonensis, Conrad, Jour. 
 
 
 
 
 
 
 
 
 
 
 
 A. N. S., viii, pi. 16, fig. 16. 
 
 
 
 
 ^ 
 
 7^ 
 
 
 
 
 
 PARADOXIDES. 
 
 Brongniart, 1822. 
 
 
 
 
 
 
 
 
 
 
 P. Thompson!. 
 
 Olenus Thompsoni, Hall, 12th Reg. 
 
 
 
 
 
 
 
 
 
 
 
 Rep., 59. Barrandia Thompsoni, 
 
 
 
 
 
 
 
 
 
 
 
 13th Reg. Rep., 116. 
 
 -X- 
 
 
 
 
 
 
 
 
 
 Vermontana. 
 
 Olenus Vermontana, Hall, Loc. cit. 
 
 
 
 
 
 
 
 
 
 
 
 These two may probably consti- 
 
 
 
 
 
 
 
 
 
 
 
 tute but one species. 
 
 % 
 
 
 
 
 
 
 
 
 
 PHACOPS. 
 
 Emmrich, 1839. 
 
 
 
 
 
 
 
 
 
 187 
 
 P. callicephalus. 
 
 Hall, Pal. N. Y., i, pi. 65, fig. 3. This 
 
 
 
 
 
 
 
 
 
 
 
 species is probably a Dalinanites 
 
 
 
 
 X- 
 
 ^; 
 
 
 55* 
 
 
 
 PROETUS. 
 
 Steininger, 1831. 
 
 
 
 
 
 
 
 
 
 219 
 
 P. Alaricus. 
 
 Billings, Can. Nat. Geol., v, 68. 
 
 
 
 
 
 
 
 
 
 
 TRIARTHRUS. 
 
 Green. 
 
 
 
 
 
 
 
 TC 
 
 
 202 
 
 T. Beckii. 
 
 Eaton. 
 
 
 
 
 
 
 -X- 
 
 
 
 
 glaber. 
 
 Billings, Can. Nat. Geol., iv, 382. 
 
 
 
 
 
 
 ^. 
 
 
 
 202 
 
 spinosus. 
 
 " Rep. 1857, 340. 
 
 
 
 
 
 
 '/' 
 
 
 
 
 Canadensia. 
 
 Smith, Can. Jour. [2], vi, 275. 
 
 
 
 
 
 
 %r 
 
 
 
 
 TRINUCLEUS. 
 
 Lhwyd, 1698. 
 
 
 
 
 
 
 
 
 
 190 
 
 T. concentricus. 
 
 Eaton, 1832. 
 
 
 
 
 
 ^ 
 
 *5\* 
 
 ^ 
 
 
 
 C LIMACTICHNITES. 
 
 Logan, Can. Nat. Geol., v, 5, 279. 
 
 
 
 
 
 
 
 
 
 
 C. Wilsoni. 
 
 " " " fig. 1-5 
 
 * 
 
 
 
 
 
 
 
 
 
 PROTICHNITBB. 
 
 Owen, Jour. Geol. Soc., v, 8, 1852. 
 
 
 
 
 
 
 
 
 
 
 P. alternans. 
 
 " " " pi. 14. 
 
 
 
 
 
 
 
 
 
 
 
 latus. 
 
 11 
 
 # 
 
 
 
 
 
 
 
 
 
 lineatus. 
 
 11 U U JJ^ 
 
 
 
 
 
 
 
 
 
 
 
 multinotatus. 
 
 " 12. 
 
 # 
 
 
 
 
 
 
 
 
 
 octonotatus. 
 
 <( <( u }Q 
 
 * 
 
 
 
 
 
 
 
 
 
 geptemnotatus. 
 
 K u u 9_ 
 
 
 
 
 
 
 
 
 
 
 
 ENTOMOSTRACA. 
 
 , 
 
 
 
 
 
 
 
 
 
 
 BEYRICHIA. 
 
 McCoy, 1850. 
 
 
 
 
 
 
 
 
 
 
 B. Logani. 
 
 Jones, Ann. Nat. Hist. [3], i, 244, pi. 4, 
 
 
 
 
 
 
 
 
 
 
 
 figs. 6-10. Dec., iii, 41, pl.ll,figs. 1-5. 
 
 
 * 
 
 K- 
 
 
 
 
 
 
954 
 
 GEOLOGY OF CANADA. 
 
 QATALOGUE OF LOWEK SILURIAN FOSSILS. Concluded. 
 
 Page 
 
 GENERA AND SPECIES. 
 
 AUTHORS AND REFERENCES. 
 
 d 
 
 
 -3 
 
 *| 
 
 oq 
 ^ 
 
 _ 
 
 J 
 
 LD 
 
 
 
 W 
 
 m 
 
 & 
 
 
 LEPERDITIA. 
 
 Rouault, 1851. 
 
 
 
 
 
 
 
 
 
 
 L. Canadensis. 
 
 Jones, Ann. Nat. Hist. [3], i, 244, pi. 
 
 
 
 
 
 
 
 
 
 
 
 11, figs. 11-15. Dec., iii, pi. 11, 
 
 
 
 
 
 
 
 
 
 
 
 figs. 6, 7, 9, 10. 
 
 
 
 
 
 -x- 
 
 # 
 
 X- 
 
 
 
 
 
 labrosa. 
 
 Jones Dec., iii, pi. 11, fig. 8. 
 
 . 
 
 . 
 
 * 
 
 
 
 
 
 
 
 Louckiana. 
 
 It It, tt It It It -Q^ 
 
 
 . 
 
 
 -x- 
 
 
 
 
 
 
 Paquettiana. 
 
 it it it, it it it j2. 
 
 
 . 
 
 . , 
 
 -X- 
 
 
 
 
 
 
 Josephiana. 
 
 It It It (I It tl IQ 
 
 
 . 
 
 
 -X- 
 
 -X- 
 
 
 
 
 
 Anticostiana. 
 
 it it tt tt it it ]_Y. 
 
 " 
 
 
 
 
 
 
 -x- 
 
 -/< 
 
 
 Anna. 
 
 tt tt tt u n it ^ 
 
 
 X- 
 
 
 
 
 
 
 
 
 amygdalina. 
 
 it tt it tt tt it ^g iQ 
 
 .. 
 
 
 
 -x- 
 
 
 
 
 
 
 ISOCHILINA. 
 
 Jones, 1858. 
 
 
 
 
 
 
 
 
 
 
 I. Ottawa. 
 
 " Dec. iii, pi. 11, fig. 14. 
 
 
 
 
 X- 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 
 gracilis. 
 
 tt it tc it it it 15 
 
 
 
 
 -X- 
 
 
 
 
 
 
 CYTHEROPSIS. 
 
 McCoy, 1855. 
 
 
 
 
 
 
 
 
 
 
 C. concinna. 
 
 Jones, Ann. Nat. Hist. [3], 
 
 
 
 
 
 
 
 
 
 
 
 i, 249 pi 10 figs 3 4 
 
 
 
 
 -;;- 
 
 
 
 
 
 
 siliqua. 
 
 It It It It It It It Q 
 
 
 
 
 -;;- 
 
 
 
 
 
 
 rugosa. 
 
 tt tt it it it tt tt 
 
 
 
 
 -X- 
 
 
 
 
 
 
 ANNELIDA? 
 
 
 
 
 
 
 
 
 
 
 
 SERPULITES. 
 
 McLeay, 1838. 
 
 
 
 
 
 
 
 
 
 
 S. dissolutus. 
 
 Billings, Pal. Foss., 56. 
 
 
 
 
 .;;. 
 
 
 
 
 
 
 splendens. 
 
 " Can. Nat. Geol., iv, 470. 
 
 
 
 
 
 # 
 
 
 
 
 
 
 
 INCERT^E SEDIS. 
 
 
 
 
 
 
 
 
 
 
 
 SCOLITHUS. 
 
 Haldeman, Sup. Mon. Lim. 1840. 
 
 
 
 
 
 
 
 
 
 101 
 
 S. Canadensis. 
 
 Billings, Pal. Foss., 96. 
 
 * 
 
 
 
 
 
 
 
 
 
 linearis. 
 
 Hall, Pal. N. Y., i, pi. 1, fig. 1. 
 
 * 
 
 
 
 
 
 
 
 
 
 PASOEOLUS. 
 
 Billings, Rep. 1857, 342. 
 
 
 
 
 
 
 
 
 
 
 P. globosus. 
 
 u tt it 343 
 
 
 
 
 
 
 
 
 -X- 
 
 
 
 
 1 It is not certain whether these fossils are sponges or corals. 
 
 2 Edwards and Haime are of opinion that Favistella is not generically distinct from 
 Columnaria, and that F. stellata is specifically identical with C. alveolata. Polyp. Foss. 
 308, 309. 
 
 3 Strophomena recta and S. pecten appear to belong to the genus Streptorkynchus. 
 
 4 The genera Holopea, Hall 1847 ; Cyclonema, Hall 1852 ; Platyostoma, Conrad 1839 ; 
 and Platyceras, Conrad 1840, are connected by such numerous transitions that it is scarcely 
 possible to draw lines between them. 
 
 6 Calymene senaria of the N. Y. Reports. It may be distinct from the typical form of 
 the species. There are several varieties in the Canadian rocks. 
 
APPENDIX. 
 
 955 
 
 LIST OF THE GRAPTOLTTID^ OF THE QUEBEC GEOUP. 
 
 GRAPTOLITHTTS. plate> Figure> 
 
 . abnormis, XI. 6 
 
 alatus, VI. 9 
 
 antennarius, XIII. 14-17 
 
 arcuatus, II. 6-9 
 
 bifidus, (also III, 9, 10) I. 16-18 
 
 Bigsbyi, XVI. 22-30 
 
 bryonoides, (also III, 11, 12, and VI, 4 ?) IV. 1-10 
 
 constrictus, I. 23-27 
 
 crucifer, V. 10 
 
 denticulatus, IV. 12-16 
 
 extensus, II. 10-16 
 
 extenuatus, I. 21, 22 
 
 flexilis, X. 3-9 
 
 fructicosus, (also VI, 1-3) V. 6-8 
 
 Headi, VI. 8 
 
 indentus, I. 20 
 
 Logani, IX. 1-9 
 
 Logani var XI. 7 
 
 nitidus, I. 1-9 
 
 octobrachiatus, (also VIII, 1-4) VII. 1-7 
 
 octonarius, X. 1-2 
 
 patulus,- I. 10-15 
 
 pennatulus, III. 1-8 
 
 pristiniformis, XIII. 11-13 
 
 quadribrachiatus, (also VI, 6, 7) V. 1-5 
 
 ramulus, XII. 9, 10 
 
 Richardsoni, XII. 1-8 
 
 rigidus, XI. 1-5 
 
 similis, II. 1-5 
 
 RETIOLITES. 
 
 B. ensiformis, XIV. 1-5 
 
 RETIOGRAPTUS. 
 
 R. tentaculatus, XIV. 6-8 
 
 PHYLLOQBAPTUS. 
 
 P. angustifolius, XVI. 17-21 
 
 Anna, XVI. 11-16 
 
 ilicifolius, XVI. 1-10 
 
 typus, XV. 1-12 
 
 DENDROGBAPTUS. 
 
 D. diffusus, XVIII. 1-3 
 
 divergens, XVII. 3-4 
 
 'erectus, XVII. 7 
 
 flexuosus, XVII. 1, 2 
 
 fruticosus, XVII. 8, 9 
 
 gracilis, XVIII. 5, 6 
 
 striatus, XVII. 5, 6 
 
 DECADE II. 
 
956 
 
 GEOLOGY OF CANADA. 
 
 GEAPTOLITID^ OF THE QUEBEC GROUP. Continued. 
 
 CALLOGRAPTUS. 
 
 DECADE II. 
 
 Plate. 
 XIX. 
 XIX. 
 
 XX. 
 XX. 
 XX. 
 XX. 
 
 XXI. 
 XXI. 
 
 XXI. 
 
 Figure. 
 5-8 
 1-4 
 
 1,2 
 5 
 6,7 
 3,4 
 
 5-8 
 1-4 
 
 9 
 
 Salteri, 
 
 DlGTYONEMA. 
 
 
 
 
 PTILOGRAPTUS. 
 P. Geinitzianus, 
 
 
 THAMNOGRAPTUS. 
 
 
APPENDIX. 
 
 FOSSILS OF THE LOWER HELDERBERG GROUP. 
 
 448 449 
 
 957 
 
 454 
 
 a 451 6 452 
 
 448. Strophomena punctulifera (Conrad) ; dorsal view. 
 
 449. Streptorhynchus Woolworthana (Hall) ; dorsal view. 
 
 450. Eatonia peculiaris (Conrad) ; a, front, and b, ventral view. 
 
 451. Leptoccelia concava (Hall) ; o, dorsal, and 6, side view. 
 
 452. L. ' imbricata (Hall) ; dorsal view. 
 
 453. Pentamerus Verneuilli (Hall) ; a, dorsal, and 6, side view. 
 
 454. P. galeatus (Dalman) ; a, dorsal, and 6, side view. 
 
 455. Spirifera perlamellosa (Hall), dorsal view. 
 
 456. S. macropleura (Conrad), dorsal view. 
 
 457. S. cycloptera (Hall), dorsal view. 
 
958 
 
 GEOLOGY OP CANADA. 
 
 FOSSILS OF THE LOWER HELDERBERG GROUP. Continued. 
 458 
 
 458. Retzia multistriata (Hall) ; dorsal view. 
 459. Mcula naviformis (Conrad) ; left valve. 
 460. Loxonema compacta (Hall). 
 461. Platyceras ventricosum (Hall). 
 4S2.Holopea elegans (Hall). 
 
 4Q3.Eurypterus remipes (Dekay), as restored by Hall ; a, upper side, 
 and 6, under side ; from the water limestone. 
 
APPENDIX. 
 
 959 
 
 FOSSIL OF THE WATER LIMESTONE. 
 
 464 
 
 464. Eurypterus remipes (Dekay) ; specimen from Canada West, natural size. 
 
960 
 
 GEOLOGY OF CANADA 
 
 FOSSILS OF THE ORISKANY FORMATION. 
 465 b 
 
 465 a 
 
 465. Spirifera arenosa (Conrad); a, dorsal view; 6, cast of interior of 
 ventral valve. 
 
 466. S. arrecta (Hall) ; ventral view. 
 
 46 7. S. varicosa (Hall) ; dorsal view. 
 
APPENDIX. 961 
 
 FOSSILS OF THE ORISKANY FORMATION. Continued. 
 
 469 
 
 ed (Hall) ; cast of interior of ventral valve. 
 
 469. S magniventra (Hall) ; cast of interior of ventral valve. 
 
 470. Rensselcsria ovoides (Eaton) ; ventral valve. 
 
 L* 
 
962 
 
 GEOLOGY OF CANADA. 
 
 FOSSILS OP THE OKISKANY FORMATION. Continued. 
 
 471 a 
 
 471 c 
 
 4716 
 
 472 
 
 471. Rensselaria ovalis (Hall) ; a, ventral valve ; b, cast of interior of 
 
 ventral valve ; c, cast of interior of dorsal valve. 
 472. Platyostoma ventricosa (Conrad). 
 
APPENDIX. 
 
 963 
 
 FOSSILS OF THE POST-TERTIARY ; CHAMPLAIN CLAYS. 
 473 & 474 475 a 
 
 476 
 
 477 
 
 478 
 
 473. Rhynchonella psittacea (Linn.) ; a, dorsal, and 6, side view. 
 
 474. Mya truncata (Linn.) ; left valve. 
 
 475. M. arenaria (Linn.) ; left valve ; a, portion of the hinge. 
 
 476. Pecten Islandicus (Mullet) ; left valve. 
 
 477. Mytilus edulis (Linn) ; right valve. 
 
 478. Leda truncata (Gould) ; right valve. 
 
 479. JLstarte Laurentina (Lyell) ; left valve. 
 
964 
 
 GEOLOGY OF CANADA. 
 
 FOSSILS OF THE POST-TERTIARY; CHAMPLAIN CLA.YS. -Continued. 
 
 480 
 
 482 & 
 
 484 
 
 490 
 
 485 
 
 480. Tellind Grcenlandica (Beck) ; right valve 
 
 481. T. proximo, (Brown) ; right valve. 
 
 482. Saxicava rugosa (Linn.) ; left valve ; a and &, showing varieties. 
 
 Jrto 771 J.__ 1 x /"I IJx A rO AT*. 4 .*.*.. /"f 7 J_"^ u ,/ljr1' 
 
 483. Fusus tornatus (Gould). 
 
 484. Trophon scalariforme (Gould). 
 
 488.Natica Grcenlandica (Miill). 
 489. 2V. helicoid.es (Johnston). 
 
 485. Trichotropis borealis (Sowerby). 490. Scalaria Grcenlandica (Perry). 
 
 486. Buccinum undatum (Linn.). 491. Acm&a cceca (Miill.) ; a, &, diff. views. 
 
 487. Natica clausa (Sowerby). 492. Balanus Hameri (Ascanius). 
 
APPENDIX. 
 
 965 
 
 FOSSILS OF THE POST-TEETIAEY; CHAMPLAIN CLAYS. -Continued. 
 493 a 494 
 
 4936 
 
 493. Phoca Greenland (Miiller) ; a and 6, two views of the skull, 
 
 one third of the natural size. 
 4Q.~M(dlotus viUosus (Cuvier), natural size. 
 
966 
 
 GEOLOGY OF CANADA. 
 FOSSILS OF THE POST-TEBTTABY DEPOSITS. 
 
 496 
 
 Euelephas Jacksoni (Briggs and Foster) ; right ramus and sympbysis, 
 with a molar in place ; about one sixth of the natural size. 
 
 Upper side of symphysis of another individual, with the elevated 
 margins of the gutter broken away ; one third of the natural size. 
 Both of these specimens are from Hamilton. 
 
APPENDIX. 
 
 967 
 
 FOSSILS OF THE POST-TEETIAEr DEPOSITS. Continued. 
 497 
 
 497. Euelephas Jacksoni (Briggs and Foster) ; side view of the specimen 
 
 represented in Fig. 495. 
 498. Side view of the specimen represented in Fig. 496. 
 
INDEX OF SUBJECTS* 
 
 Page 
 
 Accumulation of sediments, 585 
 
 Acid springs, 352, 545, 556 
 
 Agates, 500, 831 
 
 Agalmatolite, 484, 602 
 
 Age of sediments, to fix,. 572 
 
 Algoma sand, 907 
 
 Alkalies, their relation to age of rocks, 572 
 
 Alkaline waters, * 532, 549, 557 
 
 Altered rocks, see Metamorphism. 
 
 " " Devonian,.,. 428,617 
 
 " " minerals of, 579 
 
 I " Quebec group, 597 
 
 1 " Upper Silurian, 428,617 
 
 Alumina, hydrates of, 578 
 
 " silicates of, 473, 577 
 
 Aluminous sediments, classification of, 576 
 
 Amphibolite, 649 
 
 Amygdaloids, 645, 651 
 
 " Huronlan, 58 
 
 " of Lake Superior, 71, 699 
 
 " Quebec group,.. 242, 607, 719 
 
 Analyses of soils, 636 
 
 " "waters, 547 
 
 Andalusite slates, see Chiastolite slates. 
 
 Anorthic feldspars, 477, 590 
 
 Anorthosites, Laurentian, .... 33, 588, 838 
 
 " Silurian, 250, 602 
 
 Anticosti group, 298, 310 
 
 " " in Gaspe", 309, 444 
 
 Antimony, native, 876 
 
 Apatite, beds of, ; 761 
 
 Argentiferous galena, 517 
 
 Argillaceous limestones, 805 
 
 Argillites, Huronian, 830 
 
 II Lower Silurian, 600 
 
 " Upper " 617 
 
 " for roofing slates, 830 
 
 " orthoclase in, 606 
 
 Artemisia gravel 908 
 
 Ashes of peat, analysis of, 642 
 
 Asphalt, 522, 790 
 
 " for pavements, 791 
 
 Page 
 
 Auriferous blende, 518 
 
 " drift, 929 
 
 " pyrites, 517 
 
 Azoic rocks of Arkansas, 66 
 
 " " Newfoundland, ..... 66, 8 78 
 
 " " the northwest, 65 
 
 Barytes, sulphate of, 458, 770 
 
 Basalt, 651 
 
 Basin of St. Lawrence, 1 
 
 Bayer and Stanbridge anticlinal, 238 
 
 Beluga, bones of, 919 
 
 Bigsby on Azoic rocks of the northwest, 65 
 
 Birdseye limestone, 137 
 
 Bitumens, 378, 521, 786 
 
 " alteration, products of, .... 524 
 
 " in corals, 524 
 
 " liquid, see Petroleum. 
 
 Mr. Wall on, 526 
 
 " origin of, 526 
 
 " solid, see Asphalt. 
 Bituminous shales,.. 380, 528, 622, 627, 785 
 
 ' M distillation of, 784 
 
 " " in Gaspe*, 445 
 
 f < " in Portage group, .. 387 
 
 " " in Utica formation,.. 199 
 
 Black-lead,-HBee Plumbago. 
 
 Black-River limestone, " 137 
 
 Blake, W. P., on gold washing, 743 
 
 Blende, auriferous, 518 
 
 Bog iron ores, 510, 682 
 
 Bonaventure formation, 404, 886 
 
 < " trap breccia of,.. 44T 
 
 " granites beneath, 452 
 
 Boulder formation, 893, 918 
 
 ageof, 92$ 
 
 Brick clays, 801 
 
 Bricks, white and red, 801 
 
 Brine springs, 563- 
 
 Buhrstone, 41, 808 
 
 Building stones, 810 
 
 Calc-spar for lime, 804 
 
 Calciferous formation, 110, 619, 879 
 
 * Under the head of MINERAL SPECIES, pages 973-975, will be found an alphabetical 
 list of the minerals noticed in this volume. 
 
970 
 
 GEOLOGY OF CANADA. 
 
 Page 
 
 Calciferous formation, wanting east, . . 119 
 " claystonein... 113 
 
 Canals of the St. Lawrence, 10 
 
 Cape Sante" anticlinal, 155 
 
 Carbonaceous shales, 623 
 
 Carbonate of soda in waters, 557 
 
 Carboniferous formation in Gasps', . . . 453 
 
 Carburetted hydrogen gas, 527 
 
 Cattskill group, 389 
 
 Caverns in Niagara limestone, . 334 
 
 Cement, hydraulic, 804 
 
 " magnesian, 757 
 
 " of Gaspe", 805 
 
 " Nepean, 806 
 
 11 " Oneida, 807 
 
 " " Quebec, 805 
 
 " " Thorold, 805 
 
 Chalcedony replacing fossils, 629 
 
 Chambly anticlinal, 140 
 
 Champlain clays, 915 
 
 Charcoal of peat, 775 
 
 Chateau Richer anticlinal, 159 
 
 Chazy formation, 123, 619, 854 
 
 " " Leperditia bed in, . . . 128 
 
 " " red limestones of, ... 131 
 
 " " sandstones,. .124, 167, 814 
 
 Chemical geology, principles of, 570 
 
 " manufactures, minerals used in, 745 
 
 Chemung group, 382, 387 
 
 Chert or hornstone, 500, 628 
 
 Chert of Corniferous formation, 366 
 
 " for millstones, 808 
 
 " fossils in, 629 
 
 " Huronian, 57 
 
 " of Lake Superior, 67 
 
 " origin of, 574 
 
 11 of Trenton group, 629 
 
 " veins of in syenite, 41 
 
 Chiastolite slates, 430, 617 
 
 Chloritic slates, 245, 606 
 
 Chrome in, various rocks, 504, 614 
 
 Chromic iron ore, 504, 749 
 
 " " formation of, 616 
 
 Chromiferous mica, 494 
 
 " garnet, 497 
 
 Church on silicification, 630 
 
 Cincinnati anticlinal, 363 
 
 Clinton formation, 312 
 
 Climactichnites, 107 
 
 Clays, analyses of, 641 
 
 " for bricks, 801 
 
 " earthenware, 802 
 
 Page 
 
 Clays, fire or refractory, 802 
 
 Clay, Champlain, 915 
 
 " Erie, 897 
 
 Clay, Leda, 915 
 
 " Saugeen, 897 
 
 Coal, Devonian in Gaspe", 394 
 
 " of New Brunswick, 452 
 
 " fields of North America, 18 
 
 " metamorphosed to graphite, . .529, 598 
 
 Cobalt, ores of, 506, 750 
 
 Cobaltiferous pyrites, 750 
 
 Columnar markings, see Crystallites. 
 
 Copper beds, 725 
 
 Copper deposits, origin of, 735 
 
 " mining in Canada, 735 
 
 " ancient, at Mamainse,.. 701 
 
 " smelting,; 736 
 
 " ores, 71, 514, 692, 843 
 
 Copperas, manufacture of 747 
 
 Coprolites, 461 
 
 Corniferous formation, 361, 627 
 
 " " petroleum of, . . 379 
 
 " " undulations in, 379 
 
 Crystallites in limestones and chert,. . 632 
 
 Crucibles, plumbago for, 793 
 
 Danville and Sutton anticlinal, 240 
 
 Daubre"e on metamorphism, 580, 584 
 
 Dawson on clays of Canada, 915 
 
 Deschambault anticlinal, 152, 272 
 
 Devonian coal in Gaspe", 394 
 
 " series in Canada, 359, 390 
 
 " " in Michigan, 388 
 
 " " in New York, 380, 389 
 
 " " thickness of, 389 
 
 Diallage rocks, 249, 469 
 
 Diabase, 649 
 
 Diluvium or drift, 887, 893, 895 
 
 Diorite, 649 
 
 " intrusive, 663 
 
 " " of Beloeil, 665 
 
 " " "Rigaud, 665 
 
 " " "Mt. Johnson, 664 
 
 " " " Yamaska, 663 
 
 " " for building, 812 
 
 " stratified, Huronian, 594 
 
 " " Silurian, ... 250, 602, 604 
 
 " " of Acton, 604, 713 
 
 " " " Lake Superior, ... 605 
 " "Newfoundland,... 875 
 " "St.Flavien,...242, 719 
 " Wendover,... 243, 719 
 Drift, auriferous, 929 
 
INDEX OF SUBJECTS. 
 
 971 
 
 Page 
 
 Drift, stratified, 887, 929 
 
 " unstratified, 893 
 
 Dolerite, 650 
 
 11 of Grenville, 653, 839 
 
 " " Montarville, 665 
 
 " "MountRoyal, 667 
 
 "Rougemont, 667 
 
 " olivenitic, 666 
 
 " marks of flow in, 72, 667 
 
 " various ages of, 653, 668 
 
 " for building, 812 
 
 Dolomite, 456 
 
 " of Calciferous formation, . . 619 
 
 " " Chazy .. 619 
 
 " Laurentian system, ..... 592 
 
 " Onondaga formation, . . . 625 
 
 " origin of, 575 
 
 " manganesian, 613 
 
 " of Niagara and Guelph, . . . 624 
 
 " " Quebec group, 243, 613 
 
 " " Trenton formation,.. 194, 623 
 
 " replacing fossils, 457, 620 
 
 li with excess of magnesia, 615, 623 
 
 Douglastown anticlinal, 399, 410 
 
 Dundas anticlinal, 329 
 
 Dunes, 905, 924 
 
 Dykes, dolerite, 37, 653, 839 
 
 Earthenware, clay for, 802 
 
 Earthy carbonates, origin of, 575 
 
 Economic minerals, 671 
 
 Eklogite, 651 
 
 Elephant, fossil, 966 
 
 Epidosite, 265, 497, 833 
 
 Epidotic rocks, 246, 255, 605 
 
 " gneiss, 37, 833 
 
 Epsomites, see Crystallites. 
 
 Erie clay, 897 
 
 Erratic blocks, , 893 
 
 Eruptive rocks, 643 
 
 Euphotide, 650 
 
 Eurypterus limestone, 353 
 
 Exotic rocks, 647 
 
 Feldspars, decomposition of, 570 
 
 " for porcelain, 801 
 
 " of crystalline rocks, 646 
 
 " trachytes, 662 
 
 " triclinic, see Anorthosites. 
 
 Feldspathic rocks, see Petrosilex. . . . 590 
 
 Fetid calcite, 455 
 
 Fishes, fossil, 916 
 
 Fire-brick, materials for, 800 
 
 Page 
 Fire-clay, 802 
 
 " origin of, 572 
 
 Flagstones, 827 
 
 Formations, parallel, 627 
 
 " nomenclature of, ........ 19 
 
 Fossils of drift, list of, 926- 
 
 " Lower Silurian, list of, 936 
 
 " Point L<vis, list of, 862 
 
 " replaced by dolomite, 457, 620 
 
 " silicified, 629 
 
 " supposed Laurentian, 49 
 
 Furnaces, sandstone for, 799 
 
 " soapstone " 796 
 
 Gabbro, 650 
 
 " rosso,.. 255 
 
 Galena, or lead ore, 516, 687 
 
 " formation, 623 
 
 Garnet, 496, 651 
 
 " rock, white, 496, 608 
 
 " " red, 588, 807 
 
 " " itsuse, 807 
 
 Gasps', Anticosti group in, 309, 444 
 
 " limestones, 390 
 
 " " contorted strata in, 392 
 
 " sandstones, 394 
 
 " " thickness of, 404 
 
 " series, 390, 453, 880 
 
 " discordances of, 442 
 
 " dykesin, 401 
 
 " " fossil conifer of, 399 
 
 " " gold in, 437 
 
 " " mineral veins in, 400, 437 
 
 Gems, 832 
 
 Genessee slates, 381 
 
 Geography, physical of Canada, 2 
 
 Geology, superficial, 886 
 
 Glacial grooves, 890, 918 
 
 11 origin of lakes, 889 
 
 drift, 892 
 
 Glass-making, stone for, 801 
 
 Glauconite, 227, 486 
 
 Gneiss, 587, 600 
 
 " for building, 812 
 
 Gold, 518, 730, 739 
 
 " extraction of, 740, 742 
 
 " in Gasp< series, 437 
 
 " in Nova Scotia, 745 
 
 " in pyrites, 517, 739 
 
 washings, 741 
 
 Grand River, gypsum of, 762 
 
 Granite, 647 
 
 Granites, age of certain, 452 
 
972 
 
 GEOLOGY OP CANADA. 
 
 Page 
 
 Granite for building, 810 
 
 " indigenous, 587, 600, 669 
 
 intrusive, Devonian, 430, 434, 669 
 
 " Huronian, 58 
 
 " probable origin of, 669 
 
 GraptoliteSj list of, 
 
 Gravel, Artemisia, 908 
 
 Great Britain, rocks of, 932, 934 
 
 Greenstone, see Diorite, ....... 649, 651 
 
 Green Mountains, 598 
 
 Green-sand, see Glauconite. 
 
 Grey-band sandstone, . . . . 310, 316 
 
 " " for building,.... 814 
 
 Grindstones, 809 
 
 Guelph formation, 336, 624 
 
 Gypsiferous formation, 345, 625 
 
 Gypsum beda, shape and structure, 347, 352 
 
 Gypsum, 459, 762 
 
 " origin of, 576 
 
 Haldimand anticlinal, 398, 882 
 
 Hamilton formation, 382 
 
 " " oil wells in, 386 
 
 " " resemblances of, . 627 
 
 Harvey-Hill mine, 256, 724 
 
 " " plan of, 726 
 
 Helderberg group, Lower, 353, 391 
 
 " Upper,.... 362 
 
 Highgate Springs, rocks of, 273, 855 
 
 Honestones, 809 
 
 Hopper-shaped casts in rocks,. . . .345, 625 
 
 Hornblende of crystalline rocks, 646 
 
 Hot water an agent in metamorphism, 584 
 Hudson River formation, .... 198, 224, 854 
 " " " limestones of, 200, 209 
 
 " " " red shales of, 203, 219 
 
 " " sandstones of, 200, 206, 815 
 " " " thickness of,.. 2 00, 207 
 
 Huronian series 50, 66, 841 
 
 " " general section of, ... 55 
 
 " " greenstones of, 57 
 
 " " on Lake Temiscaming, 336 
 
 " contact with Lauren tian, ... 64 
 
 " limestones 56, 596 
 
 Huronian rocks. 594 
 
 Hydraulic cement. 804 
 
 Hydraulic process of gold washing. . . T42 
 
 Hyperite, or hypersthenite 588, 650 
 
 Hypersthene 468, 588 
 
 Ice grooves, list of 890 
 
 Ilmenite 501, 589, 753 
 
 Indigenous rocks 647 
 
 Page 
 
 Infusorial earth, 930 
 
 Internal heat 585 
 
 Intrusive rocks 652-670 
 
 " " theory of 643 
 
 " " classification of 646 
 
 " " rare in altered regions . 585 
 
 Iowa, rocks of, 935 
 
 Iron oxyd, removal from sediments. . . 573 
 
 Iron ores 508, 596, 672 
 
 " " chromic, see Chrome. 
 
 " " graphite in 593 
 
 " " origin of 574 
 
 " " titanic, see Ilmenite. 
 
 " ochres \. 511, 767 
 
 Itabirite. 245, 615, 678 
 
 Jasper 423, 599, 628, 834 
 
 Kaolin of Vermont 801, 930 
 
 Kyanite 473, 652 
 
 Labradorite, see Anorthosite.. 478, 812, 833 
 
 Lake Superior, rocks of 67 
 
 Lakes, glacial origin of 889 
 
 " geological relations of the great, 1 7 
 
 " of Notre Dame Mountains 4 
 
 " "Laurentides 6, 11 
 
 " "the Ottawa 9 
 
 " " the St. Lawrence t 
 
 Land-slips 923 
 
 Laurentian system 22-49, 837, 878 
 
 " " conglomerates in, 31, 587 
 
 " " general section of . . 45 
 
 " intrusive rocks in, 37, 652 
 
 " " in Scotland 22 
 
 11 limestones 591,804 
 
 " rocks 586 
 
 " " supposed fossils of. . 49 
 
 Lauzon and Farnham synclinal 241 
 
 Lead ores 516, 687 
 
 " argentiferous 517, 738 
 
 Leda clay 915 
 
 Levels of the Great Lakes 713 
 
 " on Grand Trunk Railway 15 
 
 L^vis formation 227, 860 
 
 Lignite of Brandon 930 
 
 " Lake Superior 905, 906 
 
 Lime, stone for 803 
 
 " calc-spar for 804 
 
 " tufa for, 804 
 
 " magnesian 803 
 
 " hydraulic or water. 805 
 
 " carbonate, sources of. .......... 575 
 
INDEX OF SUBJECTS. 
 
 973 
 
 Page 
 
 Limestones for burning 803 
 
 " " building 815 
 
 " " marble 822 
 
 " copper-bearing 71 1, 713 
 
 " Huronian 596 
 
 " inorganic 631 
 
 " Laurentian. . 591, 804, 815, 83 
 
 " minerals of 59 
 
 " organic 63' 
 
 " Silurian 621,826 
 
 " two classes of. 63 
 
 Lingula, composition of 461 
 
 Lithology, principles of. 569, 643 
 
 Lithographic stone. , 83 
 
 Loraine shales 1 98 
 
 Lower Helderberg group 353, 391 
 
 Macadamizing, stone for .812, 821 
 
 Magnesia 756 
 
 " carbonate of, 457, 756 
 
 " " origin of.... 574 
 
 " for cement 757, 802 
 
 " silicates of..., 489 
 
 " " oiigin of. 577 
 
 " " clays 641 
 
 " " in shales 601 
 
 Magnesian limestone, see Dolomites. 
 
 " lime ,... 803 
 
 Manganese 507, 751 
 
 Marbles, 822 
 
 " serpentines, 823 
 
 Marl, fresh water 763 
 
 Mastic for pavements 790 
 
 Marcellus shales 380 
 
 Medina formation ; 310 
 
 " " in Lower Canada,.. 205 
 
 Melaphyre 651 
 
 Melbourne and Potton anticlinal 248 
 
 Metals and their ores 672 
 
 Metallic sulphurets, origin of 574 
 
 " deposite, theory of 699, 735 
 
 " veins, see Mineral veins. 
 
 Metamorphism, discussion of 569-586 
 
 " general 584 
 
 " local 430, 582, 634, 635 
 
 " natareand conditions of, 580 
 
 Metamorphic rockj. 586-618 
 
 " " of Cape Maquereau.. 272 
 
 " " " New Carlisle. ... 446 
 
 Mica 494, 795 
 
 Mica slates 433, 687, 600 
 
 " " for flagging 828 
 
 Middle Silurian rocks .......... . 298 
 
 Page 
 Middle Silurian escarpment. ... . .... . . 13 
 
 Millstones 807 
 
 MINERAL SPECIES 454-530 
 
 Acid, sulphuric 545, 556 
 
 Actinolite 466 
 
 Agalmatolite ... 482 
 
 Agate ... 500, 831 
 
 Albite 477 
 
 Allanite 505 
 
 Amalgam, see Mercury. 
 
 Amethyst 500, 832 
 
 Amianthus. 473 
 
 Amphibole 466 
 
 Analcime 481 
 
 Andalusite 499 
 
 Andesine '...... 478 
 
 Anhydrite 460 
 
 Anorthite 479 
 
 Anthracite , ,. 525 
 
 Antimony, native.. 876 
 
 11 glance 876 
 
 ." oxyd of 876 
 
 Apatit 460, 761 
 
 Aphrodite 473 
 
 Apophyllite. . , 482 
 
 Aragonite 455 
 
 Arsenical pyrites 505 
 
 Asbestus 473 
 
 Asphaltum 522, 524 
 
 Augite 467 
 
 Aventurine feldspar 475 
 
 Axinite 493 
 
 Baltimorite 473 
 
 Baryta, sulphate of 458, 770 
 
 Baryto-celestine, see Celestine. 
 
 Beryl 492 
 
 Bitter-spar 45$ 
 
 Bitumen 521, 785 
 
 Bituminous coal 528 
 
 Black-lead, see Graphite. 
 
 Blende 514, 702, 705, 708 
 
 Blue iron earth 770 
 
 Bog iron ore 510, 682 
 
 Bog manganese 507, 752 
 
 Brown hematite 510 
 
 Brown spar 508 
 
 Bytownite 479 
 
 Calcareous spar 454 
 
 Calcareous tufa 455, 804 
 
 Carbonate of lime 454 
 
 Celestine 459 
 
 Cerium 405 
 
 Chabasite..,...,, 431 
 
974 
 
 GEOLOGY OF CANADA. 
 
 Page 
 
 Chalcedony ...., 500 
 
 Chalcopyrite . .515, 692 
 
 Chert 600, 628 
 
 Chiastolite ..,.... 499 
 
 Chlorastrolite ... 481 
 
 Chlorite 488 
 
 Chloritoid , 498 
 
 Chondrodite . . . , 465 
 
 Chromic iron. 504, 748 
 
 Chrysolite , , 464 
 
 Chrysotile 473 
 
 Clintonite , . , 489 
 
 Coal 528 
 
 Cobalt, arseniate of. 505 
 
 Cobaltiferous pyrites 506, 750 
 
 Copper, native 615, 701-707, 720 
 
 " arsenical 506, 711 
 
 " grey 692 
 
 glance 692 
 
 " purple 692 
 
 " pyrites 692 
 
 " red oxyd of 515 
 
 u variegated , 692 
 
 " vitreous 692 
 
 " yellow 692 
 
 Coracite 504 
 
 Corundum 499 
 
 Diallage 469 
 
 Diopside 467 
 
 Dogtooth spar, see Calc-spar. 
 Dolomite, see Pearl-spar. 
 
 Dysyntribite 484 
 
 Elaeolite 480 
 
 Enargite 711 
 
 Epidote 497 
 
 Erubescite 692 
 
 Epsom salt 460 
 
 Feldspar 474 
 
 " Labrador 478 
 
 " potash 474 
 
 " soda 477 
 
 " lime 479 
 
 Fluor-spar , 463 
 
 Fuchsite 494 
 
 Galena 516, 687 
 
 Garnet 496, 807 
 
 " chrome 497 
 
 Gieseckite 482 
 
 Glauconite 486 
 
 Gold 518, 739 
 
 Graphite 529, 793 
 
 Green-sand, see Glauconite. 
 
 Gypsum 459, 762 
 
 Page 
 
 Heavy spar 458, 770 
 
 Hematite, red 509 
 
 " brown 510 
 
 Heulandite. 481 
 
 Hornblende 466 
 
 Hornstone 500 
 
 Hyacinth 499 
 
 Hypersthene 468 
 
 Idocrase 496 
 
 Ilmenite 501, 753 
 
 Jridosmine 520 
 
 Iron, carbonate of 508 
 
 " chromic. 504, 748 
 
 " magnetic 509, 672 
 
 " meteoric 508 
 
 " oxalate of 513 
 
 " peroxyd of 509, 677 
 
 " phosphate of 770 
 
 " silicate of 465 
 
 " specular 509, 677 
 
 " sulphuret of 513, 746 
 
 " titanic 501, 753 
 
 " tungstate of 503 
 
 Iron pyrites, cubic 513, 746 
 
 " " magnetic 514 
 
 Ironstone, clay 682 
 
 Jasper 500, 834 
 
 Kammererite 439 
 
 Kyanite 473 
 
 Labradorite, 473 
 
 Laumontite, 431 
 
 Lead, sulphuret of 616, 687 
 
 Lederite, see Sphene. 
 
 Lievrite 455 
 
 Lime, carbonate of 454 
 
 " fluate of, 463 
 
 11 phosphate of, 460, 761 
 
 " sulphate of 459, 762 
 
 Limonite, 510, 682 
 
 Loganite, 490 
 
 Loxoclase, 475 
 
 Macle, see Chiastolite, 499 
 
 Magnesia, carbonate of, 457, 756 
 
 " sulphate of, 460 
 
 Magnesite, 457 
 
 Magnetic iron ore, 509, 672 
 
 Magnetic pyrites 514 
 
 Malachite, , . 515 
 
 Manganese, oxyd of, 607, 751 
 
 Manganite, 751 
 
 Mercury, 513 
 
 Mica, 494, 795 
 
 " magnesian 494, 795 
 
INDEX OF SUBJECTS, 
 
 975 
 
 Page 
 
 Mineral resin 791 
 
 Mispickel 505 
 
 Molybdenum, sulphuret of, 503, 755 
 
 Mundic, see Iron pyrites. 
 Muscovite, see Mica. 
 
 Naphtha, 790 
 
 Natrolite, 48 1 
 
 Nepheline, 480 
 
 Nickel ores, 506, 614, 737 
 
 " arsenical, 506 
 
 Nickel-gymnite, " 
 
 " silicateof, 
 
 " sulphate of, " 
 
 " sulphuret of, 507, 738 
 
 Ochre, iron, 511, 767 
 
 Oil, mineral, see Bitumen. 
 Oligist, see Red hematite. 
 
 Oligoclase, 477 
 
 Olivine, 464 
 
 Orthoclase, 474 
 
 Ouwanwite, 497 
 
 Oxalite, 513 
 
 Pargasite 466 
 
 Parophite, 484 
 
 Pearl-spar, 456 
 
 Peridot, see Olivine. 
 Perthite, see Orthoclase. 
 
 Petalite, 481 
 
 Petroleum, 521, 785 
 
 Phlogopite, . 494 
 
 Pholerite, 495 
 
 Phyllite, see Chloritoid. 
 Picrolite, see Serpentine. 
 Pitch, mineral, see Asphalt. 
 Pitchblende, see Uranium. 
 
 Pitchstone, 704 
 
 Platinum, native, 520, 741 
 
 Plumbago, 529, 793 
 
 Prehnite, 481 
 
 Purple copper, 692 
 
 Pyrallolite, 479 
 
 Pyrites, arsenical, see Mispickel. 
 
 Pyrites, copper, 692 
 
 " cobaltiferous, 506, 750 
 
 " iron, 513 ; 745 
 
 " magnetic, 514 
 
 Pyrophyllite, . . 473 
 
 Pyrosclerite, 489 
 
 Pyroxene, 467 
 
 Quartz, 500, 729 
 
 Quicksilver, see Mercury. 
 Raphillite, see Hornblende. 
 Renssellaerite, see Pyralloite. 
 
 Pag* 
 
 Resin, mineral, 7&1 
 
 Retinalite, see Serpentine. 
 
 Rhodochrome, 489 
 
 Rock crystal, see Quartz. 
 Ruby, see Corundum. 
 
 Rutile, 502 
 
 Sapphire, see Corundum. 
 
 Saussurite, 650 
 
 Scapolite, 473 
 
 Schorl, see Tourmaline. 
 
 Scleretinite, 79-1 
 
 Sepiolite, 577 
 
 Serpentine, see Opbiolites, 
 
 Silex, see Quartz. 
 
 Silver, native, 51 7, 708, 738 
 
 " sulphuret of, 517 
 
 Soapstone, 469, 796 
 
 Soda, carbonate of, 557 
 
 " borate, 560 
 
 Sodalite, 430 
 
 Spathic iron, 508 
 
 Specular iron, 509 
 
 Sphene 502 
 
 Spinel, 499 
 
 Spodumene, 431 
 
 Stalactites, 334 
 
 Staurotide, 493 
 
 Strontia, sulphate of, 459 
 
 Sulphur, native, '. 530 
 
 Sulphuric acid, 545^ 555 
 
 Tabular spar, 455 
 
 Talc, 469 
 
 Tin ore in the United States, 734 
 
 Titanium, 501, 753 
 
 Tourmaline, 493 
 
 Travertine, see Gale-spar, 1 612 
 
 Tremolite, 466 
 
 Tufa, calcareous, see Gale-spar. 
 
 Tungstate of iron, 5QS 
 
 Uranium, 504 
 
 Variegated copper, 692 
 
 Vitreous copper, 692 
 
 Wad, see Manganese. 
 
 Wilsonite, 433 
 
 "Wolfram, 503 
 
 Wollastonite, 465 
 
 Yenite, see Lievrite. 
 
 Zeolites, 431 
 
 Zinc, blende, 514, 702, 705, 708 
 
 " sulphuret of, see Blende. 
 Zircon, 499 
 
 Minerals of altered rocks 579 
 
 " " limestones 591 
 
976 
 
 GEOLOGY OF CANADA. 
 
 Page 
 
 Mineral vein* . 37, 59, 74, 618, 636 
 
 " theory of 735 
 
 Mineral springs, 531-564 
 
 " analyses of, 547 
 
 " " chemistry of, 550 
 
 classification of, 531 
 
 " distribution of, . . 561 
 
 " list of, 532-547 
 
 origin of, 562 
 
 " temperatures of, ...... 564 
 
 Miocene deposits of Brandon, Vermont, 929 
 
 Mississagui anticlinal 62 
 
 Mississippi valley, rocks of, 935 
 
 Missouri, rocks of, 66, 935 
 
 Molybdenum, 503, 754 
 
 Montmorenci anticlinal, 157 
 
 Moraines, 895 
 
 Mountains, Adirondacks, 10 
 
 " Apallachian, 18 
 
 Green, 598 
 
 intrusive, 9 
 
 " Laurentides, 2, 4 
 
 Notre Dame, 3, 598 
 
 " Shickshock, . 598 
 
 Stoke, ....252,435 
 
 Rocky, 18 
 
 Nacreous slates, . . . . .1 601 
 
 Newfoundland, rocks of, 66, 288, 864 
 
 Niagara formation, 321, 624 
 
 Nickel and its ores, 506, 614, 737 
 
 Nomenclature, geological, 19 
 
 Northern Silurian basin, ^. 334 
 
 Norway, rocks of, Macfarlane on, .... 616 
 
 Nova Scotia, gold of, 745 
 
 Nucleus of the continent, 
 
 Obolella slates, 863 
 
 Oils from peat, 776 
 
 " from shales, 784 
 
 Oil wells, 523, 786 
 
 Olivenitic rocks, 652, 661 
 
 Oneida conglomerate, 31! 
 
 Oolitic limestone, 264, 63 
 
 Onondaga formation, 345, 62; 
 
 " limestone, 36 
 
 Ophiolites, 471, 64 
 
 " calcareous, . . 60 
 
 " conglomerate, 61 
 
 " dolomitic, . 60 
 
 " Huronian, 59 
 
 11 Laurentian, 59 
 
 " magnesitic,.. ............ 61 
 
 Page 
 
 phiolites of Newfoundland 875 
 
 " of Quebec group, . * 608 
 
 " of Syracuse, New York,.. . . 635 
 
 " stratified, of Mt. Albert, 266 
 
 riskany formation, 359 
 
 " " in Gaspe", 403 
 
 rnament, minerals for,' 831 
 
 rthoclase in argillite, 606 
 
 " " veins, 476 
 
 )rthophyre, 654 
 
 ttawa, waters of, 566 
 
 'aradoxides slates, 282, 879 
 
 'arallelism of formations, 627 
 
 'avements, asphalt for, 790 
 
 *eat, analyses of, 642 
 
 " ashes of, 642 
 
 11 charcoal from,.. 775 
 
 " distilling, 776 
 
 " localities of, 780 
 
 " oils from, 779 
 
 eninsula of Western Canada, 16 
 
 Pennsylvania, rocks of, 932, 935 
 
 'erce' anticlinal, 885 
 
 Peridotite, 666 
 
 Petroleum, ..217,403,521, 786 
 
 " refining of, 790 
 
 Petrosilex, t . 599 
 
 Phillipsburgh series, 844 
 
 ?hysical geography of Canada, 2 
 
 Phonolite, 648, 661 
 
 Phosphate of lime, see Apatite. 
 Phosphatic nodules and shells, . . . 125, 461 
 
 Pigments, minerals used as,. '. 763 
 
 Pitchstone, .-.- 648, 704 
 
 Plants, action of on sediments, 571 
 
 " fossil, of Gasp<, 394, 401 
 
 " post-tertiary, 917 
 
 Plumbago, 529, 793 
 
 Plumbaginous slates, 529, 623 
 
 Point Peter anticlinal, 883 
 
 Porcelain, clay for, 801 
 
 " apatite for, 758, 801 
 
 Post-tertiary deposits, 887 
 
 " fossils, 926, 963-967 
 
 Pottery, clay for, , . 801, 802 
 
 Potsdam formation, 87, 619 
 
 " " a shore deposit,... 109 
 
 " group, 283,851,879 
 
 " " at Belle Isle, ., 287 
 
 " sandstone...... 799 
 
 Porphyries, 72, 645, 654, 832 
 
 Pointe aux Trembles anticlinal, 155 
 
INDEX OF SUBJECTS. 
 
 977 
 
 Page 
 
 Protichnites, 102, 104 
 
 Province-line section, 279, 846 
 
 Pseudomorphism, 483 
 
 Pyrallolite, 470, 798 
 
 Pyroschists, see Bituminous shales. 
 
 Pyroxene of crystalline rocks, 646 
 
 Pyroxenite, 667 
 
 Quartz crystals in copper ore, 729 
 
 Quartzites, 594, 587, 598 
 
 Quartziferous porphyry, 654 
 
 Quicklime, stone for, 803 
 
 Quebec diamonds, 832 
 
 Quebec group, 225, 414, 420, 423, 427, 844 
 
 " " age of, 233 
 
 " " altered rocks of, 245, 597 
 
 " " a metalliferous formation, 236 
 
 " " distribution of, 709 
 
 " " extent of, 294 
 
 " " great dislocation of,.. .. 233 
 
 " " ideal section of, 296 
 
 " " on Lake Superior,.. 236, 698 
 " " lower shales of, 235,266,271 
 " " three chief folds of, 709 
 
 Radnor forges, 686 
 
 Rapids of St. Lawrence, 10, 207 
 
 Red sandrock of Vermont, 281 
 
 Red shales of Quebec group, 229, 600 
 
 " of Medina,... 203, 205, 219, 314 
 
 Red sandstones of Medina, 312, 319 
 
 Resin, mineral, 791 
 
 Refractory materials, 792 
 
 Ridges, gravel, 909, 911 
 
 Rigaud anticlinal, 174 
 
 Ripple-mark in sandstone, 107 
 
 Rocks, classification of, 645 
 
 " eruptive or intrusive, 643 
 
 " exotic, 647 
 
 " Huronian, 594 
 
 " indigenous, 647 
 
 " Laureutian, 586 
 
 " metamorphic, 569 
 
 " palaeozoic, eastern, 597 
 
 " " western, 618 
 
 " sedimentary, 569 
 
 Roofing slates, 830 
 
 Rounded rocks, 888 
 
 Saliferous formation, 345, 625 
 
 Salt group, Onondaga, 345 
 
 Salt springs, 563 
 
 Sand, Algoma, 907 
 
 Page 
 
 Sand, Saxicava, 915, 924 
 
 " lacustrine, 910 
 
 Sand for moulding, 800 
 
 " for glass, 800 
 
 Sandstone, Chazy, 814 
 
 " forbuildingj 813 
 
 " " flagging, 829 
 
 " " furnaces, 799 
 
 " glass, 800 
 
 " Oriskany, 815 
 
 " Potsdam, 813 
 
 " Sillery, 231, 598, 814 
 
 Saugeen clay, 897 
 
 Saussurite, 650 
 
 Saxicava sand, 915 
 
 Sediments, three classes of, 578 
 
 " elements in, 579 
 
 Sedimentary rocks, 569 
 
 " " action of water on,. 571 
 
 Sepiolite, origin of, 577 
 
 Serpentine, see Ophiolite, 471 
 
 " not an eruptive rock, 644 
 
 of Newfoundland,.... 293, 875 
 
 " marbles, 824 
 
 11 polishing of, 825 
 
 Serpulites, phosphatic nature of,.. 259, 462 
 
 Shickshock Mountains, 265, 598 
 
 Shipton and Leeds synclinal, 256 
 
 Sillery formation, 231, 598, 814, 880 
 
 Silica dissolved in waters, 568, 574 
 
 " deposits of, 574 
 
 Silicate of lime in waters, 559, 574 
 
 " " magnesia " 559, 577 
 
 " " alumina in waters, 57T 
 
 Silicified fossils, 629 
 
 Silicious infusoria, 930 
 
 Silico-aluminous rocks, origin of, .... 570 
 
 " " " classes of, 644 
 
 Silver and its ores, 517, 738 
 
 Soapstone, 796 
 
 Slates, Utica, see Utica formation. 
 
 " roofing, 830 
 
 " analyses of, 600 
 
 Shales, bituminous, 785 
 
 " Loraine, 198 
 
 Soils and clays, 636 
 
 " analyses of, 637 
 
 " " table of, 640 
 
 Specular schists, 245, 510, 615, 678 
 
 Spilite, 651 
 
 Si. Lawrence, waters of, 566 
 
 " basin, 2, 8 
 
 " and Ottawa plateau, ... 8 
 
 M* 
 
978 
 
 GEOLOGY OF CANADA. 
 
 Page 
 
 St. Maurice sands, 924 
 
 St. Armand and Shipton synclinal,. . . 245 
 Steatite, see Soapstone. 
 
 Stone paints, 7e7 
 
 Stoke Mountain synclinal, 251 
 
 Structure of crystalline rocks, 644 
 
 Stalactites, 334 
 
 Sutton Mountain, structure of, 251 
 
 Sulphate of barytes, see Barytes. 
 " lime, see Gypsum. 
 
 magnesia, 756 
 
 " iron, see Copperas. 
 
 Sulphuric acid springs, 545, 556 
 
 Sulphuric acid, manufacture of, 746 
 
 Sulphur, native, 530 
 
 Superphosphate of lime, 759 
 
 Superficial geology, 886 
 
 Syenite, 39, 647, 654, 811 
 
 " of Lake Temiscamang, 336 
 
 " for building, 811 
 
 Table of formations, 932 
 
 Table of geological series, 20 
 
 " superficial deposits, 886 
 
 " soil analyses, 640 
 
 " water " 547 
 
 Taconic system, 934 
 
 Talcose slates, 601 
 
 Tar Point anticlinal, 882 
 
 Tennessee, rocks of, 932, 935 
 
 Tentaculite limestone, 353 
 
 Terraces of western Canada, 910 
 
 " " Green Mountains, 929 
 
 Tertiary drift, pliocene, , . . . . 929 
 
 " miocene of Brandon, Vt 929 
 
 Theory of eruptive rocks, 643 
 
 Thermal waters, 564 
 
 Thessalon fault, 61 
 
 Titanium, see Ilmenite, 501, 753 
 
 " in iron ores, 681 
 
 " in rocks, 614 
 
 Trachytes, 207, 648, 656 
 
 " feldspars of, 662 
 
 11 granitoid, 656 
 
 Page 
 Trachytes of Vermont and New York, 663 
 
 " calcareous, , 658 
 
 " various ages of, 669 
 
 " for building, 812 
 
 Trap, greenstone, 649, 651 
 
 " amygdaloidal, see Amygdaloids. 
 " white, see Trachytes. 
 
 " columnar, 69, 72 
 
 11 marks of flow in, 72, 665, 667 
 
 " dykes, 38, 72, 143, 839 
 
 " breccia, 187, 447 
 
 Travertine, 455, 612 
 
 Triclinic feldspars, see Anorthosites. 
 
 Tufa, calcareous, for lime, 804 
 
 Trenton formation, 136 
 
 Trenton group, 136, 855 
 
 " limestone, 136, 620, 803 
 
 Upper Copper rocks of Lake Superior, 67 
 
 " " age of, 86 
 
 " Helderberg group, 362 
 
 " Silurian rocks, 345 
 
 " " " altered,.... 428, 616 
 
 Uranium, ores of, 504 
 
 Utica formation, 198, 621 
 
 Veins, granitic, 477, 644 
 
 " feldspar in, 476 
 
 " metalliferous, see Mineral veins. 
 
 Verd-antique marble, 825 
 
 Vermicular limerock of Eaton, 345 
 
 Vertebrate fossils,. 919 
 
 Vermont, tertiary of, 929 
 
 Waters of St. Lawrence, 566 
 
 " " Ottawa, 565 
 
 " mineral, see Mineral waters. 
 
 " chemical action of, 571 
 
 Water-lime, see Cement. 
 
 " " group, 352 
 
 White bricks, clay for, 801 
 
 Whetstones, 809 
 
 Wind-marks on sandstone, 107 
 
 Wood, fossil, 905, 906 
 
INDEX OF PLACES. 
 
 Page 
 
 Abercrombie, 833 
 
 Acton, 244, 604, 690, 713 
 
 Alfred, 532 
 
 Algoma, 
 
 Allumettes, 35, 125, 176, 462 
 
 Ancaster, 323, 329, 533, 682, 903 
 
 Anticosti, 220, 298, 766, 783, 820, 923 
 
 Argenteuil, 39 
 
 Arnprior, see Macnab. 
 
 Artemisia, ; . . 328, 804, 908 
 
 Ascot, 691, 732, 748 
 
 Assumption, 533, 781 
 
 Aylmer Lake, 429 
 
 Bachehwahnung Bay, 83, 700, 751 
 
 Balsam Lake, 190, 504 
 
 Barford, 433, 437, 734 
 
 Barrie, 823 
 
 Bastard, 31, 93, 639, 681, 683, 692, 822 
 
 Bathurst, 36, 833 
 
 Batiscan, 685 
 
 Battle Islands, 78 
 
 Bay du Febvre, 534, 562 
 
 " of Chaleurs, 446, 886 
 
 " St. Paul, 35,46,160,501,534,754,807,923 
 
 Beauharnois, 90, 102, 113, 813 
 
 Beaumont, 231 
 
 Beauport, 157, 819, 925 
 
 Bedford, 674, 687, 795, 849 
 
 Beloeil, 209, 664 
 
 Belmont, 676 
 
 Belle Isle, Strait of, 97, 287, 864 
 
 Belleville, 904 
 
 Bentinck, 342 
 
 Bertie, 354, 365, 368, 378, 552 
 
 Berthier, 534 
 
 Bic, 260 
 
 Black River (Lake Superior), 690, 694, 705 
 " " Mine, see St. Flavien. 
 
 Blythfield, 27, 31, 35 
 
 Bolton, 457, 749, 752, 756, 797, 799 
 
 Bonaventure Island, 404, 438 
 
 Page 
 
 Bonnechere, 175 
 
 Bonne Bay, 292, 865 
 
 Bosanquet, 382, 387, 627, 784 
 
 Bradore Bay, 287 
 
 Brampton, 535 
 
 Brant, 351, 535, 764, 821, 835, 899 
 
 Brantford, 349, 639, 762, 902 
 
 Breslau, 338 
 
 Bristol, 678 
 
 Brockville, 91 
 
 Brompton, 436, 831 
 
 Brome, 680 
 
 Brome Mountain, 239, 656 
 
 Broughton, 731, 799 
 
 Burgess, 692, 761, 771, 794, 796, 833 
 
 Bruce Mines, 694 
 
 Burlington Bay, 914 
 
 Cabot's Head, 319, 332, 912 
 
 Caledonia, 535, 562 
 
 Campement d'Ours, 84, 196 
 
 Cap de la Madeleine, 768 
 
 " Mahue, 833 
 
 Cape Gasps', 391 
 
 Hurd, 332, 344 
 
 " Maquereau, 272, 442 
 
 " Rosier, 269, 271 
 
 " Rouge, 201,231, 628 
 
 Sant<, 155, 203, 829 
 
 Carrick, 764 
 
 C as capedia Rivers, 411, 448 
 
 Caughnawaga, 131, 817, 826 
 
 Cayuga, 347, 355, 762 
 
 Caxton, 536 
 
 Chambly,.... 208, 209, 536, 638, 657, 782 
 
 Champlain, 536, 685 
 
 Charleston, 92 
 
 Charlesbourg, 157, 201 
 
 Charlotte ville, 539 
 
 Chatham, 38, 115, 794, 811 
 
 Chateau Richer, 34, 46, 159, 589 
 
 Chatte River, 262, 264, 410 
 
980 
 
 GEOLOGY OF CANADA 
 
 Page 
 
 Chaudiere River, 42 7 
 
 Chertsey, 34, 44, 589 
 
 Chester, 723 
 
 Chevrotiere, 154, 819 
 
 Chippawa, 347, 540 
 
 Clarence, 169 
 
 Clarendon, 31 
 
 Clinton, 324 
 
 Cleveland, 606, 723, 830 
 
 Cornwall, 126, 172, 816, 827 
 
 Collingwood,..193, 211, 315, 784, 814,911 
 
 Couchiching, 191 
 
 Cow Head, 877 
 
 Cumberland, 169, 780 
 
 Dartmouth River, 406, 880 
 
 Deschaillons, 921 
 
 Deschambault, 152, 154 
 
 Doree River, 53, 694 
 
 Douglastown River, 407, 789, 883 
 
 Dudswell, 431, 617, 827, 828 
 
 Dummer, 36, 189 
 
 Dumfries, 338 
 
 Dundas, 313, 325, 802, 903, 914 
 
 Dunham, 287 
 
 Drummondville, 243, 603, 718 
 
 Eboulemens, 162 
 
 Echo Lake. 696 
 
 Ellis Bay ( Anticosti), 300, 308 
 
 Elmsley, 460, 761 
 
 Elora, 340 
 
 Enniskillen, 386, 786, 901 
 
 Escott, 675, 693 
 
 Esquesing, 327, 815 
 
 Elizabethtown, 747, 750, 816 
 
 Famine River, 428, 739 
 
 Farnham, 239 
 
 Flamborough West, 313, 325 
 
 Fergus, 341 
 
 Fitzroy, 537, 689 
 
 Fox Bay (Anticosti), 308 
 
 Frampton, , 257 
 
 Gait, 339, 895 
 
 Garthby, 733, 748 
 
 Gaspe", 3, 309, 391, 691, 791 
 
 Gaspe" Bay, 396, 402, 437, 734 
 
 Gargantua, 82, 702 
 
 Gloucester, 168, 537, 916 
 
 Goderich, 376, 894 
 
 Page 
 
 Goulais River, 905 
 
 Granby, 245, 614, 712 
 
 Grand Calumet, 48 
 
 Great Metis River, 416 
 
 Great Pond (GaspS), 270 
 
 Green Island, 684 
 
 Grenville, .. .35, 38, 40, 113, 652, 673, 794 
 796, 798, 808, 811, 824, 832, 839 
 
 Griffin Cove, 270 
 
 Grondines, 154, 202 
 
 Guelph, 331, 337, 820 
 
 Halifax, 724 
 
 Hallowell, 537 
 
 Ham, 253, 254, 733, 749 
 
 Hamilton, 312, 323, 538, 815 
 
 Harvey Hill, see Leeds. 
 
 Hawke's Bay, 291, 877 
 
 Hawkesbury, 124, 171, 538, 814 
 
 Henryville, 538 
 
 Hemmingford, 88, 829 
 
 Hespeler, 340 
 
 High Falls (Madawaska), 29 
 
 Highgate Springs (Vermont), . . . .273, 855 
 
 Hull, 129, 673 
 
 Hungerford, 180 
 
 Huntley, 117, 128, 780 
 
 Huntingdon, 32 
 
 Industry, 133, 148, 685, 819 
 
 Inverness, 681, 724 
 
 Ireland, 254, 724 
 
 Isle Bizard, 357 
 
 " Perrot, 91 
 
 " Royal, 79 
 
 Jacques C artier River, 155, 538 
 
 Joly, 539 
 
 Jones's Tract, 354 
 
 Junction Cliff (Anticosti), 224, 298 
 
 Kamanistiquia River, 63, 68, 708 
 
 Kincardine, 374, 522 
 
 Kingston, 178, 539, 632, 806, 816, 904 
 
 Kingsey, 830 
 
 Labrador, 46, 924 
 
 Lachine, 659 
 
 Lachute, 94, 115 
 
 Lacloche, 84, 194 
 
 Lanoraie, 539, 693, 781 
 
 Lansdowne, 92, 688, 771 
 
INDEX OF PLACES. 
 
 981 
 
 Page 
 
 Lauzon, 241 
 
 Laval, 800, 925 
 
 Leeds, 257, 498, 677, 724, 755, 767 
 
 London, 641, 903, 913 
 
 L'Orignal, 130, 827 
 
 Loughborough, 99, 179, 764, 794 
 
 Lyn, 813 
 
 Macnab, 677, 765, 823 
 
 Macomang Lake, 841 
 
 Madawaska River (Gaspe), 419, 425 
 
 Madoc, 32, 675, 809, 822 
 
 Magdalen River, 268, 407, 805, 922 
 
 Maitland. Ill 
 
 Malbay (Gasp6), 885, 922 
 
 Maiden, 378, 821 
 
 Mamainse, ....83, 690, 700 
 
 Manicougan Bay, 755 
 
 Manitoulin Islands, 194, 216, 320, 333 
 
 Marmora, 181, 186, 675, 822, 834 
 
 Maskanongi (Lake Huron), 697 
 
 Maskinonge' (Ottawa), 
 
 Marsouin River, 267 
 
 Matapedia -River and Lake, 415 
 
 Matanne 413, 922 
 
 Meaford, 911 
 
 Megantic Lake, 431 
 
 Memphremagog Lake, ..251, 432, 435, 809 
 
 828, 929 
 
 Metis, 261, 921 
 
 Metis Lakes, 41 
 
 Melbourne, 722, 749, 824, 830 
 
 Mica Bay, 702 
 
 Michipicoten Island, 81, 703, 737 
 
 " Bay, 703 
 
 Mille lies, 44 
 
 Milton, 244, 712 
 
 Mingan Islands, 119, 134, 164, 287, 826,924 
 
 Missisquoi Bay, 276 
 
 Missisagui River, 62, 697, 841, 906 
 
 Monnoir, Mount Johnson. 
 
 Montarville, 634, 665 
 
 Montmorenci, 158, 201 
 
 Montreal Island, 114, 125, 131, 136,141, 144 
 207, 357, 639, 659, 766, 803, 817, 827, 918 
 
 Mont Calvaire, 91 
 
 Morin, 33, 44, 838 
 
 Mount Albert, 266, 749, 825 
 
 " Healy, 348, 762 
 
 " Johnson, 664 
 
 " Royal, 142, 667 
 
 " Serpentine, 293, 881 
 
 Mount Wissick, 420 
 
 Murray Bay, 96, 162, 819, 922 
 
 Naquareau River, 148 
 
 'Jassagaweya, 327 
 
 Neepigon Bay, 79 
 
 Nelson, 719 
 
 Nepean, 94, 129, 780, 806, 813 
 
 New Carlisle, 446, 766 
 
 New Glasgow, 839 
 
 Newfoundland, 66, 288, 864 
 
 Niagara, 540, 641 
 
 Niagara Falls 321, 820, 913 
 
 " River, 312 
 
 Nicolet, 540, 562 
 
 11 River, 205 
 
 Nipissing, 678, 908 
 
 Norman Cove, 872 
 
 Normanby, 351, 900 
 
 Normandale, 683 
 
 North Cayuga, 360, 366 
 
 Nottawasaga, 317, 910 
 
 Oneida, 348, 3GO, 807 
 
 Orford, 249, 599, 603, 609, 731, 738, 825, 830 
 
 Orleans Island, 200, 225, 234, 487 
 
 Ottawa City, 165, 765, 817 
 
 Otter Head, f04 
 
 Owen Sound,.. 214, 318, 329, 770, 821, 898 
 
 912 
 Oxford, 787 
 
 Pakenham, 175, 521, 827, 924 
 
 Palladeau Islands, 195 
 
 Paquette's Rapids, 176 
 
 Paris, 350, 763 
 
 Patapedia River, 417 
 
 Pembroke, 125, 814 
 
 Perce", 438 
 
 Perth, 93, 107 
 
 Petewahweh, 930 
 
 Petite Nation, 837, 794 
 
 Phillipsburgh, 275, 820, 844 
 
 Pic Island, 80 
 
 Pike River, 542, 835 
 
 Pistolet Bay, 874 
 
 Pittsburg, , 799 
 
 Plantagenet, 170, 541 
 
 Point Douglas, 373, 807 
 
 Pointe aux Mines, 82, 702 
 
 " Claire, 140,817 
 
 " aux Trembles, 155, 819 
 
 N* 
 
982 
 
 GEOLOGY OF CANADA. 
 
 Page 
 
 Pointe du Lac, 769 
 
 Point Boucher, 215 
 
 " L<vis, 230, 232, 487, 860 
 
 " Porphyry, 707 
 
 " Rich, 215 
 
 " Daniel, 443, 771, 785 
 
 " Dover, 367, 633 
 
 Portage du Fort, 822 
 
 Portneuf, 153 
 
 Potton, 248, 250, 607, 691, 730, 797 
 
 Prescott, Ill 
 
 Prince's Mine, 707 
 
 Puslinch, 337 
 
 Quebec, 201, 230, 541, 721, 805 
 
 Radnor, 686 
 
 Raleigh, 639 
 
 Ramsay, 688, 798 
 
 Rawdon, 34, 44, 541, 589, 82 
 
 Restigouche, 449 
 
 Rigaud, 91, 112, 116, 641, 658, 665, 896, 917 
 
 Rimouski, 261, 893 
 
 " River, 418, 783 
 
 Riviere Ouelle, . . . .259, 462, 541, 783, 834 
 " duLoup (Beauce),.. 428, 740, 828 
 
 " " (en 6as), 258,921 
 
 Rockwood, 330, 82 1 
 
 Root River, 697 
 
 Ross, 36, 461 
 
 Rougemont, 634, 667 
 
 Rouge River (Ottawa), 36, 43, 917 
 
 " (Gasps'), 416 
 
 Roxton, 718 
 
 Russell, 173 
 
 Sabrevois," 541, 562 
 
 Saguenay River, 923 
 
 Saugeen River, 35, 899 
 
 Schooner Island, 873 
 
 Seneca, 349, 762 
 
 Seven Islands, 46, 96 
 
 Seymour, 676 
 
 Sherbrooke, 252, 732, 834 
 
 Sherrington, 642, 782 
 
 Shefford, 239, 657, 721 
 
 Shipton, 253, 799, 811 
 
 Shickshock Mountains, 265 
 
 Sillery, 231, 814 
 
 Silver Brook, , 789 
 
 Simcoe Lake, 193 
 
 Simpson's Island, 707 
 
 Slate Islands, 705 
 
 Tagc 
 
 Somerset, 242, 719 
 
 Snake Islands, 195 
 
 Sorel, 925 
 
 South Crosby, 31, 674 
 
 South Sherbrooke, 674 
 
 South Ham, 876 
 
 Spanish River, 696 
 
 Stanbridge, 683, 848, 852 
 
 Stanstead, 434, 752, 767, 810 
 
 Stoke Mountains, 252, 435 
 
 Storrington, 97, 177, 829 
 
 Stukley, 722 
 
 Sutton, 247, 251, 457, 677, 679, 721, 797, 828 
 
 Swanton, 280, 856 
 
 St. Alban's, 857 
 
 Ste. Anne de Montmorenci, 160, 198,511, 768 
 
 " de la Pocatiere, 542, 562, 639 
 
 " deMonts, 921 
 
 St. Ambroise, 96, 156 
 
 " Armand, 679, 690, 766, 826, 850 
 
 " Barbe's Bay, 871 
 
 " Benoit, 542 
 
 " Catharines, 543, 902 
 
 " Charles, 638 
 
 " Dominique, 205, 638, 642, 783, 820, 826 
 
 " Flavien, 241, 719 
 
 " Francis, see Vaudreuil (Beauce). 
 
 " Lake, 429 
 
 Genevieve, 544 
 
 Giles, 257, 730 
 
 Gregoire, 205 
 
 Helen's Island, 207, 356, 626 
 
 Henry, 599, 601, 720 
 
 Hilaire, 206 
 
 Hyacinth, 209, 544, 638 
 
 Ignace Island, 72, 706 
 
 " Jean (Port Joli), 639 
 
 " Jerome, 33, 781, 807, 838 
 
 " John (Dorchester), 140 
 
 " " Lake (Saguenay),... 46, 164, 220 
 
 " Joseph (Beauce), 255,731,825, 826 
 
 " Island, 196, 217 
 
 Le"on, 544 
 
 Lin, 133, 145, 818, 826 
 
 Margaret, . . . . , 730 
 
 Maurice, 95, 152, 204, 685, 782, 799, 814 
 
 Mary (Blanchard), 377, 821 
 
 11 River, 84, 906 
 
 " (Beauce), 601, 730, 752 
 
 " Nicholas, 203,241,484, 921 
 
 Ours, '544 
 
 " Paul's Bay, see Bay St. Paul. 
 
 Rosalie, 620, 603 
 
INDEX OP PLACES. 
 
 983 
 
 Page 
 
 St. Roque, 146, 461 
 
 " Scholastique, 95 
 
 " Thomas, 639 
 
 " Urbain, see Bay St. Paul. 
 
 Vallier, 684 
 
 Table Head, 869 
 
 Tadousac, 804 
 
 Tar Point, 396, 789 
 
 Temiscamang, 50, 334, 828 
 
 Temiscouata, 259, 419 
 
 Terrace Bay, 706 
 
 Terrebonne, 34, 148, 818 
 
 Thessalon Eiver, 55, 841, 907 
 
 Thorold, 313, 322, 806 
 
 Thunder Bay, 63, 67, 70, 77, 707, 771 
 
 Tilsonburg, . 787 
 
 Toronto, 903, 915 
 
 Tracadigash, 449 
 
 Trent River, 187 
 
 Trois Pistoles, 260 
 
 Tuscarora, 545 
 
 Page 
 Upton, 244, 604, 690, 712 
 
 Vaudreuil, 90, 683, 770, 813 
 
 Vaudreuil(Beauce),254,427, 603, 739, 754 
 
 798 
 
 Walkerton, 899 
 
 Wallace Mine, 695, 737 
 
 Walloostook River, 426 
 
 Wellington Mine, 695 
 
 Wentworth, 39, 673, 824, 840 
 
 Wendover, 718 
 
 Whitby, 189, 547 
 
 Wickham, 718 
 
 Widder, 385 
 
 Woodst^|^ 371 
 
 Westbury^ 831 
 
 Yamaska Mountain, 657, 663 
 
 " River, 209 
 
 York, 348, 762 
 
 River, 408, 789, 792, 882, 922 
 
RETURN EARTH SCIENCES LIBRARY 
 
 TO ^ 230 McCone Hall 642-2997 
 
 LOAN PERIOD 1 
 1 MONTH 
 
 2 
 
 3 
 
 4 
 
 5 
 
 6 
 
 ALL BOOKS MAY BE RECALLED AFTER 7 DAYS 
 
 Books needed for class reserve are subject to immediate recall 
 
 DUE AS STAMPED BELOW 
 
 FORM NO. DD8 
 
 UNIVERSITY OF CALIFORNIA, BERKELEY 
 BERKELEY, CA 94720 
 
LEV LIBRARIES 
 
: iV--. n