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Tous les autres exemplaires originaux sont film6s en commenpant par la premiere page qui comporte une empreinte d'impression ou d'illustration et en terminant par la derni^re page qui comporte une telle empreinte. Un des symboles suivants apparaTtra sur la dernidre image de cheque microfiche, selon le cas: le symbole — ► signifie "A SUIVRE ", le symboie V signifie "FIN". Les cartes, planches, tableaux, etc., peuvent dtre film6s d des taux de r6duction diffirents. Lorsque le document est trop grand pour dtre reproduit en un seul cliche, il est film6 d partir de I'angle sup6rieur gauche, de gauche d droite. et de haut en bas, en prenant le nombre d'images n6cessaire. Les diagrammes suivants illustrent la mdthode. rrata to pelure. □ 32X 1 2 3 1 2 3 4 5 6 I X < < s ■a (« s J3 G] G. M. o 5"^ :^ c -^ ?: ^^ O -; ^ X '^ -3 3 a 8 a S u 3 a 3 X H GE( a o u GEOLOGICAL SURVEY OF CANADA G. M. DAWSON, C.M.G., LL.D., F.R.S., Dibectoh REPORT ON THE GEOLOGY AND NATURAL RESOURCES OF THK AREA INCLUDE') HY TlIK NIPISSM AND TEMISCAffllNG mmm coMpniaiNf; i'ortions of the DISTRICT or NIPISSmG, ONTilRiO, AIID OF THE COUNTY OF PONTIAC, OUEBIC BY ALFRED ERNEST BARLOW, M.A. i I OTTAWA PRINTED BY S. E. DAWSON, PRINTER TO THE QUEEN'S MOST EXCELLENT MAJESTY 1899 No. 672. ' ' ' II ToG: Sill featur Nipiss Nipiss accoiu] constit series c % flue to litholog of man} critical for aid ( the dist Survey, Palfeozoi Ackno l>ee.ston, power to Norris, o Stephen places or ] V^. E., engi: of the Car of Toronto of the ioca informatio in the vicij f ing, Ontario, ami the county of Potitiac, Quebec, lying between lati- '''"•^''"^^t- tudes 4G' llV '2\" and 47' 3()' 47 " north, and extending from longitude 78° 49' o4" to longitude 80' 22' 20 " west of (ireenwich. This area is comprised in the two maps accompanying the ivport, known as the Nipissing and Temiscaming sheets, or Nos. 1131 and 138 respectively, of the Ontario series of geological maps, on a scale or four miles to one inch. The district which each map represents, measures seventy-two .\,,:i aiid miles in length from east to west, and forty-eight miles from north to •"""''* "f south, thus eml)racing an area of 34r)6 s()uare miles, or a combined area of 0912 square miles. The Nipissing sheet includes nearly the whole of Lake Nipissing and considerable portions of Dikes Tema- gami, Temiscaming and Keepawa, the boundary between the two sheets cutting the three last-named lakes about latitude 46' 55'. The main line of the Canadian Pacirtc Railway traverses the southern part |{;uiw,ivn. of the Nipissing sheet, the eastern limit crossing the railway between Calvin and Eau Claire stations, while the western boundary is sii/Uated a short distance west of Warren station. The town of North Bay is the most populous and important place, and is one of the divisional points on the Canadian Pacific Railway, as well as the '■ini«i;liHii present terminus of the Northern division of the Grand Trunk Rail- ,, i n/ i ^ ... drniul I milk way, although the actual intersection of the two lines is at Nipissing Kailway. Junction, three miles south-east of North Bay. The Grand Trunk m ♦j I MPISSINQ AM) TKMIHCAMIXd KKOION. lANlOW AreiiH ill <.)ueb<'t; aiiorti(jn of Lake Temiscaming has, in general, a north -and-.soutli direction, while the township boundaries and side-lines of Gendreau and other town- ships situated in the southern part of Lake Temiscaming, have a direc- tion of N. 60° E. or at right angles to the general trend of the lake in this vicinity, which is thirty degrees east of south. The distance be- tween concession-lines is slightly over a mile, but the lots themselves are much narrower than those on the Ontario side, each being designed to contain about 100 acres, although in many instances this area is much diminished or increased. The concessions are denoted by the Roman numerals, while the ordinary figures are applied to the lots. Occasionally, both in Ontario and Quebec, the letters of the alphabet have been used to designate the concessions. The preliminary part of the work in this district was done in 1887- Wi>rl< '>f'gun 88, while acting under instructions from Dr. R. Bell, as his assistant ; in ih«7. but only about two months of each season were devoted to this work, and by far the greater portion of this time was occupied in some of the many detailed surveys necessary in a region concerning which but little had hitherto been known. This topographical survey was, of course, accompanied by as many observations regarding the nature and distribution of the various rock formations encountered as was possible in a survey of the kind. The more pre.ssing nature of the work in connection with the Sud- ^^ '""''^ ""* bury mining district, caused my removal from this held to assist Dr. Bell in tracing out the geological and topographical details necessary for the map and report concerning that region, which has already appeared, so that work was not resumed on the Nipissing and Temiscaming sheets till 1892. The bulk of the work on these two maps was accom- plished between 1892 and 1894, although about two months of the season of 1895 was required to complete it. It was found necessary to make a large number of topographical surveys, especially in the I 1 1 i> m 1 \l i-ii 1 ■/ 1 .;i:^l '1 1 8 I NIIM8SINO AND TKMI8CAMINr. ItKRION. Mothixt of Hurvey. Work cdnimoiiccd. KeasoiiH for I'oinplct ed in 1HH7. Survtys ill 1888. Surveys in 1802-95. northern part of the district, and this portion of the work occupied hy far tho 8 hitherto published. The distancen were measured with a Rochon micrometer telescope, while the direction was determined by prismatic compass. The dis- tances thus obtained from point to point, were further utilized as bases for a compass triangulation, by which the position of many of the smaller islands and some of the more conspicuous points on the main- land otherwise inaccessible were defined with sulHcient accuracy. About the middle of .luly, 1887, aj,'reeably with instructions received from Dr. Bell, then in charge of the work in the district of Nipissing, r proceeded from Ijake Temiscaming by way of the Matabitcliouan River and Rabbit Lake to Temagami Lake, in order to complete a de- tailed topographical and geological survey of that lake. This survey was commenced on July '23rfl. The work was considerably retarded owing to the frequent presence of smoke caused by the unusually large number of l)ush fires, and many days this smoke was so dense as to render all attempts at surveying quite useless. Another cause which militated very greatly against the rapid and successful prosecution of the work during this and succeeding seasons, was the difficulty in procur- ing and retaining the services of suitabh? canoemen. In spite of these drawbacks, how«'ver, the survey of Temagami Lake was finished by September 15th, when a similar survey was undertaken of the route by way of White-bear and Rabbit lakes and the Matabitchouan River to Lake Temiscaming. During the summer of 1888, these surveys were continued, but .scarcely two months of the season were devoted to field operations in this region. During this time, however, consider- able progress was made in the topographical measurements of many of the principal lakes, among the more important of which may be men- tioned, Cross Lake, the northern part of Obabica Lake, route from the north arm of Lake Temagami, by way of Red-squ-'^rel and Annima Nipissing Lakes to Bay Lake on the Montreal River, as well as of many minor sheets of water to the north and north-east of Temagami Lake. In 1892, the survey and examination of the Nipissing district was resumed, with instructions from the Director to make whatever surveys were deemed necessary for maps, and a report of an approximately final character. An epitomized statement of the general progress of the work has been given each year, in which mention is also made of the various topographical surveys accomplished each season, in the four •1 RAHI.V KXPLORATIONH AND PIIFVIOUS HHUVEVS. 9 I Suininnry Itoports of 181)2 to 189').* During 1892 and 180;{, I wiia Ax-i^tMiit^. ably aHsiuted by Mr. J. K. K. .Johnston, upon whom devolvod the fjreatflr part of the topo},'rapliical work done during these two years. In 18.SS, mid again in 189;{ and 1891, I wa.s accompanied hj .Mr. A. M. Campbell, of Perth. During the .seiuson of 189.S 1 hr.d likewise the advantage of the assistance of Mr. K. M. Hurwa.sli, of Victoria University, Toronto. For cartographical purposes, tlie various bitse, meridian and township Sources of lines run by the Crown Lands De|)artments of Ontario and Quebec 5'^',f,'Jji^j|!v'ti|*,, have been utilized, and servo as excellent checks and corrections to the errors necessarily incident to a micrometer and compass survey. The geographical features of the area covered by the .surveyed town- ships have, in the main, been adoptei], supplemented, however, in many cases by additions and corrections of our own, wiiich were sometii\iea found neces.sary. This information was chietly availal)le in the area of the Nipissifig sheet, where over half tlie area has been divided ' 'o town- ships, and these in turn subdivided into conce.ssions ind lots. sides these a luimber of surveys of a more general character h i\ > been made, the maimscripts and published plans of whid. have been found of much aissistance in the general compilation, as well as iu furnishing details !i many cases not otherwise obtainable. "niong SurvtyH l>.v the more important of these plans, the following may be iiicniioned : V|If,""y"' Murni. .survey of Lake Nipissing and the 8turgecn River, and Logan's survey of the Mattawa River, published in the folio atlas to accompany the Report of this Survey of ISoiJ-nG. Murray's survey of Lake Nipissing, however, did not show sutiicient detail in the western portion of the lake, so that a resurvey was carried out early in 1892. Austen's map of the Temagami River, with accompanying traverses made for the purpose of ascertaining the most feasible route for the location of a transcontinental railway line, h'orrest's survey of the l". uroHt'H Montreal River was found excellent for all purposes for which it was required. Messrs. O'Dwyer and O'Hanly's survey of the Ottawa oDwytr'sixnd River and Lake Temiscaming, to delineate the boundary line between j^'irvl-vs^ ^ Ontario and Quebec, was found to be thoroughly reliable, while the Canadian Pacific Railway surveys enabled us to locate the exact <'iiniiosMl canal. CJhaiiiiilaiii': journey in 1012. Nicolas du Vignau. The sheltered nature of its water-stretches, its comparative freedom from molestation, as well as its directness as a route to tlie great lakes and bsyond, formed powerful inducements in favour of the original selection of the Ottawa and Nipi.ssing route, at a time when the birch- bark canoe was the chief and often the only method of communication. The advent of steamboat navigation on tho St. Lawrence River and the great lakes, however, as well as the building of the St. liawrence canals, have during the present century caused this route to fall into comparative disuse. The recently revived proposal to make use of these water-courses for purpo.ses of modern navigation by the building of canals to overcome the obstructing rapids, seems likely again to bring this district into prominence. Soon after his arrival in this counti-y, Samuel de Champlain, who was by nature more of an explorer and adventurer than a builder of colonies, determined on an examination of the head-waters of the Ottawa and beyond. He was all the more eager to undertake this investigation as a young man, Nicolas du Vignau, had just returned, in 1612, after a year's absence among the Ottawa Indians, with a most wonderful tale. He claimed, during his absence, to have discovered a passage by way of the Upper Ottawa to the shores of a northern sea, to whicli he had penetrated, and there beheld the wreck of an English ship. The apparent clearness and consistency of the story deceived Champlain, KARLY EXI'LOHATIONB AND PUEVIOUS SURVEYS. 11 I who fancied that he might thus find tlie much coveted road to China and Japan. Towards the end of May, 1613, Champlain, accompanied by ciiamplain's this Du Vignau, ascended the Ottawa as far as Lake Coulonge, where ""^'^ "'" he was reluctantly dissuaded by the resident natives from proceeding further. They urged, as their main excuse for not seeming willing to guide him, the many insuperable difficulties to be encountered on the route, as well as the reputed fierceness and witchcraft of the Nipiss- ing IndianS; through whose country it was necessary to pass. Here also he learned that tiie whole story of Du Vignau's pretended discoveries was a fabrication, and that far from undertaking any such important journey as reported, h^s had resided continuously and (juietly at the village during the entire period of his absence from civilization. This information, which was subsequently corroborated by Du Vignau's own tardy confession, enraged and disheartened Champlain, who, convinced of the fruitlessness of any further effort at the time in this direction, returned to Montreal, and subsequently to France. Early in 1615, however, Champlain returned to Canada, bringing ciuvniplain's with him four Recollets, one of whom Father Joseph Le Caron, was •■^l'|<>''ations destined for missionary work among the Huron Indians. Arriving at Arrival at Montreal, he found a large concourse of Indians already assembled, who Mi'iifeal. had come hither from their homes in the vicinity of Lake Simcoe. These savages, always more eager for temporal than spiritual help, again pressed Champlain to aid them against their hereditary foe, the formidable Iroquois Deeming it expedient at the time to comply with this oft-repealed reijuest, Champlain hurriedly descended to Quebec to make the necessary preparations, leaving Le Caron and some of his compatriots with the assembled Indians to await his return. During Champlain's absence, however, the Indians decided to go back forth- with to their ov/n home without him, and accompanied by Le Caron and his associates commenced the ascent of the Ottawa River. When Champlain returned to Montreal and found the place deserted, he Ui^coviry of immediately hurried after them, pursuing the usual course up the \i,ii!!gi,i„ j,„rt Ottawa and Mattawa rivers, over the height-of-land to Lake Nipiss- Huron, ing and tlience down the French River to Lake Huron. Champlain was thus the first European, with the exception of the humble friar who had only just preceded him by a few days, to gaze on the waters of Lake Huron, which ho christened " Mer Douce." J ■ f . lU Champlain's map of New France, which was made in 1632, included ciiampliun's all sketches and surveys from 1603 to 1629. Only th<; main routes ot ""*''• travel are represented, while the whole map exhibits, in a very rough manner, the salient physical features encountered during the progress 12 I NIPISSINO AND TEMISCAMINf} RErilON. Exploratiiiii clfist'ly con- nected with fiirtradp. of theso journeys and explorations. Lake Nipissing is called "Lac de Biserinis " while a rude outline of the Ottawa River ahove its confluence with the Mattawa is given, that must have been drawn from infor- mation supplied by the Indians. The exploration of this district, as of others elsewhere through- out Canada, is inseparably bound up with the history of the fur-trade, the successful prosecution and extension of which required the constant addition of new territory. We thus find that many of the first ex- ploratory expeditions wero often undertaken by adventurers at their own expense, with the promise of various marks of distinction from those in authority in cjuse of the success of their undertakings, while fur-trading licenses were granted to enable these men to indemnify themselves for their pecuniary outlay. Delisles iii!i|p '^he limits of this traffic were quickly extended both northward and andiKwitioiM.f westward, and we find by reference to Delisle's map (1703) that the Fort des ^ ■'^ _ _ , , . Abitibis. French then had a post (Fort des Abitibis) north of the height of-land on the river Abitibi. This post, according to the memorial of Begon* was the most advanced station of the Fnnch toward Hudson Bay. From this same memorial, it also appears certain that the route north- ward by way of Lake Temiscaming and the Abitibi River (Monsony or Monsipy) was one of the best known, although the French traders avoided the immediate vicinity of Hudson Bay in order not to expose themselves to the insults of the Indians who were friendly to and traded with the English posts already established in that vicinity. It Exiwditidiis to does not seem unreasonable to suppose, therefore, that some of the ex- peditions despatched by the Governors of Cancada towaril the close of the 17th century, to take possession of Hudson Bay, adopted this well known route by way of the Upper Ottawa and Abitibi rivers. All the earlier maps indicate many of the streams flowing northward from the height-of-land into James Bay with tolerable accuracy, thus showing that the early voyageurs were well acquainted with this portion of the country. Hiidaon l>!iy towards tlic closfi of ITtli century. Fort Teiiiiscii niini< early e8tai)lisli('d. Fort Temiscaming must have been one of the first posts established by the Northwest Company, if not acijuired after its abandonment by the French, for Mr. Roderic Mackenzie, a clerk in this company who wrote" A General History of the Fur Trade,' which forms the opening chapter of Sir Alexander Mackenzie's Travels in North America says : *Menioire de Eegon, Oct. 20 1725, qui expli(iue lea anciennes lin'ites du poste de TeniiscaminiTue. fVoyajjes from Montreal throufirh the Continent of North America to the Frozen and I'acific Oceans in the years 1789 and 1703. London, 1801. p. xxxiv. •J KAHLY EXPLORATIONS AND PKEVIOl'S SURVKYS. 13 I " Lake Teiniscaniing wliero there has always been a trading post " Miuki'ii/ic's while one of the buildings which had lieen used as a store-house and "'^'' *" which was removed only a few years ago, bore dates on the large cedar beams wliicli pointed to its erection some time near the close of last century. Fort Temiscaming afterwards became the liead-quarters of the Utadquintirs Hudson's Bay Company in tliis district, containing the residence of the j'j jj (^•^^ Chief Factor and all the necessary adjuncts in the shape of buildings, etc., which usually go to make up a well equipped establishment, form- ing one of the most impui-tont centres of the fur trade and containing besides a library embracing many volumes on science, travels and gen- eral literature. In 1888, however, this post, so long established, was iJ'inovnl abandoned, and a small store was erected at "The Point" near the ' village of Baie des Pisres, which was found more convenient for purposes of general trading ; while the opening,' up (»f the Canadian Pacific Rail- way had previously caused tile removal of the iiead-tiuarters to Mattawa. Temagami post, now situated on the west side of Bear Island !"»♦'• until the opening of the railway, when it gradually* fell into disuse and was finally abandoned altogether about the year 1890. Hunters HnntetK Lodge, originally a trading establishment, situated on Hunters ''"''^"'■ Narrows in Keepawa Lake, was abandoned about the same time. At several points on the Ottawa River and the lower portions of Lake Temiscaming, temporary posts were erected from time to time, but these were of no permanent importance, and when the reasons which brought tiiem into existence disappeared, they were given up and forgotten. Buildings originally erected in 1887, and designed for i5ayi,Mi<|.,,(ist. storage purposes on liay Lake, an expansion of the Montreal River, have i iif ! ( i i" ? ; i^i. 14 I MPISSINfJ AM) TKMI.SCAMING REGIOX. Lon^ Point. Decrt fnr-trafle. nst' III since been raised to the dignity of a post with an ofticer in charge. At present, in the area of the accouipanying map-sheet.s, there are only three cstahlishment.s, Temaganii, Bay Lake and Long Point (on «' Quinze Lake "), which receive any gi eat quantity of fur.s, although a considerable number of skins come in casually to the posts at Mattawa and Baie des Peres during each year. Of these Temaganii is the most important, but the gradual opening up of considerable areas in this district to settlement, and the diminution in point of number both of the fur-bearing animals and the Indians who are chiefly engaged in their capture, is already having a marked effect, showing a gradual, or in some cases a rapid decrease in the number of skins annually brought to market. The opening chapters ot ]Mackenzie's narrativf, previously mentioned, give a lirief description of the route generally pursued by the fur- trading canoes in gaining access to the various forts and trading posts of the inteiior. The i-apids and portages of the Mattawa are enum- erated, the names in most cases being the same as those in use at the present time, although the river itself is here called Petite Riviere. Nepisingui (Nipissing) Lake is also mentioned, and a short account given of the Riviere de.s Francois.* The first geological account of the Work liy I )r. region in question was that of Dr. J. J. Bigsby, who had come to ill IS-.'o. Canada as medical officer to a regiment. About the yeai- 1820, he received an appoirtment from the Colonial Government to make a generid report on the geology of Upper Canada, the absurdly small sum of twenty-six pounds, as he informs us, being granted as pecuni- ary aid to carry out this extensive undertaking. Dr. Bigsby lirst made an examination of the Ottawa, Mattawa and French rivers, to- gether with Lake Nipissing, having been granted a free passage to Sault Ste. Marie in one of the Northwest Company's canoes. He gives a good account of the Ottawa River itself and of the country adjoin- ing this stream, and mentions that the Mattawa River, which was the western branch of the Ottawa, often called the Little Ottawa, was known as the Tessouac River by the Indians. The occurrence of crystalline limestones at the Talon Chute is noticed, among other inter- esting facts. The position of " La Itonde," a Northwest Company's post, is noted as being situated at the mouth of the Vase River, as well as its subsequent removal to one of the islands in Lake Nipissing. t Cry-iriiiliiii' lilllCStKllCH Mt Talon Cluit)'. nia>fiieti( During the pR)gress of the magnetic survey of British North America, executed between 1842-1844 by Sir J. H. Lefroy, various * See |i]i. xxxiv. anil xxx\. MackMi/.ie'M Voyages. t Shoe and Canoe, vol. 1. London, 1850. pp. 105 to 171. formations •] EAHLY KXPLORATIONS AND I'KEVIOUS SUfiVEYS. l.-) I observations were taken in this rej^ion to ascertain tlie magnetic varia- tion, 'vhile latitudes were obtained at the following places : Hudson's Bay Company's post Mattawa, First portage on Little (Mattawa) River, Lake Teinisiquc (Lower Trout Lake); Lake do Talon or Lake Walrond ; Trout Lake, formerly called Lake de Grande Vase ; Height-of-land portage, towards Lake Nipissing ; and Cross Point on the south shore of Lake Nipissing, where a cross had V)een erected to commemorate some fatal accident.* For many years the region in the vicinity of the Upper Ottawa U|i|"r<)tt!i\v;i IT • 1 1 1 • 1 ^ II "listrict Kiver was comparatively unknown, except to the occasional traveller ,,,niiia',ai\fly and missionary, and to those engaged in the fur-trade, whose business "'"^""">'- necessitated constant journeying to and fro along the main canoe- routes. Tn time, however, the almost inexhaustii)le supply of valualjle timlier known to exist in this district, attracted the attention of the enterprising lumberman, wlu)se operations were so ((uickly extended IjuniiHiii!.,' north-wc'sLward that, by the year 1 friYi>hi(ivl five miles above the "des Joachim " liapids. As this was the highest at Heniu'tt point yot reached in the topographical delineation of the course of the BnK.k. Ottawa, it was decided to make this the starting point of the contem- plated survey of the upper portion of this stream. The distances were determined by the Rochon micrometer telescope, while the bearings and angles of intersection wore obtained by means of a theodolite. The diflFerences in level of the river at all the rapids were ascertained by careful levelling with a proper instrument and stall', the fall in the intervening stretches being estimated from a knowledge of the strength of the current. This survey was continued up the Ottawa as far as the first chute on the llivii-re des Quin/.e, a short distance above the head of Lake Temiscaniing. During the same season, and as a necessary adjunct, a similar survey was undertaken of the Mattawa River, from its junction with the Ottawa to its head-waters in Trout Lake, including also the portage-route by way of the Riviere de la Vase to Lake Nipissing, as well as a small portion of the shore-line of this lake in the vicinity of the mouth of this inlet. Observations for latitude were obtained at the starting point, the mouth of the Mat- tawa, the mouth of the Vase on Lake Nipissing, as well as at the mouth of the Keepawa on Lake Temiscaniing. In fact, every precaution was taken to make this survey as accurate as was possible with the instruments and time at his disposal. The various topographical details, delineated in a map subsequently compiled by Sir William Logan himself on a scale bearing valuable notes regarding the encountered, is at present on file at this office, and although not issued as a separate publication, the information has been made use of in every subsecjuent map covering the district. Survey to i.^uiiizf KivtT. Survey of .Matt;nv;i Kiv.T. I>(i0iilitifs (1 .ili>;t'r\:itiiiu fi»l- livtitiidf Miip l.y Murniy'^ sur\cvs \n ISairiC. SI of one various mile to an inch, rock formations A portion of the Ottawa River in the neighbourhood of the Mattawa, as well as the whole of this latter sti-eam, were, however, incorporated in the atlas to accompany the report by Mr. Alexander Muriay (1853-56). During the summer and autumn of 1854, Mr. Alexander Murray, of this Survey, was engaged in making exploratory surveys to the east of Lake Huron and Georgian Bay. These included a survey of the southern shore of Lake Nipissing, from the point where the French River measurement ceased in 1847, to the mouth of the Vase, where connection was made with Sir William Logan's survey of 1845, and thence of the north shore, of this sheet of water toils "north- west angle."* In 1855, Mr. Murray continued this survey, commenc- • Report of ProgreeB, Geol. Surv. Can., 1853-56, p. 101 et seq. 11 EARLY EXPLORATIONS AND PREVIOUS SURVEYS. 17 I Surveys i>f Luke. ing at the outlet of Lake Nipissing into the French River, along the western coast making connection with the work of the previous year.* In 1856 this survey was again extended, this time a start being made from the Hudson's Bay Company's Post on Sturgeon River near Lake Nipissing. Ascending the Sturgeon River for about fifty-two miles to the moutli of the Maskinonge, the measurements were carried up this important branch through Murray, Washkigamog, Maskinong^-wagaming and Mattagamashing lakes to Wahnapitae Lake, and down the Wahna pitae RivT to Lake Huron.f In 1855, Duncan Sinclair made a survey of Keepawa Lake, with a view of defining and locating certain timV)er limits. This survey, although excellent for the purpose for which it was undertaken, never- theless lacked certain details essential for a correct elujidation of the geological features, thus necessitating a re-survey v/hich was accom- plished by Mr. J. F. E. Johnston, of this Department Acting under instructions from the Commissioner of Public Works, Canal surveys. Mr. M'^alter Shanly, C.E.J in 1856-57 made » ueiailed examination of the route contemplated for a canal to connect the waters of the St. Lawrence with those of the Great Lakes by way of the Ottawa, Mattawa and French rivers, and Lake Nipissing. In 1858-59, another examination of the same route was made by Mr. T. C. Clarke, C.E.,^ also in accordance with instructions received from the Commissioners of Public Works. In 1867, Mr. A. G. Forrest, acting under instructions from Forrest's the Crown Lands Department of Ontario, made a survey with transit «»""^';y "f and chain of the Montreal River, starting from its intersection with a Kivcr. due west astronomical line, supposed to be run on the parallel of latitude of 47°56', between Michipicoten Harbour on Lake Superior and the head-waters of the Montreal River. This astronomical line was started about the same time from its eastern and western extremities. Mr. Duncan Sinclair who was entrusted with the eastern portion of the line succeeded in running a distance of 105 miles from the Montreal River, while Messrs. A. P. Slater and R. Gilmour, ran eighty- ; i t- ' 'I u t .Vstronoiiiical line. *ReiK)rt of Progress, Oeol. Surv. Can., 1853-56 pp. 128 and 135 et seq. +Report of Progress, Oeol. Siirv. Can., 1853-.56, pp. 146 et sef). JRejwrt of Walter Shanly, Esq., On the Ottawa Survey,— Toronto. March 22nd, 1858. Also Report on the Ottawa and French River Navigation I'roject, — published by order of the Montreal Board of Trade, 1803. § Return of Recent Survey and Report of the Engineer on the Ottawa Ship Canal Quebec, 1860 by Thos. C. Clarke, C.E. 2 :i'!. 18 I NIPI88ING AND TEMI8CAMINO REGION. ForrestV work. fiiii HP I" Traverse liy Lindsay RUHS€!11. Surveys tiiulcr Mr. Rowan. Work by W. McOuat. Survf^y of four miles eastward from Michipicoten Harbour. Mr. Forrest, from the intersection with Sinclair's line made an instrumental traverse of the Montreal River to its mouth on Lake Temiscaming, a distance of one hundred and one and a quarter miles, at the same time taking notes on the timher and other natural resources of the country extending for three miles on either side of the stream. These surveys, commenced in 1866, were completed in 1867. Their primary object seems to have been to determine the feasibility of the construction of either a wagon road or railway to the Red River country through the district in question.* About the same lime (June 13th to August 16th, 1867), Mr. Lind- say Russell, made a micrometer traverse of Lac des Quinze and the Upper Ottawa, connecting with H. C. Symmes' survey of Grand Lake. Mr. Russell during the same sei.son made a similar survey of the route to Lake Abitibi, as well as a traverse of this large sheet of lake, then for the first time correctly measured.! In 1871, Mr. Alexander McKenzie, acting under instructicms from Mr. James H. Rowan, who hud charge of the Canadian Pacilic Rail- way surveys from the Mattawa to the Red River, made a track-survey northward by the Ottawa and Abitibi rivers to James Bay, returning by way of the Moo.se and Michipicoten rivers to Lake Superior. J In 1871-72, Messrs. Lloyd, O'Hanly and Austen, also under Mr. Rowan's instructions, made exploratory surveys from Mattawa by way of the Ottawa and Montreal rivers to a point about half-way between this latter stream and one of the branches of Moose River. § In 1872, Mr. Walter McOuat of this Survey was engaged in a geological examination of that portion of the country to the north and east of Lake Temiscaming. The work performed by Mr. McOuat in the Temiscaming region embraced a most painstaking geological exam- ination of Rivifere des Quinze, Lac des Quinze and the route thence northward to Lake Abitibi, including a micrometer survey of the shores and islands of that lake. He also made a micrometer traverse of BlanclieKiver. (;j,p Blanche River as far as Round Lake, accompanied by an examina- *See Remarks, on Upper Can.ada surveys, 1867 ]>]>. 6<)-02. tSee Reix)rt Cominissioner of Crown Lands, (juel)ec, 18G8, p. XVII, also descrip- tions of the Surveyed Townshiiis and Territories of the province of Quebec, 1889, pp. 416-424. +See Progress Retwrt on Surveys Canadian Pacific Railway, 1872 p. 74. Also Report on Surveys Canadian Pacific Railway, 1877, pp. 5-47 and 48. § See Progress Rejwrt on Canadian Pacific Exploratory Surveys, 1872. These surveys comprised Divisions B, C and D, re8i)ectively, mentioned in these reports. The surveys were begun on June 10th, 1871, and the last of them was completed by July, 1872. See also Report on Surveys, Canadian I'aei fie Railway, 1877, pp. 5 and 47. tion to ac conta embn 2^ •AMIOW ] EARLY EXPLORATIONS AND PREVIOUS 8DRVET8. 19 I tion of the rocks in the immediate vicinity of this stream.* The plans to accompany his report have never been published, but the information contained has been utilized in subsequent general geological maps embracing this area. In 1872-74, Messrs. O'Hanly and O'Dwyer, joint commissioners for l'n>vincial ^ . , -, , , . J ' ■) lioundary Ontario and Quebec, made an instrumental traverse of the Ottawa siirvcy. from Mattawa to the head of Lake Tomiscaming, and .surveyed a line running northward from a point on the " Chenail du Diable," near the mouth of the Riviere des Quinze as far as the height-of-land.t During the year 187G, in connection with the location of the Canadian ^ • •'• H. 8UrV6V9 Pacific Railway, Mr. Marcus Smith, then acting engineer-in-chief, made an examination of the eastern portion of Lake Nipissing, as well as of the " Beuve" (Veuve) River as far as the forks, about twenty- five miles from the mouth. t In 1879, Mr. W. A. Austen, for the Canadian Pacific Railway, ran a trial location survey from a point situated a short distance (404 feet) east of the deep-water landing at South-east Bay (or East Ray) of Lake Nipissing, in a north-easterly direction for sixty-three miles up the valley of the Sturgeon River.g As a part of the same survey, Mr. Austen made a micrometer survey of the Temagami River, the southern portions of Cross and Temagami lakes as well as the route from thence to Maskinong^-wagaming Lake, by way of Obabica and Wawiagama lakes. During the summer of 1884, commencing in June, Mr. T. Guerin, Gnerin's engineer of the Public Works Department, Ottawa, undertook an ' examination of the Ottawa River and Lake Temiscaming with a view to ascertaining the feasibility, at a reasonable cost, of the various schemes urged on the Government from time to time, looking to an increased facility in the navigation of these waters.|| In the summer of 1884, Dr. Selwyn, during the progress of an Work by examination of the numerous rock-cuts exposed along the line of the l)r. Selwyn, •Report of Progress, Geol. Surv. Can., 1872-1873 pp. 112 et seq. t The manuscript plan of a scale or 40 chains to one inch beari; the date, Dec. 27th, 1875, while the joint report filed vvitii the Crown Lands Department, is dated Ottawa, Dec. 7th, 1874. + Report Canadian I'acific Railway, 1877, pp. 359-3()(). § Appendix 18, "Reiwrt Canadian Pacific Railway, 1880, pp. 290-296." A plan on 4000 feet to an inch, detailing these explorations, as also two jirofiles of the Sturgeon River are on file at the Deiiartment of Railways and Canals, Ottawa, and have been of much assistance in the compilation of the accompanying maps. i Ann. Rep. Minister of Public Works, 1884-85, pp. 103-124. 2\ 20 I NIPISSINr. AND TEUI8CAMINO REOIOK. KossIIh. \i: :i Kxaiiiiiiatioii by Prof. C. K. (JillHi-t. Prof. Wright'; observatiun.-i. F. H. Taylor's observations. Canadian Pacitic Railway, paid a visit to the Manitou Islands in Lake Nipissing, and the Ii.st of the fossils then collected from the Canibro- Silurian outliers comprising seventeen specie.s, together with a few notes regarding their occurrence was published by Dr. H. M. Ami*. The Rev. J. M. Goodwillie, who was stationed at North Bay for some years, has made an extensive collection of the fossil remains from these islands, and these have now been examined and their identification has greatly iulded to the list appended to this report. Mr. Ulrich determined a small collection of fossils for Professor N. H. Winchell, which were collected by Mr. T. D. Ledyard, of Toronto.! In 1889, Prof. N. H. Winchell paid a visit to North Bay, and gives a record of his observations made in that vicinity. | In 1889 Mr. G. K. Gilbert made an examination of the vicinity of North Bay and the country eastward-^ towards Mattawa, with a view to obtaining any evidence regarding the former existence of T.n out- let for the Great Lakes, immediately following the retirement of the ice-sheet. The possibility and even the probability of the existence of .such an outlet had been looked upon for some time with favour by .some geologists, although facts in support of these views were not forthcoming previous to the communication made by Mr. G. K. Gilbert to the meeting of the American Association for the Advancement of Science, held in Toronto in August, 1889. The general sub.stance of the remarks then made were published under the title of "The History of the Niagara River. "§ In Soptemlier, 1892, Prof. G. F. Wright visited the neighbourhood of North Baj- and Mattawa, making certain observations seemingly confirmatory of the former existence in the Mattawa valley of this outlet, and embodying the results of his observations in a paper entitled, "The Supposed Post-glacial Outlet of the Great Lakes through Lake Nipissing and the Mattawa River." || In the autumn of 1893, Mr. F. B. Taylor made some observtvtions in regard to the occurrence of beaches in the vicinity of North Bay, and their relations to this supposed old outlet of the Great Lakes. * Can. Rec. Science, April, 18f)2, pp. 108 ot seq. + American fJeologist, vol. XVIII., No. 3, September, 1896, p. 178. + EiRliteenth Annual Report, Geol. and Nat. Hist. Survey, Minnesota, 1889, p. 501. § Sixth Annual RejHjrt of the Commissioner.s of the State Re.servation at Niagara for 1889, pi>. (il-84, and reprinted in the Smithsonian Report for 1890, pp_ 231-2.57. i Bull. Geol. Sec. Am., vol. IV., 1893, with discuasion by Dr. Robert Bell, pp. 423-42(>. •' •ARkOW J OENEKAL PHYSICAL FEATURES. 21 I The results then obtained were communicated to the (Jeologioal Society of America, and published in the bulletin of that society.* In 1895, another visit was paid to the Nipissing District with the similar object of gaining additional information in regard to the recent changes of level, t In 189(5, a third visit was paid to the region in tlie neighbourhood of the Mattawa and Ottawa rivers, and the results then obtained were communicated to the Geological Socifty of America. In 1890, William Ogilvie, acting under instructions from the Depart- I,;ititu(l« und ment of the Interior, Ottawa, fixed the latitude and longitude of ^I';^naw'll! ' Mattawa, the latter by telegraph from Ottawa. In 1892, Messrs. H. K. Wicksteed and Patterson, under the direc- Siirve>;8()f tion cf Mr. J. C. Bailey, C.E., of Toronto, made the location ,'i.i„'iesi5(iyRy, survey of the Nipissing and James Bay Railway from North Bay to the North east Arm of Lake Temagami. INIr. Patterson had charge of the location of the southern portion of the line from North Bay to Marten Lake, and Mr. Wicksteed of the northern pare. The building of the Temiscaming branch of the Canadian Pacific Surveys by M. Railway and the surveys and levels made in connection therewith, have been used in the present map and report, the information being kindly supplied by Mr. M. H. McLeod, the engineer-in-charge. General Pliysical Features. The generial character of the country may perhaps be best described (jentral as that of an uneven or undulating ro^ky plateau, with a gentle slope t'luiracter of towards the east and south-east. Although in detail the surface of this plateau is far from uniform, consisting of a succession of more or less parallel rocky ridges, with intervening valleys occupied by swamps or lakes, still the district as a whole has a general elevation varying from 900 to 1200 feet above the sea. There are no very prominent hills, the highest seldom attaining a greater altitude than 300 feet above the surrounding region, while throughout most of the district, hills of 50 to 100 feet in height are rather conspicuous topo- graphical features. The highest land in the whole area is situated near the north-west corner of the Temiscaming sheet, immediately to * Bull. Geol. Soc. Am., vol. V., pp. ()20-(J26 with two maps, also American Geologist, vol. XIV., Nov., 1894, pp. 282-285. t Ihid, vcV XVIII, August, 1806, pp. 108-120. a 22 I NIFISSINO AND TEMI8CAMINO HEfllON. the west of Lady Evelyn (Mus-ka-na-ning) Lake, where a range of hills of which Maple Mountain is the highest peak, i-Ihch to tht; height of a little over 2000 feet above the sea, according to Dr. Bell. [nflutmcf of The influence exerted by the underlying rook on the general con- iiiulo'i-lying . , 1.11 -1 rockonMuifucc tour ot tlio surface, is perhaps nowhere better exemphned tlian in the contour. region embraced in this report. In the southern imd south-eastern portions, where the prevailing rocks are the various gneisses and granites included as Laurentian, there are no hills of any great height, the general surface presenting, as usual, a rather monotonous succes- sion of low rounded hills, with correspondingly shallow rocky valleys. In the northern and wistnrn portions, however, tho.so arous in which the ([uartzites iire present, as well as those in which the plutonic rocks, chietly granite and diabase, are prevalent, rise into rather important elevations ; while in those regions which are underlain by the slaty member of the Huronian, are on the other hand low and flat. A remarkable resemblance exi.sts between the contour of the surface, occasioned by the presence of the diabasic rocks, and that jiroduced by the heavy-bedded and massive quartzite, that forms the highest member of the Huronian exposed in this district, both rising into compatatnely high rounded or broken ridges, and rendering the stretches of country where such rocks prevail, exceedingly rough and hilly. This is especially the case with the region to the north and north-west of Wakemika and Lady Evelyn lakes, and also between Friday and Whitebear lakes and the Montreal River ; although the whole of the area coloured on the map as underlain by those rocks partakes essentially of this rugged character. This rough and broken contour is in marked contrast to the flat surface cliaracteiistic of the region in which the slates obtain. The contrast is probably nowhere better shown than in the north- eastern part of Lady Evelyn Lake, where the quartzite which crosses the lake at the Obisaga Narrows forms high and perpendicular cliflFs for a short distance, while to the east, as far as the Waswaning Nar- rows, the shore on both sides is low and swampy, with only a very occasional exposure of the flat-lying slaty rocks. At the elbow to the east of the Waswaning Narrows, a high ridge of diabase crosses the lake, forming rugged hills which constitute the western side of that portion of the lake known as the Mattawapika. Thus within a few miles, on the same lake, are exhibited examples of all three types of surface produced by the underlying quartzite, slate and diabase. Character of The large area coloured as granite, to the north-east of Lake Tema- granite areas, gami, may perhaps be best described as a region of flooded roches Examples of differing tojwgraijhy. hollow lakes o and Ml united Pro!) sented the ()M rooky which surface indicate sion, th below t lake, wl gray un before t mouth o vail, but expansio face of tl usually an asce country i hills are i The M Sturgeon depressioi The d is known as The Ottav Mattawa i panying n the confin( by far the maps. Tli 3000 squa square rail Otter-tail i smaller tha of considei included ir (.A mow. UENKKAL ITIYSICAK FEATUKKS. 23 I inorutonnilea, for tlie hills art! ull low and rounded, while the interveninj; hollows aro occupied by exceodinf,'ly intricate and shallow, swampy lakes or marsheH. Tho valleys ot" the smaller rivers are usually narrow, and many of the streams are nothing l)Ut a succession of small lakes united by rapid rocky or bouldorv discharginf; clumnels. Probably one of the most interesting of the physical features pre valley ,,f sented by the district is the valley occupied by Lake Temiscaming and '"Vy.'V l^'^*^^"^ the Ottawa lliver. The greater portion of this valley is a very steep, TfiniKciuning. rocky g<>rg", fringed on either side by lofty hills or perpendicular dill's which rise abruptly to a height of from 100 to 000 feeot above the surface of the water, while the average of a largn number of soundings indicate that the lake has a mean depth of over 400 feet. The depres- sion, therefore, occupied by these watei's would be about 1000 feet below the level of the surrounding country, and as the bottom of the lake, wherever examined, consisttsd in the deeper portions of a very line gray unctuous clay or silt, this depth nniy have been much greater before the accumulation of this material. I'^om Mattawa to the mouth of the Moi u oal River, these abrupt and rocky shore-lines pre- vail, but above the mouth of this stream the lake undergoes considerable expansion and the shores exhibit a more gradual slope towards the sur- face of the water. The traveller ascending the Ottawa lliver is thus usually impressed with the mountainous character of the district, but Adjoining an ascent of the hills on either side at once shows that the adjoining '^" ' ' ' ' country is comparatively level, and that what appeared as ranges of hills are in reality the inclosing walls of this great valley. The Mattawa and Montreal rivers and in a lesser degree the Sturgeon and Ttmagami rivers occupy rather deep and ia\portant depressions in this rocky plateau. The district is traversed with rivers which are as important and well ]^.^\^^.^ known as the lakes which they .serve alternately as inlet and outlet. The Ottawa is of course the largest, but only a portion of this, from Mattawa to Lac des Quinze is included within the area of the accom- panying map-sheets. The Sturgeon likewise finds its source beyond the confines of this region, as also does the Montreal River, although by far the greatest portion of both streams is represented on the present maps. The Sturgeon is the larger of these two rivers, draining about 3000 square miles, while che Montreal drains an area of about 2500 square railes. The Matabitchouan, Mattawa, Keepawa, Temagami, Otter-tail and Otter rivers are also worthy of mention, although much smaller than the rivers first named. The Blanche River is a stream of considerable size, but only a small part of the lower portion is included in the Temiscaming sheet. I Kivcr vnlleys. 24 I NIPISSINCJ AND TRMISCAMINCJ REGION. m Lakes. In coramon with other regions characterized by the presence • of Archaean rocks, this district is remarkable for the number of lakes both large and small which are scattered over its surface. These lakes are in themselves noteworthy, not only for their many intricacies, but also because of the great number of islands which Distribution dot their surfaces. At first sight these lakes are seemingly governed dependent on |jy j^q i^^^ jj^ regard to their distribution, but a somewhat closer exam- geological •' ° ' . , structure. ination reveals the dependence of geographical outline on the geological structure. In order to bring out more fully uhe intimate relation sub- sisting between the topographical outline and the nature and attitude of the enclosing strata, a careful compilation and correlation Oi^ the various strikes or direction of the foliation of the j'neisses has been m-'de, exhibit- ing with as close an approximation to the truth as is possible the various curves and folds assumed by these rocks. Principal "phe following nine lakes, with their areas and elevation above mean sea-level may be particularly noted : — Area. Height Square Miles, above sea. Lake Nipiasing 345 640-5 6478 " Temiscaming 125 577 S-Ogi-S " Keepawa 120 87;V7-883 " Temagami. 100 964 Lac des Quinze 40 845 Lady Evelyn Lake 18 930 Obabica Lake 11 932 Obashing Lake 11 822 Rabbit Lake 8 938 Outlets of Lake Temagami, during the earlier portion of the summer, drains Temaganii. both northward, by way of Nonwakaming and Lady Evelyn lakes into the Montreal River, and southward by way of Cross Lake and Temagami River into the Sturgeon, the water thus ultimately finding its way into Georgian Bay and Lake Huron. The southern outlet, however, is the larger and deeper stream, while the northern one is >-v , . j, usually dry towards the end of July each summer, and is thus only Rabbit Lake, utilized in time of high water. Rabbit Lake finds its main outlet into the Matabitchouan River from the north-east corner of the lake, but a bay extending to the south-east is connected at extreme high water with Ross and Burwash lakes at the head of Macdonald Creek, which in turn empties into the Matabitchouan River at the Anninia- Fourth Bass Lako. Annima-nipissing Lake, a large and important iiipissing sheet of water situated between Lake Temagami and the Montreal Lake. . . , River, which has usually, as the name implies, been regarded as the Elevations of ultimate source of the Nipissing water, is 1070 feet above the sea, while highest lakes. Qpeeches Lake, which is in reality at the summit, is 1085 feet above the i •] DENUDATION. 95 I ! i sea. The highest lake in the whole region is Wilson Lake, at the head of one of the branches of the Matabitchouan River, and this is 1173 feet above the sea, while the height-of-land between this lake and the Montreal River is a little over 1200 feet above the sea Dermdatlon. In many of the descriptions which have from time to time Pre-glacial appeared concerning this, in common with other Archwan regions, «'^'=''^'"tio"- undue prominence has been given to the erosive effect produced dur- ing the glacial epoch. The prodigious number of lakes both great and small which are .so eminently characteristic of districts "r'^erlain by Archwan rocks, have in general been referred to as original rock-basins which owed their existence to the excavating power of an immense glacier, while the maramillated hills and complementary valleys every- where prevalent, as well as the constant occurrence of parallel grooves and scratches, have been adduced as additional evidence of the adequacy of the glacier to produce all the inequalities of the existing surface. The detailed examination of the region, however, amply demonstrates that the sculpturing to which the surface owes its present configuration, was practically completed long before the advent of the glacial epoch, and that the main valleys, especially those of the Ottawa and Mattawa rivers, were in existence long prior to the deposition of the Pala'ozoic sediments. In the first place, the more important lakes and rivers occupy such Depth of the deep and extended depressions that seem inexplicable on any theory ""^ ^" '"J**- of glacial action or ordinary erosion by water. The bottom of Lake Temiscaming 's on an average about a thousand feet below the level of the surrounding country, and in no place did the sounding lead reveal the original rocky bbttora which has been more or less deeply covered by silts and by accumulations of drift material. Portions of the Mattawa and Mon'^ieal rivers are fully six hundred feet below the level of the roi ky plateau through which they flow, and in many places exhibit steep, often peipendioular banks, composed of the hardest and most massive crystalline rocks, Secondly, the trend of many of these valleys 'oes not coincide with Many valleya the general direction of the ice-flow, as revealed by the stria' and "'?t odincKlent f _ T J \\\t\\ direction grooves which mark many of the exposed rock-surfaces of the plateau, of ice flow. These striae in general vary from S. 10° W. to S. 30° W., while S. 20° W. may be assumed as a fair average of the direction of the ice-flow throughout this region. The deepest valle}', that occupied ■ i^i\ ! I 26 I NIPISSIKG AND TEMISCAMING REGION. ■ARLOW, J Some sti'iiu coiTospond with direc- tion of certa valleys. Valleys not corresponding wit!) strike. Cut in rocks of different composition. Valley of Montreal River. by liake Temiscaming and the Ottawa River, from the mouth of Wabi Creek to its confluence with the Mactawa River, has a direction of S. 30° E. while the valley of the Mattawa runs about east-and-west, thus forming consideraljle angles with the general striation, while the Mon- treal and Sturgeon rivers are intersected almost at right angles by these grooves and scratche.s. On the shores of Lake Temiscaming, and also on the JNIontreal River, many of the stria? exhibited have a direction corresponding with these valleys. These may either represent a dif- ferential iMOveiuent in the mass of the ice itself, whereby the lower portion was forced by reason of its plasticity, to conform to the inequalities of the existing surface while the upper portion continued on its general south-wesierly course ; or, as seems more probable, these grooves may have belonged to a local glacier occupying these valleys towards tiie close of the glacial period. On the upper or wider portion of Lake Temiscaming, stria> belonging to the general glaciation may be noticed on the same rock-surface as other markings which belong to this local glacier, but the more abundant and strongly marked grooves throughout the lower portion of the valley, are seen conforming to its various changes of direction. Again, many of these valleys do not correspond with the strike of the rock in their immediate vicinity. The Ottawa valley is the best illustration of this fact, for the foliation of the gneissic rooks which compose most of its shores intersect tliis gorge almost at right angles. The depressions occupied by tlie Sturgeon and Montreal rivers also form considerable angles with the strike of the rocks in the immediate neighbourhood. Very often the streams occupy singularly straight and deep chasms in very hard rocks of different composition, valleys which it seems impossible that the ordinary erosive action of ice or water could ever have opened up, and which preserve their uniform direction with very little deviation in their course even when the river has left a softer rock to enter an area where the hardest varieties prevail. The Montreal River, from "The Notch," near its mouth, to the bend above the portage to Mud Lake, a distance of twenty-one miles, flows through a rocky gorge, the course of which is in general N. 40° W. At this point the course of the valley changes abruptly to S. 45" W., which is maintained till Bay Lake is reached, a distance of four miles. From this point upw.ird a valley extends as far as the (Jreat Bend, beyond the confines of the present mtp, which is almost if not quite parallel to that occupied by the river below Mud Lake portage. Of course the river presents many minor deviations in its dow the vulj success] characti little or The e these va early tii conglora Logan c shallow I the Hun senting t fringe fn Temiacac west side stones ari the penin limits of the eastei angular o which foi These det talus, fori ence took composed with a sm grit rest uj before tlu glacier flo\ polished tl the meshes hillocks. resting on t six miles Rivieres, a sandstones no fossils, \ The occu valleys she indicate the ^ ■ARLOW, ] DENUDATION. 27 I its downward course, but the remarkable uniformity in direction of the valley through which the stream meanders, ia maintained through successive alternations of slate, quartzite, graywacke and diabase, the character and composition of the surrounding rocks having apparently little or no effect in determining the course of this depression. The existence, likewise, of Pahi'ozoic outliers occupying portions of Paheozoic these valleys, seems ample proof of their existence as such from a very "" "''^^' early time. The occurrence of an outlier of limestones, shales and conglomerates belonging to the Niagara, was noticed by Sir William Logan on Lake Temiscaming in 1844. This outlier appears as a shallow syncline resting unconformably on the slates and quartzites of the Huronian. The conglomerate, grit and arenaceous limestones repre- senting the basal portion of the section, may be seen forming a narrow fringe from Piche's Point to Chiefs Island, on the east side of Lake Temiscaming, while a small patch of similar rocks crops out on the west side from Haileybury noitliward towards Wabi Bay. The lime- stones ai-e present on the islands to the north of Bryson Island, and on the peninsula between Suttons and Wabi bays extending beyond the limits of the present map. The boulder-conglomerate that occupies the eastern shore to the south of Chiefs Island, is composed of large angular or subangular blocks derived from the Huronian quartzite which forms rather abrupt hills immediately behind this exposure. The.se detached fragments doubtless repre.sent what was originally a I ',;(«»! bwls of talus, formed at the foot of this steep slope, and when the submerg- * '"■!?"■"»• ence took place, the intervening spaces be;.- :. ^'.lA v, detritus composed of the same materials, in a finer iilatt i iS together with a small proportion of calcareous matter, ' His- con,^ "ate and grit rest upon a surface which had clearly ass lju) J a hammock} character before the depo.sition of these sediment? • 'he acf/ion of the glacier flowing down Lake Temiscaming 1 - ■ *•* • ' „..iated and polished the whole, leavir.ga surface with a net-like struttui'e, through the meshes of which protrude rounded or ovoid sections of these rocky hillocks. Limestones and sandstones of Black River age are seen FUiKk River resting on the mammillated surfaces of Laurentian gneiss on the Ottawa, '""^* ""^' six miles below Matttwa, and also about five miles above Dei'x Rivieres, as well as on the Manitou Islands, Lake Nipissing, while sandstones which are probably of Chazy age, but which have yielded no fossils, were noticed on Iron Island in the same lake. The occurrence of such outliers at various points throughout th^se Tiansgienaion valleys show that they existed in very early Paheozoic times, and "^ Pivlseozoic indicate the transgression of the sea thus far inland at intervals during \lv 28 I NIPISSING AND TEMISCAMING REGION. M ;', numincjckf. Pre-glacial rock-surface. Cliffs along lakes and rivers. this, the Paheozoic, \ he submergence having been greatest during the Niagara, when the sua reached the northern end of Lake Temiscaming and may possibly have been connected by narrow arms and straits with that extending southward from Hudson Bay. The rounded or moufonn^e surfaces of all these rocky elevations, though no doubt accentuated by later glacial action, have in the first place been due to the unequal progress of rock decay. The work of Lawson, Low, Coste and Laflamme,* who have during the progress of their several explorations made critical and extended examinations of the relations existing between many outliers of Palaeozoic strata and the subjacent Archtean rocks, clearly shows that the mammillated surface long antedates the glacial epoch, and was as characteristic of the surface upon which the earliest Palaeozoic sediments were deposited, as that upon which the great glacier rested in glacial times. The chief cavities, vertical precipices and deep, narrow gorges must have been determini'd by great transverse or lateral breaks. The causes which operated in their formation must have been in force with marked intensity long before the deposition of the Niagara, for as has been shown, the valley had been practically completed before the depc :- tion of these sediments. The rounded contours of the rocky plateau and the intervening hollows, doubtless represent the depth to which these crystalline rocks had undergone disintegration during the immense la[)se of time while they were exposed to the action of the weather and other denuding agencies before the glacial epoch, while the ice simply removed the loose material resulting from such decom* position, smoothing and striating the rocky surfaces encountered. Both quartzite and diabase, and sometimes also the massive slate (or graywacke) which occurs as a transition between the more fissile slate beneath and the quartzite above, frequently from cliff's from fifty to two hundred feet in height, the angle of slope being considerably lessened by a talus of angular blocks detached from above. Goiid examples of these quartzite cliffs are furnished by the shores on the west side of Lake Temiscaming, opposite Bryson or Moose Island, at th(3 Obisaga Narrows on Lady Evelyn Lake, as well as by the steep hills on the west side of Cliff" Lake, while the Manitou or Devils Rock on the west side of Lake Temiscaming, south of Haih>ybury and the western shore of Temagami Lake, opposite the Hudson's Bay post are excellent instances of the vortical precipices produced by exposures of diabasic rocks. Prominent cliffs formed of * Bull. (Jeol. Moc, Am., vol. T, pp. 1(53-173, also Annual Ke|xirt, Geol. Surv. Can., 1882-83-84, part n. BARLOW 1 the ma! Kiver ii of Lad; frost an which t that one garni, hf the caua Althoi agricultu land are are to be earning oi although Lands De Gluigues a Baby and this side, On the op into lots, t of the lak valleys of five of the eluded wit The area rolling cla\ loam or sai appears at has in man; fire.s, this c Quinn Poi] gray clay th of quartzitf rise abrupt characterize appearance On the t and broken. Along the 1 »OIL. 29 I the massive slate or graywacke may be noticed on the Matabitchouan River immediately above the Fourth Bass Lake, as also on the west shore of Lady Evelyn Lake, south of Wendabin Bay. The action of the frost and weather are continually loosening large masses of these cliffs, which then fall witii a great noise, and this phenomenon is so fie(juent that one of the lakes (iNIanito-peepagee), to the west of Lake Tema- gami, has received its name on the supposition that the Evil One was the cause of the disturbance. SoU. Although the district as a whole cannot be said to be suitable for Areas of agricultural purposes, still in many places considerable areas of good '""'" land are known to exist. The largest continuous tracts of such land are to be found in the vicinity of the northern portion of Lake Temis- caming on both sides of the lake, and thus both in Quebec and Ontario, although the larger proportion is in the latter province. The Crown Lands Department of Quebec has sub divided the two townships of In Quebec. Guigues and Duhamel and portions of four others, Fabre, Laverlochere, Baby and Neudlac. These by no means exhaust the arable land on this side, but are sufficient for the present requirements of settlement. On the opposite shore of the lake, Ontario has laid out and divided In Ontario. into lots, twentj'^-five townships which extend along the western side of the lake, and running in a north-westerly direction include the valleys of Wabi Creek and the Blanche as far as Round Lake. Only five of these townships and the southern portion of four others are in- cluded within the "v ja covered by the accompanying map. The area thus sub-divided is in general composed of level or slightly Cliarauter c.f rolling clay land. In some places the clay sub-soil is overlain by clay loam or sandy loam, while in other instances a rather barren yellow sand appears at the surface. In the province of Quebec, where the surface has in many places been almost completely denuded by repeated forest fires, this clay is best seen. From the Quinze River a little south of Quinn Point, large areas are covered with a thick mantle of stiff (;>i,^y .,i_.ji„j, gray clay through which protrude exceedingly rough and prominent hills of quartzite, granite, diabase and breccia-coni.'lomerate. These hills rise abruptly from an otherwise level clay plain, for the surface characterized by the presence of this clay exhibits a singularly flat appearance with only a gentle rise towards the base of the hills. On the Ontario side, the township of Lorrain is rough, rocky Lwriin. and broken, and for the most part unsuitable for farming purposes. Along the valleys and in the vicinity of Lake Temiscaming the soil 30 I NIPIS8ING AND TEMI8CAMINO REr.ION. Bucke and Dyuioud. Linu'stone plateau. Hiuhun and Henwiiod. Valley of Mattawa. Valley of Sturgeon River. Kinoky I''m11s and Teuiagumi Kiver. is clay, but these clay flats are of comparatively small extent. To the north-west, however, in the townships of Bucke and Dyraond there are quite a number of farms, and a large area of cultivable land exists, so that the villages of Haileybury and Liskeard seem destined to become the centres of a considerable agricultural community. The top of the limestone plateau which constitutes that portion of the Niagara outlier forming the promontory dividing the northern end of the lakp, is generally overlain by a light sandy loam soil, although in many places the underlying rock is destitute of any such covering. • In the south-western part of Dymond and the southern portions of Hudson and Henwood, a series of rocky ridges of the Huronian slate occur. In the township of Henwood these ridges have a general north- and-south trend ; while in the township of Hudson the slate rises into hills some of which are nearly 200 feet in height. North of these ridges, according to Mr. Hermon, the soil is white clay, the surface generally level and the appearance of the couutiy flat and swampy. Between Mattawa and North Bay, to the south of the Mattawa River, in the townships of Papineau, Calvin, Bonfield and Ferris, con- siderable areas of l.'ind exist which may be utilized for farming pur- poses, and their proximity to the line of railway makes these of value. Already these townships contain a large number of excellent farms and the region is rapidly becoming settled. The soil is usually a clay- loam, rather rocky and stony in places, but seems to yield excellent crops. In the vicinity of North Bay the land is sandy and light. The valley of the Sturgeon, below the Temagami River, contains many wide and extensive flats which are susceptible of improvement, but above this stream the valley is much contracted and the flats decrease both in number and extent as the river is ascended, and towards the mouth of the Maskinonge River the country becomes much more broken and for the most part poor and rocky. Between Smoky Falls and the mouth of the Temagami, the country in the vicinity of the river is tolerably level and composed of gray clay overlain by sand. The soil is for the most part a sandy loam and affords support to a thick growth of hardwood and evergreens which by their sturdincss attest the good qualities of the soil beneath. Clearances have been made at intervals along the river, with the exception of that portion flowing through the Indian reserve, as far as the mouth of the Temagami, A short distance below the mouth of the Pike River, on the south side of the river, is an axtensive farm cultivated for many years for the pur- poses of supplying the lumbering camps of Mr. J. R. Booth, and a roii'J connects this depot with the Canadian Pacific Railway at Cache Bay station. 1 1 CLIMATE. 31 1 To the west of Sturgeon Falls there are a large number of farms W-uve River, which continue up the valley of the Veuve River, almost as t'ar as Warren station, where the valley becomes very narrow. The soil throughout the valley is a stiff gray clay, and as the vegetable mould overlying has been burnt off it has a tendency to cake in dry weather. In the vicinity of Sturgeon Falls the soil is very sandy, but the clear- Near Sturgeon ances continue to the east as far as the boundary of the Indian reserve, and to the south almost to the lake shore, although the land in general in this direction is flooded during the spring freshets. On the Montreal River above Bay Lake, there are large areas of Montreal arable land, especially between Bay Lake and the Mattawapika. The region to the north-west is very flat and level, underlain by clay^ and althoujih swampy at present, would probably be easily drained or dry up when cleared. These areas are most likely continuous with similar tracts noticed to the south-west of the townships of Henwood and Hudson. A large tract of country extends from the vicinity of North Bay lietweeii and the southern part of the townships of Widdifield northward to (n,,! (),,i,„'ii;a the Opimika Creek. The soil is in places sandy and in some spots I^*'"'"^^'*' considerable clay is present, but the whole of this stretch of country is covered by a mixture of hardwoods and evergreens, thus denoting a rather good soil beneath. The greater portion of the district, how- ever, is extremely rocky and barren, the level areas being chiefly occu- pied by swamps, many of which would be ditticult to drain, while the area thus drained would in most cases be insufficient for purposes of farming. Of the country surrounding Temagami Lake and the greater Oreat \»Tt of part of the central portion of the area, only small tracts would be al)le for available for purposes of settlement. The soil in general is extremely ^'^''"''"K- light and without the aid of artificial fertilizers would soon fail to yield any adequate return. The rosy picture too often drawn of immense tracts of land available for agricultuial purposes, is to say the least very misleading, for apart from possible mining and its timber resources, by far the greater portion of the region will only be valuable as a health and recreation ground for tourists and sportsmen The great tracts of forest as yet untouched by the axe, the vast number of picturesque lakes, both great and small, with fish and game in abun- dance seem to render the district especially attractive for such purposes. Climate. In regard to the climate of the district as a whole, it may be said (Jcneral in a general way, that the advent of spring is from three weeks to a [;|™aeter ' 32 I NIPISSING AND TEMISCAMING REGION. Oijeniiig of navigation. Closinfc. Progi'f'ss I if spring. r '■: I ; Harvest. Summer frosts. month behind that of the region immediately surrounding the city of Ottawa, with a correspondingly earlier setting in of the winter. The winter is as a rule one of long continued and severe frosts, while the summer is proportionately shorter and much cooler than the country bordering the lower Ottawa. The average fall of snow in winter as well us th(! rainfall during summer is likewise considerably in excess of that in regions further to the south. Navigation generally opens on Lake Temiscaming about the end of the first week in May, although in occasional unfavourable seasons it is sometimes delayed a few days longer, while Keepawa Lake does not usually break up till a week later, In 1893, the ice on the latter lake broke up and moved out between the 15th and 17th of May. Lake Temagami, which occupies the heigh t-of-1 and between the waters flow- ing to Lake Temiscaming and those emptying into Georgian Bay, being nearly 400 feet above tlie last-named lake, does not generally break up till the latter part of May, the lake usually being clear of ice about the 24th of May. The season of navigation closes, as far as Lake Temagami is concerned, between the 10th and 15th of November, while on Lake Temiscaming steamers have been known to make fairly regular trips within a few days of Christmas, although as a rule these boats cease running early in December. The snow begins to melt about the middle of A.pril, and has gener- ally all disappeared by the 10th of May, although both snow and ice were noticed in secluded nooks and cracks along the sides of the precipitous cliff's on the west side of the Ottawa River as late as the end of May. Mr. C. C. Farr, formerly of the Hudson's Bay Company, and now postmaster of Haileybury, who has become identified with this young and flourishing settlement, states that " seeding-time com- mences about the first week in May and ends, so far as oats are con- cerned, about the fourth of June, though oats have been sown as late as the 20th of June, and have done fairly well. Potatoes can be planted as late as the 20th of June, and it does not profit much to put them in before the 24th of May. Corn, cucumbers and melons can be sown about that date. Haying commences about the 14th July, harvest the loth August." Summer frosts, so much dreaded by the farmers, specially in districts newly opened for settlement, have in the past proved a rather serious barrier to the successful raising of wheat, while oats have suflFered severely, particularly in clearances situated some distance from the larger bodies of water. Frosts generally occur from the 18th to the 25th of August on the calm, clear nights following heavy north winds. TIMBER. 33 I In the vicinity of Lake Temiscaining the settlers often escape them altogether on account of their proximity to this large sheet of water, or their crops are but slightly injured, the more tender vege- tables frequently being the only sufferers. The gradual clearing up of the land and the draining of many of the swamps will, however, materially mitigate this difficulty, particularly in the district in the vicinity of Lake Temiscaming, which is the area most suitable for extensive settlement. The Native Inhabitants. The Inflians who reside within the area under description belong to imlians. the once numerous and powerful Algonquin family. They speak the Otchipew or Chippewa language, the same as that in use among the many bands which are scattered over the wide territory to the north and west of Lake Superior, with only a few minor alterations. They are divided into three bands known respectively as the Nipissing, Temiscamingue and Temagamingue bands. On June 30th, 1887, the m. • , . census taken by the Department of Indian Affairs showed a total Indian population of 394, while on June 30th, 1897, this population had only been increased to 430. The census taken in 1887 showed the following numbers in each band, Nipissing 165 Temiscamingue 136, and Temagamingue 93, while that taken in 1897 shows the popu- lation of the several bands to be, Nipissing 193, Temiscamingue 162, and Temagamingue 75. While therefore the total Indian population of the district shows a slight increase, one of the bands (Temagamingue) is slowly but surely decreasing. Two of the bands are comfortably settled on spacious reserves but no tract of land has yet been allotted residence. to the Temagamingue band. The Nipissing band resides chiefly in two small villages situated on the north shore of Lake Nipissing. The larger of these is about two miles west of North Bay to the south- west of Beaucage station on the Canadian Pacific railway, while the smaller one is located near the western boundary of the reserve, about four miles south east of Sturgeon Falls. The Indians and associated half-breeds have built a considerable number of rather substantial dwellings, each with a small cultivated patch attached, on the northern bank of the Quinze River, forming the village or settlement of North Temiscaming. 1 Mi I Timber. All the early explorers speak in terms of enthusiasm of the original White pine, great forests of the region here described. The most valuable tree from 3 34 I NlPISSmo AND TEMI8CAMING REGION. •kHUlW I' I a commercial standpoint is the white pine (Pinus Strobus), and in spite of tl»e extensive operations carried on almost uninterruptedly by the lumbermen throughout a large part of this region during the past fifty years, this tree is still present in considerable quantity. Next Red pine. in importance and more abundantly distributed is the Norway or red pine (I'inus reshiosa.) In the early years of the lumber trade, the greater value of this tree caused it to be sought for at more remote distances than the white pine, and thus we find at this time that camps for cutting red pine timber were many miles in advance of those erected for the purpose of securing white pine loi^s. The superior qualities of the white pine, however, soon came to be recognized and in time completely drove the red pine from the market, or so limited its sale that only a few of the finest trees were hewed down and utilized. Of late years, however, the marked diminution in size and quantity of the white pine has again brought the red pine forward, and both varieties are now cut without discrimination. The red pine seems to flouiish on the apparently sterile sand plains, which are a feature in many parts of this district, and frequently forms excee('ingly thick groves on the sides of hills where sand and gravel have collected, or on points composed of these drift materials which jut out into many of the lakes. Jack-i)ine. Jack-pinc, called by some, pitch-pine, or bastard spruce {Pinus Banksiana) is very often encountered in the more barren and rocky areas, and its presence seems an almost certain indication of the ex- treme poverty of the underlying soil. It is usually more or less scrubby or stunted in its growth, although occasionally, as in .some areas to the north-west of Lake Temiscaming, it attains sufficient dim- ensions to be utilized for rough lumber. In the vicinity of the south- ern and eastern shores of Lake Nipissing, the scanty groves of dwarf-like evergreens are almost wholly composed of this species, the hardy roots penetrating the various cracks and crevices of the rock. This tree S'lso seems to select sandy or gravelly plains which have been overrun by fire and which had previously been occupied by a luxuriant growth of red or white pine. Spruce. Both white and black spruce (Picea alba and Picea nigra) are fre- quently met with, the latter being more abundant, but are too small to be of any commercial value for lumber, although many individuals would make excellent masts or spars. Cedar. White cedar (Thuya occidentalis) is usually found fringing the banks of streams or the shores of lakes, where it often forms a thick and at times an almost impenetrable undergrowth. Overhanging trees are free high wj ©red, b< marshy hills, an a dense less stur hollow a many tin The w occurren second gi species in though s green, esj large tree as in the I be procure Temagami of their ki of good an Three vj the balsam or aspen p Of aspen ( stately tree country to arac, someti A mericana) degree the s forest where immense tra iko and Otte abundant su stantly met ' favourable tc The balsan the moist ai ward to the I below the a observed as ; H J TIMUEK. 35 are frequently undermined by the waters or current during tikiies of high water, and thus it happens that most of the drift-wood encount- ered, belongs to this species. Its favourite haunt also seems to be the marshy hollows or tlats, which so commonly occur between the rocky hills, and extensive areas of swamps are almost entirely covered with 3. dense forest (jf this tree. As a rule, the tree is small and more or less stunted in its growth, while the larger individuals are frequently hollow at the butt. To the north and north-west of Lake Temiscaming many tine specimens of this tree were noticed. The white or canoe birch {Betufa papyri/era) is also of very common W)\ite liirch, occurrence, and together with the aspen poplar forms the prevailing second growth in areas which have been recently swept by fire. Both species in these instances form very thick groves of tall and straight though small trees. Interspersed with the more prevalent ever- green, especially where the soil is deeper and better, are occasional large trees which are of sufficient size to furnish good bark for canoes, as in the Sturgeon River valley, where good sized specimens may still be procured. The birch-bark canoes made on Lakes Nipissing and Temagami and at Mattawa, have always been considered the very best of their kind both in build and material, but of late years the supply of good and suitable bark is becoming perceptibly less. Three varieties of the poplar were noticed throughout the region Poijlar. the balsam or rough-barked poplar {Populus balsamifera), the white or aspen poplar (Populus trernuloides) and the large toothed poplar or aspen {Populus grandidentata). The poplar sometimes forms stately trees, especially in the Sturgeon River valley and in the country to the north and north-west of Lake Temiscaming. Tarn- Tuiniirac. arac, sometimes called hackmatack and occasionally juniper (Larix Americana) is abundant, and in common with the cedar and in a lesser degree the spruce, affects the low-lying areas or those portions of the forest where moisture nay be readily and constantly secured. The immense tracts of swampy land between the head-waters of the Tom- iko and Ottertail rivers to the north of the Spruce Lakes contain an abundant supply of good sized specimens of this tree, and it is con- stantly met with all through the region whenever the conditions are favourable to its growth. The balsam or fir {Abies bahamea) is one of the most common in BmIsuh.. the moist areas. Hemlock {Tsuga Canadensis) was noticed north- H.mlDLk. ward to the Indian portage-route to Keepawa Lake, a short distance below the mouth of the Keepawa River, but no specimens were observed as far north as the Old Fort Narrows. It occurs rather H 36 I NIPISSINfJ AND TEMISCAMIN*; REfilON. •ARLOW. il i I I i I r>aHH\V(K)(l. Yew. Al<]er and willow. abundantly and of large .size in the vicinity of Lake Nipissing and on the Sturgeon River, but was not remarked in the northern and north- western portions of the region. The basswood or linden tree ( Tilia Americana) was occasionally noticed on the Sturgeon River, while Sir William Logan mentions individuals two feet in diameter, associated with black birch and maple of similar dimensions, in the hardwood strip of country extending from behind the hills north of Trout Lake at the head of the Mattawa River to the Opimika Narrows on Lake Temiscaming. The basswood was also noticed mixed with maple, elm, poplar and balsam near the mouth of the Blanche at the north end of Lake Temiscaming. The American yew, sometimes called ground hemlock {Taxus haccata var. Canadensis) is an exceedingly common shrub, and is particularly noticeable, as when present it often forms an almost impenetrable un- derbrush. Alder and willow of several varieties are present in the various swamps or lining the banks or shores of streams and lakes. scarce, Maplp Hardwood Although nearly all the principal varieties of hardwood are found in a"ir.l. ' this region, the proportion which such trees bear to timber of a softer description is quite insignificant. Of the maple family, perhaps the most abundant is the sugar maple (Acer Saccharum), which is fre- quently of large dimensions. The soft maple {Acer rubrion) is also present in large quantities, but the black or bird's eye maple (Acer nigrum.) is only rarely met with in the valleys of the southern portion of the region. The mountain maple (Acer spicatuni) is one of the com- mon varieties in moist ground, while the striped maple (Ao'r Pennsyl- vanicum) was noticed in many places. This tree is often called Moosewood, because the green and juicy tops form a favourite food for the moose, although the true " moosewood " (Dirca palustris) was noticed in many places suitable to its growth. Moosewood. Yellow birch. lilack birch. Oak. Large trees of yellow birch (Beiula Intea) were remarked through- out the region, especially in the vicinity of the northern end of Lake Temiscaming, while specimens of the black or cherry birch {Betula lenta) were seen over thirty inches in diamatfr in the region to the north of the Mattawa River. The blue oak or swamp white oak (Quercus macrocarpa) is the most abunda>;l 'A the oak family, and its favourite haunt seems to be the alluvial flats or intervals along the banks of streams where the soil is sufficiently moist and fertile. Here it is associated with the white elm (JJlmus Americana), which forms large and beautiful trees, the black or water ash (Fraxinus sambucifolia). The white oak (Quercus alba) seems to delight in lighter and drier soil, and good specimens were seen growing in the vicinity of Fort Temiscaming. The as far north as o Virginica) is toleral growing with the Ai hardwood land abou Temiscaming. Of the wild fruits, sparingly representee trict on the Ottawa, dant on all neglect and in the vicinity oi riparia) was seen gn well as on several islt low-bush cranberry (( on many of the marsh The former species is swampy flats in the vi Lake Nipissing is tl formerly were a source band of Indians, who to sell to the traders o variety of cranberry (( command a sufficient j The high bush cranb along the river-valleys low. Tiie bushes are height, and are especia! head of Lake Temiscamii earning, and fringing t: further to the south. Th ( Vaccinium Canadense a which have been lately known to set fire to som( of this fruit. Vacciniun locality, but is also freqi posed to the sun's rays, v ant though much better j soil as well as localities v Of the deer tribe the m and the red or Virginia . i v.i •AKLOW. I FAUVA. 17 I Temiscaniing. The red oak (Quercus rxibra) was also noticed in places as far north as our explorations extended. Ironwoo the large-mouthed and small-mouthed, are present (Micropterus sal- inoides and M. dolomieu). There is an extreme variability in point of colour which is clearly owing to the nature of their surroundings. In colour depen- lakes and streams where the water is of a prevailing brownish tint, the dent on sur- *^ . roundings. bass have a correspondingly dark hue, while in the clear, greenish water of Lake Temagami and Little Lake to the east of the Old Fort Narrows, the bass have a pale-green coloration. This variation in hue is not a peculiarity affecting the bass alone, but may be also noticed in the trout, pike and especially in the pickerel. The finest specimens of these fish may be secured in Lady Evelyn Lake (which contains no trout), Temagami, Red Cedar, Annima-nipissing, White- bear Net and Rabbit lakes, although these by no means exhaust the list ; while on Lake Temiscaming and Little Lake, though not so abu .idant, the specimens obtained are generally of verj large size. The rock bass or red eye (AmblG])lite3 rupeatris) a; id the common Rock -bass and 3unfish (Lepomis pallidus) are also extremely numerous where condi- Sun-fish, tions are favourable. The common yellow perch and the pike-perch or pickerel are closely Perch, allied forms. The yellow perch [Perca americana), although of good quality, is generally small, rarely attaining over one pound in weight, while the average size is very much smaller. It is not of economic importance as a food fish like the pickerel. The pickerel {Slizostedium Pickerel. vitreum), called by the French, dore, is possibly next to the trout and whitefish the most valuable food fish found in the region. During several weeks of summer (l(if,'ioal The several geological systems and formations represented in the Subdivisions. rggJQ^ covered by the accompanying map-sheets and subjacent to the Pleistocene superficial deposits, may be thus stated in descending order : — i Silurian — Niagara. Camuro-Silurian — Trenton. Birdseye and Black River. iHuRONIAN. Laurentian — Diorile-gneiss and granite-gneiss or " Fundamental gneiss." The Archa'an rocks of the region here described may naturally be separated into two great subdivisions, that of the so-called Lower Laurentian Laurentian and the Huronian, although a few small isolated inliers of andHuronian. crystalline limestone, and one at least of a dark -gray, exceedingly sf^ueezed and altered gneissic rock, are found to be inclosed in the ordinary granitic and dioritic gneisses. These are unimportant in this district, and so small in area that it has not been possible to distin- guish them separately on the map. They resemble very closely rocks which in regions further to the south and south-east are known as the Arch wan roclvs. •ARLOW Grem discus those in this the su Unc includ( materii positioj a differ scure ai sent re| charact( by alter some rej make ai later anc Detail by varioi that mos massive ( been imp magma o deformati complete been urse of these r Every prefaced 1 to include molten or bardeninj: associated It must here repres just given, distinct or rocks as a they now p it wjl be 8 wheie a qui GEOLOGY — GENERAL STATEMENT. 43 1 Grenville series. The present report therefore does not include an}' (irenville discussion of the relations of the rocks classed as Huronian with ■''"''>*'*'• those of the Grenville series. These two series do not come in contact in this area, and the question of their relations is at present being made the subject of special investigation in central Ontario. Under the name Laurentian, in the area here described, are Laurcntian. included a great number of varietal forms of granitic and dioritic materials, having essentially the chemical and mineralogical com- position of such rock-types, but differing in their foliated texture, a difference which although almost invariably present is sometimes ob- scure and occasionally fails altogether. Their subdivision in the pre- sent report is based solely on their petrographical and .nineralogical characters, for although their prevailing foliation, fre:juently marked by alternating bands of varying composition and colour, resembles in some respects an original stratification, it has been found impossible to make any such stratigraphical subdivision corresponding to that of later and truly bedded formations. Detailed investigations both in the field and with the microscope, . by various geologists and petrographers, have of late led to the belief gneisses. that most of these gneisses have an origin in common with their moie massive equivalents, and that the prevailing foliated character has been imparted to the rock-mass by differentiation in a slowly cooling magma of more or less heterogeneous composition, or as a result of deformation by pressure after the rock had undergone either partial or complete consolidation. The cogency of the arguments which have been urged in favour of the recognition of the greater part, at least, of these rocks as foliated irruptives now seems beyond question. Every recent report aiming at scientific accuracy, is necessarily ,j,]^^ ^^^^ ^^ prefaced by an apology or e.xplanation of the use of the term Laurentian the nume to include such gneissic rocks of irruptive origin, that have been in a molten or plastic condition at a time subsequent to the deposition and hardening of later truly stratified rocks with which they are intimately associated and occasionally interfoliated. It must therefore be clearly understood that in placing the rocks here representing the Laurentian at the base of a table such as that just given, it is not intended to indicate that they stand for any distinct or prolonged lapse of geological time, nor to aflBrm that these rocks as a whole, in their present condition, and with the foliation they now possess, really antedate those of the Huronian system. This, it w 11 be shown, is not the case in many, if not in most instances wheie a question of the kind can be determined. I • .: :i 1' 1 it Hi! ^^ ^W7 ° ? ?yffi l'BiB WI "ll 44 I MPIS8IN0 ANi) TEMISCAMINO REGION. BARtOW Origin of Fundamental gneiss. Formation of granite and diorite gneiss. Successive intrusions. '"'i'lj.te near Anikiinii-nipis' sing Lake. Granite area between Rab- bit and Tenia- ganii Lake. The Fundamental gneiss is here therefore accorded a priority in description to which it is not structurally entitled, a.s it may possibly represent in great part, the first-formed crust of the earth, which, neces- sarily thin and fragile, and so liable to frequent upwellings of the molten mass beneath, has undergone successive fusions and recement- ations before reaching its present condition. As at present mapped, it is regarded as a complex of irruptive plutonic rocks, representing re- peated and intricate intrusions of basic and acidic material. Although in many instances, and i.i limited areas, the succession of such irrup- tions can be rascertained, with tolerable accuracy, any attempt to cor- relate this succession in detail over extended areas, has invariably ended in more or less complete failure. In general, however, it may be stated that the earliest secretions of the magma from which these rocks have solidified consisted of a series of granitic and dioritic gneisses, very evenly and distinctly foliated, varying in colour from reddish through reddish-gray and gray, to dark- green and almost black. These gneissic rocks were subsequently invaded by a massive, deep- red biotite-hornblende-guoi i tl;Ht usually possesses a more or less distinct foliated structure, marked by the parallel alignment of the bisilicate minerals. It seems highly probable, however, that no great lapse of time intervened between these successive irruptions, as the latter in all probability represents the residual portion of the magma, necessarily more acidic and homogeneous in composition. Dykes of coarse pegmatite, as well as of fine-grained aplite, cut the diflferent varieties of gneissic rocks or are frequently interfoliated with them. To the north-east of Lake Temagami, there is a large area of flesh- red granite, which in many places, especially in the vicinity of Carry- ing and Annima-nipissing Lakes, has a distinct foliated structure. In appearance, composition, and behaviour it has so close a resemblance to similar rocks mapped as Laurentian further to the south that it is proposed to include it with these rocks. Between Temagami and Rabbit lakes, there is a somewhat similar granite, which, however, is continuous with the main Laurentian area to the south, and is accordingly designated Vj) the same coloration. In both cases these rocks pass by insensible gradations into a medium- textured dark-green gabbro or gabbrodiorite, with which they are intimately associated, by an increase in the plagioclase and the pre- ponderance of hornblende as the coloured constituent. Although in the accompanying map these gabbro masses are shown in the colour usual for such basic intrusions, it must be borne in mind that they are believe that hi The and mi trast, e ing th( stratifie vulcani.' and str volcanic cesses oi rate wh member or round degrees ( rocks, en similar n sericite fi In earl dance of foliation ficiently i strata res granites, recent yet. earning, si general .■•:« " chloritic as essentif been evide they have rearrangen correlated face in thi diabase anc reveals a c that cannol Throughf able into th follows : — ( slate. (3.) 1 '] GEOLOGY — GENERAL STATEMENT. 45 I believed to represent basic portions or segregations of the same magma that has elsewhere crystallized as granite. The Huronian rocks are generally clastic in composition, appearance, Hurouiun and microscopic structure, and in this respect are in marked con- trast, even in their most altered phases, to those described as constitut- ing the Laurentian of the district. A large proportion of these stratified rocks indicate the existence of intense and widespread vulcanism, which evidently chaiacterized this period ; their composition and structure showing a most intimate association of undoubted volcanic ejectamenta with material resulting from the ordinary pro- cesses of erosion and sedimentation. The breccia or breccia-conglome- rate which is so abundantly represented, and here forms the basal member of the Huronian, is composed chiefly of anj^ular, sub-angular, or rounded fragments of red and gray granite, diabase of difl'erent degrees of texture, and various fine-grained slaty and halleflintalike rocks, embedded in a fine-grained, often argillitic matrix, consisting of similar material in a much finer state of division, with chlorite and sericite filling the smaller interstices. In earlier reports on these rocks, the much greater relative abun- p-^ju. ,„i^co,i. dance of the granitic fragments, coupled with the so. ^ewhat distinct ceiitions foliation observable in a few of these, was evidently taken to be suf- ficiently strong and positive evidence to justify their description as strata resulting from the degradation of the Laurentian gneisses and granites. The more detailed and critical examinations made during recent years, covering the country between Lakes Huron and Temis- caming, show, however, the error of sich a conclusion in any wide or general sense. Thus the rock, first described under the name of " chloritic slate-conglomerate " by Sir William Logan, must be regarded as essentially of pyroclastic origin, the volcanic ejectamenta having erate.°^"^ "" been evidently spread out upon the bottom of a shallow sea, where they have undergone in many instances considerable attrition and rearrangement by water. Much of the coarser material cannot be correlated with anything now known to be present at the earth's sur- face in this region ; while the intimate association of this rock with diabase and gabbro intrusive masses, rather than with the granites^ reveals a close genetic relationship subsisting between these rock.s, that cannot be regarded as merely accidental. Throughout the area, the Huronian, where fully represented, is separ- ^ . , . ,,. , !■• 11... i-i • T 1 Division of able into three distinct subdivisions which are, in ascending order, as Huronian. follows: — (1.) Breccia or breccia-conglomerate. (2.) Grayicacke shale or slate. (3.) Felspathic sandstone or quartzite. . \ I .i. !: , 46 I NIPISSINQ AND TEMI8CAMING REGION. Breccia congloinerato, (Iraywacke and ahale. is: i Arkose. Birdseye and Black River on Lake Nipissing. As a rule, the lowest uumber, or breccia-conglomerate, presents only obscure evidence of stratification, and wherever such were visible the rock occurs in thick massive beds, showing only a slight inclination or dip. This may be well seen in the hills on either side of Lake Temiscaniing between the Montreal River and the Old Fort Narrows. Where subjected to pressure, however, as is very frequently the case, the cleavage-foliation thus developed is a much more prominent structural feature and is thus very often mistaken for the bedding. This is especially the case in the region immediately adjacent to Lake Temagami, where this rock is very widely exposed and where it is associated with and squeezed between large masses of diabase and granite. Superimposed upon this, and forming a transitional rock upwards into the succeeding subdivision, are beds of varying thicknesses of gray- wacke or felspathic sandstone, less massive in structure ; while the coarser fragmental material gradually disappears as an ascent is made in the series. The succeeding shale or slate, which is in general very similar in composition to the graywacke or the finer matrix of the breccia-conglomerate beneath, is often beautifully banded in vary- ing shades of green, purple or brown. The cleavage in most cases corresponds with the bedding, although occasional instances were noticed where cleavage or jointage planes were developed at con- siderable angles with this bedding. Superimposed on this slate, in many parts of the area, is a very massive much jointed quartzite or grit, generally sea-green in colour because of the abundance of minute scales of sericite distributed through the finer portions of the rock. Occasionally, however, it has a reddish tinge, and the arkose then closely resembles a granite, both in composition and appearance. The rock is so massive that it is often only by the parallel alignment of certain coarse quartzose and otiier fragments that the original bedding can be distinguished. These various members of the Huronian here follow one another in regular and often nearly horizontal succession, except in the vicinity of the large igneous masses, where they show considerable evidence of disturbance as well as of alteration. The Pahvozoic rocks represented in this area consist of outlying patches of the following formations : — (1) Birdseye and Black River, (2) Lower IVenton, (3) Niagara. The outliers representing the Birdseye and Black River formation, are exposed on some of the islands composing the Manitou group in Lake Nipissing. These are of very limited extent and consist of sand- stones, limestones and shales, the whole section probably not exceed- ing thirty feet in thickness. MRLOiv. 1 Some SI overlying Ottawa R exposures, and thus s occurring The Nici light-buflFc conglomen slates and of Lake Te low, shallo The coar sand, are n surface bei erratics, esj paratively s with coarse position of types preva able distanc ing, and Tei district, the by deposits is a thick ar many places in flats of cc cut deep anc plains are st< strata. In i of which is o utilized in th valleys, and covered by < boulders. In the vici depth of coai the gray clay the vicinity o: forming flats have been fo Bw. 1 GEOLOGV — GENERAL STATEMENT. 47 I Some small exposures of sandstones and arenaceous limestones occur Trenton overlying unconfornmbly the gneissic rocks of the Laurentian on the Mattawn. Ottawa River below Mattawa. The fossils secured from these thin exposures, indicate that the containing rocks are of lower Trenton age, and thus somewhat higher in the str.itigraphical succession than those occurring on the Manitou Islands. The Niagara formation, as exhibited in this district, is composed of Niagara forni- light-bufFor cream-coloured limestones and shales, with a basal boulder- Tenilscani'ing conglomerate, or sandstone, unconformably overlying the Huronian slates and quartzites on the shores and islands of the northern portion of Lake Temiscaming. The strata composing this formation form a low, shallow, synclinal trough. The coarser varieties of drift material, such as boulders gravel and Pleistocene sand, are rather abundantly represented on ths higher grounds, the ^P°^''^''' surface being everywhere more or less encumbered with the larger erratics, especially on those slopes facing southward, while the com- paratively shallow and rocky intervening valleys are frequently tilled with coarse yellow sand, sometimes derived mainly from the decom- position of rock almost in situ. These boulders are usually of rock types prevalent in the district, but some show carriage from consider- able distances. With the exception perhaps of the Mattawa, Nipiss- ing, and Temiscaming valleys, there is little or no clay present in this district, the Hatter details of topographical outline being given chiefly by deposits of coarse yellow sand. In the Temiscaming valley, there is a thick and extensive deposit of a stiff, stratified, gray clay which in many places effectually conceals the rock beneath. This clay occurs in flats of considerable area, through which the various streams have cut deep and tortuous channels, while protruding through these clay plains are steep and rocky hills of the prevailing types of the Huronian strata. In the wide depression the deepest and most northern portion of which is occupied by the Mattawa River, and which has also been utilized in the construction of the Canadian Pacific Railway, the minor valleys, and often too the separating rounded rocky elevations, are covered by clay deposits containing a considerable intermixture of boulders. In the vicinity of North Bay and Sturgeon Falls, a considerable depth of coarse and yellow sand is present at the surface, concealing the gray clay beneath ; but to the west of Sturgeon Falls, especially in the vicinity of Verner, the stiff, gray, stratified clay comes to the surface, forming flats which have been burnt over or cleared. So far no fossils have been found in these clays, although in places diligent search ^ ^ m 1 ;■ I , '1 ■I .;. i ■ I 48 J NIPISSINQ AND TEMISCAMINO REGION. Are s covered by (liffcreiit rock forma- tion». was made for any such evidence of their origin, especially in the hard concretionary nodules which may be occasionally noticed. The areas covered by the several rock-formations maj' be stated roughly as follows : On the Lake Nipissin;,' sheet there are about 3186 square miles of Laurentian, and 270 scjuare miles of Huronian, while on the Lake Temiscaming sheet there are only 946 square miles of Laurentian, 2470 square miles of Huronian and associated eruptives, and forty square miles of Silurian. The two sheets combined there- fore show 4132 square miles occupied by Laurentian, and 2740 square miles by Huronian and associated granites and diabases. The Silurian covers about forty square miles, but extends north-westward to a con- siderable distance beyond the northern confines of the Lake Temis- caming sheet. The aggregate area of Cambro-Silui'ian strata exposed on Tiake Nipissing and Ottawa River is less than two square miles. Laurentian. Origin of name The name Laurentian was originally proposed by Sir William Logan, in 1853, as the most appropriate designation for rocks classified by him in previous reports as the " Metaraorphic Series," and which were believed to be identical in composition and origin with similar rocks so named and described by Lyell. The term thus introduced soon received an almost universal adoption by geologists, as a conveni- ent one for the gneissic crystalline rocks found to underlie unconform- ably the Palseozoic strata, and presumably forming the oldest of the geological systems. The urgent need of such a distinctive appellation was recognized as a consequence of the ambiguity which would neces- sarily arise from the use of such a general term as "metamorphic," which is applicable to any group of strata in an altered condition, while the peculiar fitness of the name was suggested by the fact that these rocks were found to constitute the bulk of the Laurentide moun- tains, a series of elevations lying to the north of the River St. Law- rence, and which were so called by the late Mr. Garneau, the historian of Quebec. Griffin of term The term "gneiss" or "gneuss" was originally employed by the "gneiss, early Saxon miners for the country-rock containing the Erzgebirge silver ore deposits The rocks so named were divided into a " red " and " gray " variety, which although differing somewhat in their component minerals presented many features in common that caused them to be included under a uniform designation. The rocks so described are closely analogous in composition and structure to many of the rocks Urgent need of name. •AHLOW. ' J within "gneis adopte* tially ^ solely ( pecuJiai differen howevei variety but whi( parallel Althoi inapplica except as examinee term, as i microscop The ori more or It mulgation Hutton ar definition primeval c sedimentai been remoi Such rocks mental gne upon whic Metamorph the most pc structure ar internal hea The vario a long time while masses unyielding tc the most pro to be entirelj allied rocks, surviving tra which had e 4 m •] LAURENTIAN. 49 I within the area of the present map-sheets, and to which the name "gneis.s"has been usually applied. The name was very generally adopted hy geologists, and its use was primarily restricted to rocks essen- tially granitic in their composition and appearance, differentiated solely on account of their foliated texture ; the persistency of this peculiar structure over large areas, presumably furnishing proof of a diff'erence in origin from the normal or massive type. Gradually, I'^e of term however, the use of the term became so extended as to include a great variety of crystalline rocks differing widely in composition and origin, but which exhibited in connnon a more or less decided tendency to a parallel arrangement of their component minerals. Although modern petrographical studies have demonstrated the (fueiss useful inapplicabilitj' of such a term for purposes of accurate description, '/ield'teVin!!''^'^^ except as an affix to denote the structural features of the rock-types examined, the name must still be employed as a convenient " field " term, as a means of rough description anc' correlation, where detailed microscopic examination is either impossible or considered unnecessary. The origin of these gneissic crystalline rocks was, for a long time, ( )riKin of cry- more or less a matter of theory and conjecture. Previous to the pro- ' mulgation of the theories regarding rock metamorphism, first held by Hutton and subsequently by Lyell, to whom we owe the first use and definition of this term, these rocks were regarded as portions of the primeval crust, which had either never been enveloped by the later sedimentaries, or from which such covering, if originally present, had been removed as a result of subsequent upheaval and denudation. Such rocks were then almost invariably referred to as the " Funda- mental gneiss or granite " and believed to be the basement or floor upon which all subsequent sedimentary formations were deposited. Metamorphism, either regional or contact, has always been considered the most potent influence in the destruction of evidences of original structure and composition in rocks subjected to the effect of the earth's internal heat, or that engendered by the proximity of eruptive masses. The various changes, however, which this term describes, were for Met- a long time thought to be confined entirely to sedimentary strata, }j,',',i, while masses of igneous plutonic rocks were regarded as too hard and ""^nt'ii'y rocks unyielding to be at all affected by the metamorphosing agencies of even the most profound orographic movements. Foliation, though long held KoHivtion dis- to be entirely distinct from stratification in the case of slaty and other t'^ctfro™. *' _ _ "' stratitii'ivtion. allied rocks, was in the instance of these gneissic rocks regarded as the surviving traces of the parallel structure due to original sedimentation, which had escaped obliteration. It is only in very recent years 4 ■ fon- ledi- W \i : > i? >' I Work by LoHReii. Work by Lehmann, 50 I NIPI88WO AND TEMI8CAM1N(1 UEOION. Daubree's opinions. Results of work by Niiu- mann and Reusch. Work by Ten! 1 and I Williams. that this impro.sHion has been overcome by detailed examination and study, both in tiio field and with the micro.scope, carried on by many individual observers in large and widely separated districts, showing clearly that foliation and schistosity cannot be assumed to denote original stratification. The first really exact and satisfactory account of crystalline schists resulting from the nietumorphism of massive eruptives, was given as the outcome of the detailed work by Loss^n in the Hartz Mountains, who, as early as 1872*, directed attention to the deformation of diabases occurring in contact with granites, and showed the close analogy existing between the results of contact and regional metamorphism, as well as the production by metamorphic agencies of a foliated structure not connected in any way with stratification. The most important contribution, however, iu regard to the effects of dynamic metamorphism, appeared in 1884, from the pen of Prof. Johannes Lehmann, who after several years detailed studies on the origin of crystalline schists, based on a very large number of observa- tions, made chiefl}' in Saxony, but also in Bavaria and Bohemia, pub- lished his celebrated memoir on this subject.! The conclusion is reached that "gnt'iss" is simply a structural form of granular felspathic rocks, and as such is capable of subdivision according to composition into varieties corresponding with the types of the ordinary massive plutonics, while the prevailing parallel structure may be,but very rarely is, original. He regards these foliated rocks as of igneous origin and not in any way related to sedimentary deposits, the characteristic structure being developed as a result of " stretching " when the rock was in a solid state. It is further concluded that such rocks become more evenly and finely banded in proportion to the intensity of such " stretching " action. Daubr^e was also convinced that the schistose and foliated structures frequently assumed by massive rocks was not connected with original stratification, but secondarily developed as a result of pressure before the rock had wholly solidified. JNaumann emphasizes this latter fact, while Reusch, from studies undertaken in the vicinity of Bergen in Norway, also comes to similar conclusions. In England, Teall, from his examination of the metamorphic area in the vicinity of the Lizard in Cornwall 1 1 reaches results closely resembling those of Lehmann j *Zeit8chr. Deutsch. Geol. Gesell. vol. XXIV, p. 763, Berlin, 1872. fUntersuchungen iiber die Enatehung der Altkrystalliniachen Schiefei-gesteine. Bonn, 1884. JEtudes synthetiques de geologie Experimentelle, p. 432. Paris, 1879. liGeol. Mag., Nov., 1886. MMOW, 1 while ii Marylar and Ma has shov ginally u ation an( Lake dis various : were larg under an viscid, col plained a« ing or def Previou morphism sunken str by Lyell ai world-wide in the desii events as r should hav( itteating th -at revealir crust, asaci wellings of a series of part of fol denudation outward res undoubted which were 1 ation ; as we abundant rea resented by t intimate asso( have originate also cited as a sediments. S most classic b *Bull. U. s. tAnnual Rep MMOW. LAURENTIAN. 51 I while in the United States, in the gahbro area near Baltimore, Maryland, as well as in the greeustone-achist area of the Menominee and Marquette regions in Michigan, tlie late Prof. Geo. H. Williams has shown the secondary development of a schistose structure in ori- ginally massive plutonic rocks.* In Canada, Lawson,t from his examin- ^V^^k by ation and studies of the rocks of the Lake of the Woods and Rainy Lake districts, was the first to draw attention to the fact that the various foliated crystalline rocks usually classified as Laurentian, were largely plutonic rocks, which have crystallized slowly, probably under an extremely gradual diminution of temperature, from a thickly viscid, coherent or tough hydrothermal magma. The foliation was ex- plained as a result of " differential pressure which by causing a yield- ing or deformation, induced a flow in the mass." Previous, however, to the appearance of these results, the nieta- Metamor- morphism of sedimentary rocks occurring " as deeply buried and sunken strata " had been so clearly described and so strongly advocated by Lyell and others, that their views gained an almost immediate and world-wide credence and adoption. It is therefore not surprising that, in the desire to trace back as far as possible the sequence of tr ^logical events as revealed by the accumulation of stratified deposits, there should have been included at the base a complex of crystalline rocks ittesting the presence not of conditions favourable to sedimentation .at revealing the early unstability of the necessarily thin and weak crust, as a consequence of which it was probably peculiarly subject to up- wellings of the molten mass beneath. The ultimate result being a series of immense batholitic intrusions, composed for the most pait of foliated plutonic rocks, which subsequent upheaval and denudation have revealed at the present surface of the earth. The outward resemblance of these foliated or gneissic rocks to certain Restunblance undoubted clastic rocks, present in later geological formations, gtiiititied which were known to have undergone extensive deformation and alter- ''"''^^• ation ; as well as their interfoliation with truly bedded rocks seemed abundant reasons for their classification as one uninterrupted series rep- resented by this immense accumulation of stratified material. Their intimate association with crystalline limestones, which were believed to have originated in much the same manner as later calcareous strata, was also cited as additional evidence of their depoi'tion as ordinary aqueous sediments. Subsequent work in the county of Argenteuil, rendered al- most classic by the detailed labours of Sir William Logan, as well as *Bull. U. S. Geol. Surv.. Nos. 28 and 62. fAnnual Report Geol. Surv. Can., vol. I., (N.S.)., Part c, c, 1885. 52 I NIPiaSINO AND TEMISCAMINO RKOION. Difficulties at- tending first examinations. Use of micro- scope. in other extensive areas of Arch-Tan rocks in Canada, have since shown the fallacy of many of the conclusions then reached, and both Adams and Ells are firmly convinced that the undoubtedly clastic rocks pre- sent in the area usually considered as " typical " of the Laurentian, form but a small proportion of the rocky complex, while they are associated with and inclosed by much greater volumes of ^jneissic rocks closely allied in petrographical characters to granite, diorite and gabbro. In the early years of the Canadian Geological Survey, the advance of accurate and detailed information regarding these rocki was greatly retarded for iseveral very obvious reasons. In the first place, by far the larger portion of the country characterized by the presence of such rocks v/as a vast almost uninhabited wilderness of forest. The only access to such regions was by means of canoes, through obstructed and often little known routes of travel. These conditions have in a great many instances been improved of late years by the gradual settlement of the country and the necessary construction of roads. In the i-econd place, great difficulty was fo.' a long time experienced in obtaining trained and reliable observers competent to deal with the mtmy diffi- cult and complex problems presented. Sir William Logan, when carrying on his work in this connection, was often forced to depend for information covering many essential details, on observations by men scarcely possessed of the requisite qualifications. Thirdly, the extreme metamorphism and deformation to which all such rocks had presumably been subjected on account of their very great antiquity, and the absence of any known methods by which their original minute structures and mineraloj^ical composition could be deciphered, presented seemingly insuperable barriers to the complete and satisfactory explanation of tneir origin. In the fourth place, the very natural assumption that such rocks represented extremely meta- morphosed sediments, and the consequent application of the ordinary methods of geological research made use of in the much later and typical stratified deposits, served only to aggtavate the difficulties already existing. The adoption of the microscope for petrographical research removed the main difficultier attending a satisfactory study of these rocks, m.arking an era in geology, since which time the progress in exact knowledge has been rapid. In fact, i\:^ accumulation of reliable in- fofraation connected with this long-debated subject has already assumed saoh large proportions that many geologists look hopefully forward to the time when we ehail prooably possess an even more complete knowledge LAURENTIAN. 53 I of these rocks and their manner of formation th&n we now do of many more recent rocks. In 1844, when Logan decided l.o make an examination of the region 'iogan'a work bordering the Ottawa River, he found a mass of foliated crystalline 'Kiver.*"* rocks that seemed to him capable of subdivision into two conform- able series, although in this as well as many succeeding reports, he included them under the one group, which he subsequently called Lower Ll. arentian. The lower or older series consisted exclusively of "syenitic gnpi-is showing no end to the diversity of arrangement in which the minerals and the colours will be observed, but there id a never failing constancy in respect to their parallelism. But this though never absent is sometimes obscure." These rocks were sup- Sulxlivision posed by Logan to occur in the form f>f a low anticlinal arch in the .,,i(j Lower region extending from the Mattawa River to the vicinity of the com- I-iiiurentian. bined mouths of the Montreal and Matabitchouan on Lake Temiscam- ing. The upper series is stated to crop out in the district fo the south of the Mattawa and Ottawa rivers and to be characterized " by the presence of important bands of limestone which have undergone extensive cystp-llization as a result of extreme metamorphism," while the various gneissio rocks which separate the several bands of limestone "differ in no way either in constituent quality or diversity of arrange- ment from the gneiss lower down." Subsequently, this lower gueiss was called the " Ottawa Series,'' Ottawa and while the upper group, diflferentiated solely in the tirat place on account gj^"j^' ^ of the presence of the limestones, was included under the name Middle Laureiitian or Grenville Series. The name Upper Laurentian was Upper Lau given to a terrane formed chiefly of anorthositos which were after- ^"^ '' "" wards shown to be of irruptive origin, and with which were classified by mistake certain gneissic and limestone bands, identical in char- acter with those included as the Grenville Series and to which they clearly belong. In the district therefore covered by the Nipissing and Temiscaming sheets, the rocks to be described would, under the old classification, have been included as Lower Laurentian, although in the area to the south of the Mattawa River, precisely similar gneissic rocks, because of their inclusion of small isolated patches of crystalline limestone, have usually been described as of Grenville or Middle Laurentian age. These patches of crystalline limestone are only very occasionally present and are evidently caught up by and embedded in much greater volumes of gneissic or foliated rocks here of truly igneous origin. In such a way as to point to the conclusion that in tliese limestones we may have i i 1 5 ;(■',: ;- iT. 54 I NIPIdSING AND TEMISCAMINO BKGION. Use of torni Laurentiaii. Two groups of gneisses. ' i^ small remaining portions of a sedimentary series, which, although highly altered, have not been wholly absorbed by ihe surrounding foliated material. The term Laurentian, as applied in connection ■vith the map-sheets here under description, therefore includes only such granite and diorite gneisses as are usually characteristic of this ancient complex. The gneissic rocks exposed throughout this district fall naturally into two great groups. . An acidic group : — consisting of those foliated rock- similar in composition to granites, etc., to which they correspond, their differentiation being determined solely by their foliated tex<^' -' which usually pronounced, is sometimes obscure and occasioi ,y altogether absent. II. A basic group : — These rocks occur interbanded with the more acidic gneisses and represent either basic segregated portions of the granite magma, or foliated basic irruptives allied to diorites, diabases, etc., caught up in it. The results obtained from the detailed petrographical examination of the large number of thin sections prepared from typical specimens, specially selected as representing all the observed varieties occurring in the region, coupled with extended observations concerning their field relations, has furnished the most convincing proof that the vast majority of such rocks may be referred to some type of irruptive mat- erial. On the other hand, those gneisses whose origin may be in doubt and which are in some cases held to be sedimentary, constitute an ex- --. . . , ceedingly small proportion of the whole series. In fact, the results Sir A. lieikie. obtained from the examination and study are very closely analogous to the conclusions arrived at by Sir Archibald Geikie regarding similar old rocks exposed in the British Isles, who says : "These rocks are in the main various forms of eruptive material ranging from highly acidic to highly basic ; they form in general a complex mass belonging to successive periods of extrusion ; some of their coarse structures are probably due to a process of segregation in still fluid or mobile, pro- bably molten material consolidating below the surface ; their granulated and schistose character and their folded and crumpled structures point to subsequent intense crushing and deformation ; their apparent alter- nation with limestone and other rocks which are probably of sedimen- tary origin are deceptive, indicating no real continuity of formation, but pointing to the intrusive character of the gneiss." CARLOW. ] The( charact( 1. Cc the ider known many c; local we f>hism. In ord gneissic study in the Lab( are the n Silica Alumina Ferric oxide Ferrous oxic Manganous t Lime . . Magnesia . Potassa . . Soda Water at ioo ir above Tota I. Grani in previous toid gneiss massive anc parallel disf and only ve all continuo quartz, witl sericite, chh "Annual Re !l •] COMPOSITION OF GNEISSES. 01) I The chief facts which together seem to prove the originally igneous character of the rocks above referred to may be stated as follows : — 1. Composition of the gneissic rocks. — The microscope reveals at once the identity of these in mineralogical composition with the different known varieties of granite and diorite, the constituents present, in many cases, showing little or no alteration, except that produced by ^f gneisses. local weathering, or as a result of somewhat limited dynamic metambr- ^hism. In order to ascertain whether the chemical composition of these gneissic rockd would bear out the conclusions derived from their study in the field and under the microscope, six analyses were made in the Laboratory of the Survey by Mr. F. G. Wait. The following are the results : — * \n. ^\ Silica Alumina Ferric oxide Ferrous oxide ... . ManganoHs oxide. . . Lime Magnesia Potassa Soda Water at 100° C . . . „ above 100° C. Totals... . I. 71 CO 14-84 1-25 tr. 103 0-37 7 00 3 13 OlO 0-49 I II. 30 "6 a he u III. (59-39 17 -40 99-99 1-38 "2-14' 0-52 2-77 518 0-00 0-47 o a to 07-74 1(;-13 1-.00 l-9() tr. 4-41 1-30 1 30 4-92 0-10 0-80 IV. a tc VI S i ■S.2 Analyses. 99-37 100-28 07-50 66-94 44-92 18-23 17 -84 18 88 2-73 2-39 4-30 13-76 tr. 0-26 1-85 1-8G 9-07 1-56 1-82 5-38 4-25 3-36 0-53 3-79 1-85 2-94 0-08 015 0-20 0-90 1-75 1-62 100-55 99-87 100-29 I, Granitite-gneiss from west shore of Taggart Bay, Keepawa Lake — in previous reports usually referred to as red orthoclase gneLss, grani- toid gneiss or gneissoid syenite. The rock is of a deep flesh-red colour, I'esmption of r .... i/.].-!. gneisses, massive and granitic in appearance, the foliation being imparted by the parallel disposition of the coloured constituents. It is highly felspathic and only very occasional thin bands of basic material occur which are at all continuous. It contains much microcline, orthoclase, plagioclase and quartz, with much smaller quantities of biotite and epidote, Sphene, sericite, chlorite, apatite, allanite and zircon are present as accidental •Annual Rei>ort, Geol. Surv. Can., vol. IX., (N.S.) Part R., pp. 18-20. 'hi 56 I NIPIbSING AND TEMISCAMING REGION. i iM 3I ' m i Description of or secondary minerals. The rock has evidently been subjected to con- analysed, siderable pressure. The felspar and quartz have often undergone advanced granulation, while the surviving large individuals exhibit marked Lndulous extinction. Microcline, as might be expected, is abundant, as also areas of granophyre. II. Granitite-gneiss from south shore of McLarens Bay, Keepawa Lake. This was selected as representing the light reddish-gray granitic genisses so common in the district. The hand specimen shows a light- gray, rather fine-grained micaceous granitic rock, tinged with red oxide of iron, and showing only indistinct foliation. Composed of orthoolase, microcline, plagioclase, quartz and biotite with a little apatite, zircon, sphene, magnetite and occasional minute individuals of secondary muscovite and epidote. The biotite sho%vs a slight alteration to chlorite in some instances and occurs for the most part in small isolated plates, possessing a rude parallelism and rarely aggregated together. It shows only slight evidence of pressure. III. Granitite-gneiss from west shore. Lake Temiscaming at north end of Opiraika Narrows. A good average sample of the ordinary so-called gray-gneiss. Macroscopically, this is a very distinctly foliated rock, the foliation being produced by alternating bands of light and dark-gray colours. The darker bands are composed almost wholly of the coloured constituents while the light-gray portions are made up chiefly of quartz and felspar. The thin section shows quartz, orthoclase, plagioclase, biotite and epidote as the principal constituents. Epidote and titanite are common inclusions in the mica. IV. Granite-gneiss from the north-west shore of Leonard Inlet, Wick- steed Lake. The hand specimen shows a rather coarse-grained, grayish, indistinctly foliated rock, much stained with yellowish-brown iron oxide and showing large phenocrysts of white orthoclase. The chief minerals present are orthoclase, microcline, plagioclase, quartz, biotite and muscovite. Apatite, zircon, epidote, zoisite, allanite 1 and pyrite were also noted in very small quantities. The rock has evidently been subjected to considerable dynamic action. The muscovite is primary intergrown with perfectly fresh reddish-brown biotite. V. Cyanite-granite-gneiss from the east shore of the Ottawa River, half a mile north of Snake Creek. The hand specimen shows a coarse- grained granitic rock with a distinctly banded structure caused by layers rich in biotite, alternating with layers of quartz and felspar comparatively free from that mineral. The distinctive feature of the rock is the abundance in portions of it of a light, to deep-blue cyanite, in large columnar individuals, some of which are half an inch across and an inch in length ; garnets of a deep pink colour are also plentiful, ■ARIOW. ] COMPOSITION OP GNEISSES. 57 I I* and some individuals are as much as half an inch in diameter. Under the microscope the rock is seen to be composed of orthocla.se,plagioclase, quartz, biotite, cyanite and garnet with smaller quantities of muscovite, graphite, titanite, zircon, apatite, pyrite, pyrrhotite and epidote. The rock is typically holocrystalline and granitic and shows no extreme evidence of granulation. VI. Quartz-mica-diorite-gneiss from Ottertail Creek, lower end of the 2nd portage above the junction with the north branch. In the hand specimen this is a dark-gra}-, almost black, glistening, evenly foliated rock stained in places with iron oxide. lb is composed of plagio- clase, orthoclase, quartz, hornblende and biotite, with sphene, apiitite, zir. con, pyrite, magnetiteand limonite as accessory minerals. The hornblende is much more abundant than the biotite. The evidence of pressure is very limited. The rock constitutes the dark basic bands so character- istic of exposures of the gray gneiss. Time would not permit of the separate analysis of each rock-type included in the accompanying table, and therefore no attempt can be <^/neral result t J 's > r of examiationa made to institute comparisons in detail with the published analyses of granites and diorites. Sufficient has been done, however, to show somewhat clearly that in general these foliated rocks bear a close analogy in chemical composition to their massive equivalents, while on the other hand, they are quite different in this respect from any rock resulting from ordinary processes of sedimentation. As Dr. Adams remarks,* the points of distinction and those which mark them as of igneous origin are, high silica, combined with low alumina and big., percentage of alkalies. The lime also, as is usually the case in granites, is in excess of the magnesia. It would seem, however, that the granite- gneisses, as a rule, are more basic than their massive equivalents, although presenting an equally wide range in their silica contents. The decrease in silica is accompanied by an increase in tht alumina, while soda tends to exceed potash in the more basic varieties thus marking a passage to the gabbros and diorites. The high percentage of alumina with low alkalies noticed in No. V. is due to the presence of cyanite, but otherwise the composition is essentially similar in every other respect to the ordinary granitites of this and other Archican districts. There is as is usual in granites, the preponderance of lime over magnesia which though slight in this case, is nevertheless in marked contrast to the sillimanite gneisses described by Adams* where the magnesia is often nearly three times as abundant as the lime. i hi > A W 1 :il!^ "Annual Report, Geol. Surv. Can., vol. VIII. (N.S.) Part J, p. 44. i 7 ■ n 58 I NIPISSING AND TEMISCAMING REGION. |-Si i- :i-, {< i i ! ^It •) ' The quartz-micadioi'ite ^VI.) is analogous in chemical composition to the most basic phases of the gabbros and diorites. The hornblende and biotite are much more abundant than the felspathic constituents, while quartz is only very sparingly represented. Structure.!. 2. Microscopical structure. — The various thin sections examined, show unmistakfcbly the holocrystalline structure so characteristic of granite, diorite and gabbro, the felspar and quartz individuals forming comparatively large areas of interlocking grains, especially in the more acidic portions or bands in the rock, with which are associated the hypidiomorphically developed bisilicate constituents. There is no sug- gestion whatever, in the great majority of such rocks, of the secondary enlargement which in certain arkoses and quartzites pro- duces a somewhat similar interlocking arrangement, as the rocks have, in many instances, been subjected to but limited metamorphic action. The foliation, which is the differentiating characteristic of these rocks, is often so coarse that it is only apparent in large specimens or some- what extended exposures of the rock. This parallelism is, therefore, often indistinguishable with the microscope, so that in the thin sections the resemblance is complete between foliated and non-foliated varieties of such essentially similar mineral aggregates. At the present day, fused magmas are regarded as a more or less complex solutions, which, by reason of their high temperatures, obey the same laws in the order and method of their solidification as those which govern the crystellization of ordinary solutions of a similar Order of heterogeneous composition. Thus, in the numerous thin sections generation. examined, a certain general and definite order is observable in the generation or crystallization of the various component minerals that has been rather closely adhered to in the progress of consolidation. In this manner zircon, sphene, apatite and primary epidote, which are the first to form in the slowly cooling mass, are almost invariably present in shapely outlined and well developed crystals, evidencing considerable freedom from restraint during the progress of their formation. The various iron ores which may happen to be present, are of earlier generation than the coloured or bisilicate individuals, which latter are usually present with hypidiomorphic outline, although occasional individuals often show sharp and well delined crystallographic bound- aries. The customary grouping together in masses or nests of such basic material, produces a mutual interference of the constituent individuals which militates greatly against perfection of crystal boundaries. The various apatites, sphenes, etc., which are the first minerals to form in the cooling rock-mass, usually occur, as might be expected, either 4. Jjij line of ju doubted and detai between which Jat gneissic rt respect to ^f BARLOWc ] COMPOSITION OF GNEISSES. 59 I embedded in, or in close conjunction with such ferro-magnesian con- stituents, although the rest of the rock, while much poorer relatively in such minerals, mplication of pressure. The somewhat uniform direction in strike of this banded structure, I'lnfomiity of over the larger portion of the area covered by the accompanying map- *■'"'• sheets, and its marked correspondence indirection with the line of out- crop of the neighbouring stratified Huronian rocks, seem to point to the conclusion that the resistance off'ered during the irruption of these gneisses by such hard strata, has been the irtain determining feature of the direction of foliation. During the progress of this igneous invasion, the forces of upheaval acted along certain definite lines or centres, thus producing irregular ovoid forms, often of great area, the inner Snuctmal portions of which are now occupied by comparatively fiat-lying gneisses, or, in occasional instances, by more massive or granitoid varieties, sur- rounded by an outer border or zone where the foliation becomes much more pronounced. In certain instances, where the dome-like structures thus produced have been denuded, and are of limited extent, a great diversity exists in both the direction and angle of dip of the foliation within a comparatively small area, but where, as is usual thoughout this district, these ovoid areas are of great size, the direction of foliation shows a corresponding increase in uniformity. Intimately associated with these gneisses and granites, are certain portions, often of themselves constituting considerable and there- fore important rock-masses, which, on account of certain peculiarities of composition, as well as from their structural relations with the surround- ing rocks, have been commonly referred to as " pegmatite," and which by ivgtnatite. reason of their usually coarse crystallization have been sometimes called "giant granite." Haiiy first applied the name pegmatite to the intimate admixture of orthoclase and quartz, also known as graphic granite. Later, Naumann extended its u.-e to include all the coarse varieties of muscovite-granite, vein-like in appearance and fre- quently containing tourmaline. Subsequent writers, as detailed inves- tigations into its composition and origin proceeded, have still further .' J' mi: !! 62 I NIPISSINQ AND TEMISCAMINO RRGION. widened its use, until, at the present day, the employment of the term in connection with that of the parent plutonic mass with which it is associated is necessary, before any definite idea can be formed of its Ufle of terms, precise mineralogical composition. In petrography the terms micro- and macro-pegmatite have always been used in a structural sense only, to denote those intergrowths of quartz and felspar, or of two differing species of felspar which are sometimes characteristic of occurrences in rocks of these minerals. Thus the various plutonic masses of syenite, diorite, gabbro and diabase, may each have their individual pegmatitic equi- valents, representing the final product of their solidification, although the abundance of such aggregates in connection with these rocks is much less than in the case ot granites. This com. parative iufrequency is perhaps most adecjuately explained by the relatively much greater basicity of such rocks, their more rapid rate of cooling, as well as the comparative scarcity, throughout the greater portion of the mass, of any such abundant and intimate assoc- iation of fused rock and heated water as would tend to their for- mation ; for, while it has been clearly shown by M. Fouque and Michel-Levy, that diabase and similar basic rocks may be artificially reproduced in the laboratory from a state of simple dry fusion, it is extremely doubtful whether any extensive intrusive process produced by natural causes is ever unaccompanied by a greater or less abun- dance of superheated water as an integral portion of the fused mass. In the region under description, the granite pegmatites are, as usual, by far the most abundant, but there are occasional dykes in which the occurrence of oligoclase and hornblende as the main constitu- ents would determine their classification with the diorites. Composition of pegmatite. In composition, these pegmatite masses consist essentially of quartz and the more acid felspars, chiefly orthoclase, oligoclase, albite and microcline, while muscovite is the prevalent ferro-magnesian con- stituent, when any is present, and hornblende and biotite are much less characteristic. The parallel intergrowth of orthoclase and albite to which the name perthite lias been applied, is an abundant and sonje- times prevailing felspathic constituent of the pegmatite dykes, especi- ally in the vicinity of Mattawa. The composition is therefore some- what variable, but these dykes or vein-like masses are essentially simi- lar, though somewhat more acid than the normal plutonic rock ox which they represent the most highly differentiated or final product of con- solidation. Thus, in those areas where the gneissic rocks contain a sup- erabundance of basic material, with plagioclase as the predominating felspathic constituent, the associated pegmatite usually shows a cor res ■AHIOW J ponding most abi pegmatil ponderar region, is pegmatit muscovit normal p, ance of h of the iro the miner The pej to call for In other d developme pegmatite Claire stat are usually some of tl; by Mr. R. locality by com para tivi an abundan Erables rap its most per acid bands abundant a gneisses nea east of Matt of the Iarg( however, a c The intrus that the vari manner due i disproved, wl phase or final lization of cei *Annual R« March, 1899, p. ■J COMPOSITION OF QMISSES. 63 I ponding increase in relative basicity, oligoclase seemingly being the most abundant felspar. In areas of hornblende-granite, the associated pegmatites contain hornblende as the coloured constituent. The pre- ponderance of the granitite gneisses or hiotite-granite-gneisses in this region, is represented also by a far g»-eater relative abundance of the pegmatitic phases of such rocks, while the far greater prevalence of muscovite, which usually occurs altogether replacing the biotite of the normal parent plutonic, evidences the presence of the greater abund- ance of heated water tending to the more or less complete elimination of the iron present in this bisilicate and the consequent conversion of the mineral into muscovite. The pegmatites have not yet been examined sufficiently in detail Accessory to call for any lengthy mention of their accessory or accidental minerals. In other districts these masses are especially noted as favouring the development of many of the more unusual and rare minerals. In a pegmatite dyke cutting gneissic rocks about a mile north-west of Eau Claire station, opaque crystals of beryl occur. The crystals secured are usually of a pale yellowish but sometimes of a bluish colour and some of them would exceed five pounds in weight. An examination by Mr. R. A. A. Johnston, of some specimens collected from the same locality by Mr. C. W. Willimott, showed likewise the presence of the comparatively rare minerals, xenotime and polycrase. Cyanite, although an abundant constituent of the granitite-gneisses in the vicinity of Les Erables rapids and the mouth of Snake Creek on the Ottawa, exhibits its most perfect crystallographic development in the coarser and more acid bands which are evidently of pegmatitic origin. Fluorite is also an abundant and frequent constituent in the pegmatites cutting the gneisses near the Ottawa in the township of Cameron, about five miles east of Mattawa. In the necessarily more or less hurried examination of the large number of these pegmatite masses, there was found, however, a conspicuous monotony in composition. The intrusive character of pegmatite is now so generally recognized, that the various theories, formerly extant, regarding it as in some manner due to aqueous infiltration and deposition, may be considered as ^ . . 1. 1 , ., , . , . . , Tntrusive in disproved, while the view that pegmatite constitutes the most acid cliaracter. phase or final differentiation product attending the progressive crystal- lization of certain intrusive plutonic rocks has been very clearly and *Annual Report, Geol. Surv. Can., vol. IX. (N.S.) p. 13 R ; also Am. Jour. Sc, March, 1899, p. 243 : also Summary Report Geol. Surv. Can., 1898, p. 167. U 64 I NIPISSINO AND TEMISCAMlVa KEOION. OpinioiiH of .Messrs. W. () C''rosl)y and M. F. Fulinr. Forniiition of lie^fuiatite. ably set forth by Lehniiinii*, Broggerf, Williams J and others, and all have given expression to the opinion that water played a most import- ant role in their formation. Probalily the most satisfactory explana- which has yet appeared, is that lately issued as the joint production of Messrs. W. O. Crosby and M. L. Fuller, (^f Boston. S These author.s recognize " that the most satisfactory explanation of this blending of the pegmatite with quartz vvina on the one hand, as with the normal granite (m the other, is to be found in a corresponding blending of aqueo-igneous fusion with igneo-acjueous solution ; and this dynamic gradation, it appears to us, can only result from the gradual hydration of the residual magma during the slow centripetal solidification of a body of magma and a consequent elimination of water." Til ihis paper the authors further state that pegmatite should be regf.ided, " not as a distinct specie.i or family of rocks, but rather as a possible textural phase of all, or nearly all, the plutonic rocks ; and we may, in general, say of any plutonic rook, that it may be crypto-crystal- line, microcrystalliue, macro-crystalline or pegmatitic." The consensus, therefore, of recent opinion, seems to favour an intrusive origin for pegmatite, the progressive increase in hydration of the residual magma being explanatory by a corresponding increase in acidity of its later crystallization. The stages represented completely by the occurrences in this region, show a perfect and practically uninterrupted continuity during the consolidation of these rocks, from an original condition of hydro-igneous fufion characteristic of the magma from which the comparatively fine and even-grained parent plutonic is generally believed to have resulted, to conditions of aqueous solution which must have obtained in the viscous mass from which the latest quartzose segregations have solidi- fied. Such views are in harmony with the known occurrences of most of the quartzose masses and veins, so frequently present in these Archa'an rocks, and which have evidently originated by a process closely allied to that described above, in consequence of the deposition from super- saturated solutions of highly siliceous material, and are substantially contemporaneous with the parent plutonic mass with which they are so intimately associated. *Ueber die Entsehung der altkrystallinischen Schiefergesteine 1884, p. 24etBeq. f Die Mineralien der Syenitpeginatitgiinge der siidnorwegisphen Augit und Nephe' '' syenit I, Theil pi). 21.5-225. Translated by N. N. Evans, Can. Rec. Sc, vol. V No8. 2 and 3, pp. 33-4(5 and (Jl-71. JOrigin of the Maryland Pegmatites, XVth Ann. Rep. U. S. Geol. Survey, pp. 675-686. §Technology Quarterly, vol. IX., No. 4, December, 189G, pp. 326-356. MKLOW Thi as tht covite sion ij of idi quarts crysta ment ( these occur n crystal especia! seems materia stricted not onlj partialis composii The e formatio plutonic progress Of receni holocryst plutonic to a porp pointed o posed mat the progr( The ino masses, is striking cf plutonic ro of the quai "olely to la Liiat It is between th t- aiewhat i presenting walls, and is often occu 5 •] COMPOSITION OF ONEISSES. 65 I The nge relations of the component minerals are practically the same A^'i- lulatidnM 1 • .1 1 , !• 1 • 1 nil 1 • ,.•! of coIIllHpnfllt as that in the more usual types or plutonic rocks. Ihus biotite, mus- niiiunilH. covite, and the more basic felspars, crystallized out in regular succes- sion in the order mentioned, showing a gradual decrease in perfection of idiomorphic development. The more acid felspars, and finally the quartz follow, the latter, especially, showing little or no evidence of crystal boundaries, occupying the interspaces left by the earlier develop- ment of the more basic constituents. When drusy cavities exist in these pegmatites, as well as in the quartzose and more vein-like occurrences, the silica sometimes exhibits a decided tendency towards crystalline development. The presence of such unfilled spaces, especially in the immediate vicinity of such perfect crystal forms, seems to furnish evidence of the insufficiency of the siliceous material in solution to fill the spaces, permitting a more or less unre- stricted development of the remaining quartz. They likewise point, not only to the extreme acidity of the last remaining portion of the partially solidified magna, but also to its approximately homogeneous composition. The exact depth below the earth's surface necessary for the formation of these pegmatites and their parent masses of normal plutonic rocks, as well as the amount of pressure during the progress of their crystallization, is a mere matter of spe-^ulation. Of recent years a perfect gradation has been traced from tha typical holocrystalline structure characteristic of granite, gabbro and other plutonic rocks, in a vertical distance of a few hundred feet upward, in- to a porphyritic phase at the surface ; while the pressure required, as pointed out by Brogger, would be obtained by the presence of superim- posed material, great enough to prevent the water, separated out by the progressive crystallization, from escaping freely to the surface. The most distinctive feature concerning the development of the; e Coarse coxtnie masses, is their extremely coarse crystalline texture, which is in very I'fKin'itite. striking contrast to the normal or usual crystallization of the parent plutonic rock with which they are associated. The resemblance in many of the quartzose varieties to quartz veins, originally regarded as due solely to lateral secretion and aqueuus deposition, is so very marked that it is difficult to see how any hard and fast line can be drawn between these separate occurrences. Usually in these cases there is a aewhat indistinct zone-like arrangement of the material, the masses Some quartz presenting a finer grained felspathic portion in the vicinity of the ^n."titic* m walls, and showing a continuous transition towards the interior, which orij^in. is often occup' d by comparatively large allotriomorphic masses of almost 1 H If s n-: i i' z 66 I NlPISSIXr; AND TEMISCAMING IlEGION. pegmatite. Coin])()sii:iop of i)fgiiiatitt', pure quartz. Uaually there is a perfect gradation into the parent plutonic whan this is the inclosing rook-mass, while an undoubted passage can very frequently be traced into areas of pure quartz, and occasionally into rather typical or ordinary i[uartz veiixS. Two phases of In the rt^gion embraced by this report, there are two somewhat distinct plif.aes of such rocks. The most frequent and abundant is perhaps represented by the acidic facies of the gneisses constituting the coarser and more felspathic and quartzose bands. These present ail the distinguishing characteristi<;s of pegmatite, jilthough occurring in perfect conformity with the prevailing fc'.i.cion. In composition they show the usual great preponderance of felsf>ar and quartz, with only very occasional flakes of biotite, which in many cases hns undergone notable bleaching owing to the 'elimination of a considet-able pro- portion of the iron originally present. Such biotite is much paler in colour, with less marked pleochroism, and shows the brilliant clu'omatic polarization colours, though p^;i'haps in a less degree, so characteristic of the lighter' coloured mica. The most frequent and abundant coloured constituent, however^ is muscovite, which in some cases, at least, is an original constituent, although a great deal has undoubtedly resulted from the alteration of the biotite. These pegmatitic bands very evidently re|iresent the residual and more acid portions of the magma which liave crystallized iti situ, and may be referred to as examples of what has been called "sedentary pegmatite." They usually show a perfect, tliough somewhat rapid, transition into the more basic bands imiiiediatt;ly adjoining, and are therefore to be regarded as more strictly contemporaneous than those constituting the second mode of occurrence. These are masses or apophyses of residual and con- se(iuently more fully hydiated and acid portions of the magma, which have invaded and tilled various cracks and fissures occurring in the gneissic massif or in the neighbouring clastic ''icks. They are usually present in more or less marked conformity with the foliation of the gneissic rocks, but very often fill rifts which intersect this at consider- able angles. Although in the detail of their structural relations, many of these occurrences are obviously newer than the associated gneisses, the general examination of the masses throughout the whole area seems to show that they must be regaided as substantially of the same age. The process of crystallization was evidently practically continu- ous, from the first development of the earlier constituents in the still molten and ^'^scous magma to the filling in of the most minute cracks and fissures by the remaining quartz, marking the final step in the complete solidification of the whole masn. Intimately associated geneti- cally with these pegmatites, are certain veins and even veinlets of quartz. Sedentary pegmatite. Structural relations. Relative age. Metliwl of formation. sometin. the prev These ar contact 1 and it se tions of si of the nu so freque In thoi present h position, 1 parallel al or nuclei c uents. S than the r erable mas the irrupti are simply they merg( both are sti to the norti and Anniff more or le scales resul This foliati slates on tl centre of t end of Ore glomerate o but which J foliated gne basic mater ever expose and microcl tion of a rat passes by ir exposed on field station rock is 80 m Wl lere g» magma has ■ARU>«i ] OOMPOSITION OP GNEISSES. • 7 I sometitL containing felspar, which penetrate and anastamose through Origin of some the prevailing gneisses as well as through the clastic rocks of this district. ^'"'^' These are especially numerous and M-ell developed along the lines of contact between the various plutonic masses and the Huronian elastics, and it seems probable that by far the greater number of these infiltra- tions of secondary quartz are due to the extravasation and differentiation of the numerous large masses of these deep-seated irruptives exposed so frequently throughout this area. Foliation of liouiogoneoiis gniMssos. Kt'!ati .t" age. Granite around Anninia- lll'.llllSS Tjake. "g In those portions of the area coloured as Lanrentian, wher^ the rocks present have solidified from r. magma more or less homogeneous in com- position, the foliation generally present is seen to consist usually of a parallel alignment of the biailicate individuals, or, at most, of small nests or nuclei composed of an aggregate of scales or fragments of such constit- uents. Such rocks are in many instances of somewhat later generation than the more evenly foliated gneisses, and frequently contain consid- erable masses or fragments of these that have been caught up during the irruption of the former. At other times, such homogeneous masses are simply more granitoid portions of the prevailing gneiss, into which they merge both across and along the strike of the foliation, so that both are strictly contemporaneous with one another. The area of granite to the north-east of Lake Temagami, especially in the vicinity of Carrying and Annima-nipissing lakes, has a marked foliated texture, due to the more or less parallel disposition of aggregates of greenish chlorite scales resulting from the decomposition of the biotite originally present. This foliation is more pronounced near the junction with the Huronian slates on these lakes, gradually fading on passing inwards towards the centre of the mass. On Lake Teraiscaming, as well as near the south end of Cross Lake, the Laurentian in contact with the breccia-con- glomerate of the Huronian is a massive granite, very poor in bisilicates, but which gradually merges southward into very typical and evenly foliated gneiss, showing the usual alternating sequence of acidic and basic material. In the vicinity of Lake Nasbonsing, the rock, where- ever exposed, is a massive flesh-coloured gneiss, very rich in orthoclase and microcline, while the foliation is produced liy the parallel disposi- tion of a rather sparing quantity of hornblende ard garnet. This rock passes by insensible gradations into the more evenly foliated varieties exposed on the north sliore of the lake between Nasbonsing and Bon- fleld stations, although in the vicinity of Bonfield station itself, the rock is so massive thaL little or no structural details could be traced. Where greater ln^tarogeneity in the original composition of the Foliation > if magma has prevailed, the foliation present shows a correspondizig fil!^,!**" Ijaurentian on Tcniiscaiiiing and Cross Lakes. (ini'issof Lake Xaslxjnsiny. 5i ogt'iieous composition. i 68 I NIPISSING AND TEMISCAMING REGIOX. ''I; fill il . H^ i m Structural relations. Methtid of formation. Dynamic a.^tion. increase in the perfection of its development, consisting cas it does of alternating bands of lighter and darker coloured material, representing numerous varietal forms of rock-types which may be referred respect- ively to either the acidic or basic gn.ups already mentioned. This foliation it is which generally characterizes the rocks exposed in the area covered by the accompanying map-sheets. The component bands are of variable thickness. Occasionally there is an exceedingly sharp line of demarcation between the alternating folia, but as a general rule there is a complete, though somewhat rapid transition from one to the other. Even in their subordinate arrange- ment the constituent bands show the same marked tendency towards parallel arrangement, and a thick bed of prevailing felspathic com- position will, in cross section, present .short dashes or small patches of biotite or hornblende all drawn out in one direction ; while, on the other hand, the more basic portions show a similar definite arrange- ment of long lenticules of lighter coloured material, in which a relatively greater amount of felspar or quartz is present. The continuity of these folia, both large and small, is broken at frequent intervals, some- times abruptly, but usually by a gradual thinning out in either direction. Frequently, before such interruption takes place, bands of essentially similar composition may be formed immediately above or below, which in tui*n pinch out in both directions to be again replaced by others. This irregularity in horizontal arrangement is equally true of their downward or vertical extension, so that the whole section, of even a small area of any such rock-exposures, presents an exceedingly compli- cated arrangement of lighter and daiker material of greatly varying acidity and basicity. It is quite evident from their macroscopic arrange- ment, that their formation was attended with an extremely gradual diminution of temperature, for the frequent absence of sharp lines of demarcation between these bands of widely different composition, seems to point to the re-absorption by the later and more acid portions of the magma of the first formed or faster cooling basic portions, perhaps many limes repeated before the final consolidation of the whole mass. In many places, the dark bands evidence the action of extensive crushing and crumpling, showing that great movements have taken place in the whole series. These movements were doubtless approxi- mately synchronous, and closely connected with tlie invasion and cooling of the more .acid portions of the magma. The most curious and coniplicated structures are thus often produced, this complexity being enhanced by the frequent dislocation, accompanied sometimes by considerable separation and displacement, of those portions which BARLOW 1 COMPOSITION OF GNEISSES. 69 I evidently existed originally in unbroken continuity. Such intricate structures are, however, usually extremely local in their development, the gneiss elsewhere in the vicinity often showing little or no sign of extreme disturbance. Although, as a general rule, the direction of this foliation shows a marked uniformity over large areas, there is a con- siderable diversity in arrangement in this regard, as indicated on the accompanying maps, A careful correlation of the many observations made, shows clearly Mode of that these gneissic rocks occui- for the most part in the form of large "'^''"''''snce. rudely oval or concentric masses whose longer axes have in general a direction according with the prevailing strike of the foliation. Fre- quently such large ovoid masses present quaquaversal dips, which in cross-section simulates the ordinary anticlinal arch. About a mile east of Mattawa station, the Canadian Pacific Railway cuts through a small Structural dome of these gneissic rocks, composed of beautifully sharp alternating '^''' "'^'^'^* felspathic, micaceous and quartzose bands, showing a remarkably per- fect example of very pronounced differentiation. The section as pre- sented on either side of the railway track, presents a marked resem- blance to a low anticlinal dome. Plate III. The truly igneous character of the composing rocks, however, v^ould not permit of such an interpretation. In size these ovoid masses vary greatly, some of the curvings belonging to ellipsoids many miles in diameter while others are a mile or less in diameter. As a rule the folia or lamince have a prevailing dip to the south-east or south, which is singularly uniform over large areas. This inclina- Dip. tion is generally rather steep, usually considerably over 45°, while, frequently, as in many places along the shores of Lake Temiscaming, the foliation is almost, if not quite, vertical. On Seven League Lake and southwards to Mattawa, as well as westwards to Tomiko Lake, the bands frequently succeed one another in almost hori- zontal succession, the dip, if any, being generally southwards at a low angle. Even in this area, however, there are frequent exceptions to this rule, and the rocks often show a rapid change in this prevailing horizontality as though the bands had been subjected to frequent disturbances and dislocation during the progress of their formation. Thus in the vicinity of North Bay and the northern portion of Lake Nipisiing, the gneisses often approach a vertical attitude, while on the southern shores in the vicinity of French River, similar rocks are nearly horizontal. 'i i; 70 I In Work by iMesHi'H. Kerrier uirI Barlow. Ohject of studies. Classificatiiiii of glU'isSft^. Princi|)li' of classificati(jn. NIPISSINO AND XEMISCAMINO REGION. PBTKOGRAPHY OF THE LAUBENTIAN. The petrographical work done in connection wich the present report was carried out with the co-operation of Mr. W. F. Ferrier, Litliologist to the Geological Survey, to whom credit must be given for many of the results obtained. The writer and Mr. Ferrier worked in conjunction on the problems involved and with so free an interchange of ideas throughout, that no attempt will be here made to separate the examinations, more than to mention that many of the more critical specimens were made the subject of special study by Mr. Ferrier. The main object of these detailed studies has been, not only to obtain more accurate information with regard to the composition and minute structures of the various rocks, but also to gain an increased know- ledge of their origin and the relationship existing between the alter- nating bands of relatively greater or less basicity. Incidentally, a table has been prepared, showing a classification of these old crystalline rocks, displaying not only their composition, but also their close affiliation with one another. This table may recom- mend itself to petrographers, as it has done to the authors, and it is hoped may be found of material use in future work undertaken in areas of similar Archaean gneissic rocks. Much microscopical work has also been accomplished in connection with a series of specimens taken as illustralive of the various contact phenomena exhibited along the line of junction between the Lauren- tian and Huronian. This has enabled a more accurate interpretation and description of the various facts having reference to the relative ages of th^-^e two series of rocks. Field-work, no matter how careful or extended, in areas characterized by the presence of Archtean strata, must of necessity lose much of its value if unaccompanied by concurrent petrographies) 1 studies. In the present instance, the results have been adduced, not only from a critical and extensive examination of the numerous rock-exposures in the field, but also by a careful correlation of the facts thus ascertained with those acquired in the petrographical laboratory. Classification. Any system of classification applied to sucli a series of foliatefl rocks must, necessarily, in some respects, be unsatisfactory ; but a grouping together according to their mineralogical composition seems on the BARIOW. I whole knowlf As a petrogi allied i plutoni might 1 sometiu ance or It mi arbifcrar to a cer excludir petrogra examine referred. Xo ati collected selected i As pre two greai dominant Biotite is first divis The fir; on the Arranged collectiop. 1. vj-nui epidote. 2. Gnei 3. Gnei 4. Gneii 5. Gneis biotite. 6. Gneif 7. Gneis Tlie rela be seen by i I ■] PETROGRAPHY OF THE LAURENTIAN. 71 I ation. whole to be the best that can be cadopted in the present state of our knowledge. As already stated, however, there cau be no doubt that all of the petrographical types represented in the gneisses from this region are allied iu their chemical composition and mineral constituents to such plutonic igneous rocks as granite, syenite, diorite, gabbro, etc., but, as might be expected, there is a passage from one rock-type to anotlier, sometimes gradual, sometimes very abrupt, according to the abund- ance or scarcity of certain minerals. It must be borne in mind that the classification here adopted is an 9''^*"^**^^. . » , classificati arbitrary one, based on the mineralogical composition of the rocks, and to a certain extent on variations in their structure, the object bein;.;, excluding theoretical considerations, to establish certain well defined petrographical types that have been found to be constant in the area examined, and to which specimens from other districts may be referred. No attempt has been made to examine minutely all the specimens collected, but good examples of the more prevalent types have been selected and described in detail. As previously stated, the gneisses of the region may be placed in pnoissesdlvis- two great divisions, the acidic, characterized by orthoclase as the pre- great classes. dominant felspar, and the basic, by the predominance of plagioclase. Biotite is by far the most abundant ferro-magnesian constituent of the first division, and hornblende of the second. The first division may be subdivided into seven groups, dependent Acidic on the presence of one or other of the coloured constituents. divid^Hnto Arranged, approximately, according to frequency of occurrence in the '**^^'p» groups. coliectiot\ tlijy are as follows ; — i. Criuisses characterized by the presence of biotite and primary epidote. 2. Gneisses in which biotite alone is present. 3. Gneisses in which both biotite and rauscovite occur. 4. Gneisses in which hornblende accompanies the micas. 5. Gneisses in which cyanite, graphite, garnet, etc., accompany the biotite. 6. Gneisses in which hornblende alone is present. 7. Gneisses in which muscovite alone is present. The relationship of these rocks to their analogous massive types may be seen by reference to the accompanying table. I ' 9f k' r Two varieties of l)asic gneisses. No arbitrary line possible. Absence of augite. '2 I NIPISSING AND TEMISCAMING REGION. Of the second division, the basic, or hornblende gneisses, two varie- ties may sometimes be distinguished, first, those which represent seg- gregated bands of the more basic material of the original granitic magma, and secondly, those which are undoubted basic eruptives folded-in with the more acidic gneisses. It is not always possible to make this distinction, but examples of each of these two varieties have been observed. Classified according to their mineralogical composition they naturally must be placed close to each other. Amongst the first, whilst certain names have been applied to individ- ual specimens, it is manifest that no hard and fast lines can be drawn in the field. For instance, a band of which one portion would have the mineralogical composition and characters of a quartz-mica-diorite may pass insensibly into material having all the characters of a horn- blende-granitite, according as the plagioclase diminished and monocli- nic felspar increased in quantity. One remarkable fact in connection with these basic bands, is the great scarcity in them of augite, none of the hornblende containing cores of that mineral, or affording any direct evidence of having originated from it. In the Laurentian area lying to the north of the Island of Montreal recently described by Dr. Adams,* on the contrary, the basic bands in the gneiss appear to consist largely of pyroxene rocks. /. — 2'he Granite-gneisses. Orthoclase gneiss. Composition. In colour these rocks range from a light-gray to a decided red. The red rocks represent what has usually been called by the older writers on the Archaean, the "red orthoclase gneiss," but we find in the field every gradation from the gray to the red gneiss, the one passing im- perceptibly into the other in many localities, and the microscopical examination has failed to detect any essential point of difference between these two varieties. The red gneisses contain a large quantity of hydrous iron-oxides distributed through them, to which the coloration is due, and they * Annual Report, Geol. Surv. Can., vol. VIII. (N.S.), Part j,, 1890. 1 BARLOA J PETROGRAPHY OF THE LAURENTIAX. 73 I also appear to have a larger proportion of microcline than the gray ones. Plagioclase was not observed to exist in any greater quantity in the gray varieties than in the red ones. Many of the more altered mica-gneisses have assumed a dark-green Chloritization colour, owing to the chloritization of the biotite, but microscopic ex- ' J"'*''"- amination shows that they may be included in the same class as the typical unaltered ones. These chioritized raica-gneisses have been freciuently, though erron eously, sp>)ken of as hornblende-gneisses by the earlier geologica' observers in this region, who were misled by their colour, and had not the advantages afibrded by microscopical examination of the rocks. A remarkable feature of these gneisses is their comparative freedom from iron ores. When pyrite occurs, it is almost always associated with large clove- brown sphenes. In the case of the micaceous gneisses, i.e., those in which biotite Scarcity of alone, or biotite and muscovite together constitute the predominating liornblende. ferro-magnesian constituents, hornblende was observed in only two instances, and then in minute quantities. The almost total absence of augite from these rocks is to be parti- cularly noted. Even in the basic hornblende-gneisses of the region, this mineral is very rarely, if ever, to be found. A. Biotite muscovite gneisses — [Granite-gneiss). — The rocks grouped structure, together under this heading are, like the other gneisses, holocrystal- line and granitic in their structure. Both biotite and muscovite are present as the chief, and in fact almost the only coloured constituents. These two micas occur intergrown with each other in aggregates of Composition, broad fresh plates. The specimens representing this rock-type a"e, apparently, not very numerous in the collection. Those examined are remarkably free from epidote, iron ore and titanite. Orthoclase and microcline are the predominating felspars, and granophyric intergrowth of the quartz and felspar is a common feature. B. Muscovite-granite-gneiss— {Pegmatite in part). — The rocks thus designated and classified, are of comparatively rare occurrence as strictly integral portions of the gneissic complex, and where present constitute the latest secretions from the original magma. 74 I NIPI8SING AND TEMISCAMING REGION. ComiKDHitioii of muHcovite- granite-gneiss. I Iff: II! I I (Iranititi^ gneisses. Biotite- epidote- giieisa. Biotite-gneiss. In reality they represent interfoliated bands of pegmatite, although of much finer texture than the rock to which that name is usually applied. In colour they are wliite, light-gray, or pale-pink, presenting glistening or pearly cleavage planes. Under the micro- scope they present the usual interlocking holocrystalline aggregate of quartz, orthoclase, plagioclase (oligoclase) and microcline, with a smaller amount of sericite (hydrous muscovite) arranged in long drawn- out scales, and plates which traverse the rock in curving and approximately parallel bands. A small quantity of epidote find zoisite in crystals and grains, some of which may be primary-, is associated with small scales of sericite, the latter, at least, being one of the products of the incipient decomposition of the felspathic con- stituents. Occasional small flakes or scales of a much bleached biotite occur, some of which form a parallel intergrowth with the muscovite. The specimens examined have undergone extensive defor- mation, as a result of pressure subsequent to the cooling of the rock, and both felspar and quartz have suffered a somewhat marked granu- lation, while the surviving individuals of both the.se minerals exhibit wavy extinction rather perfectly. Some of the muscovite is doubtless of primary formation, although some has evidently resulted from the shearing of the felspar. C. Biotite-granite-gneissfis — (Gramfitft-gneisses). Var. («) Biotite- epidote-gneiss. — The combination of biotite and epidote as the prin- cipal coloured constituents, forms a well defined rock-type which has been found to be remarkably constant over large and widely separated areas, and is the one which is represented by the largest number of specimens. These rocks are undoubtedly of irruptive origin, and are, in fact, foliated granitites, thoroughly holocrystalline and granitoid, varying from coarsely to finely crystalline ; the constituent minerals being, a.s a rule, equally developed on all sides. Var. (6) Biotite-gneiss. These are foliated, holocrystalline, granitic rocks in which biotite alone, or accompanied by very trifling (juantities of secondary epidote, is the ferro-raagnesian constituent. Biotite- cyanite- giieiss. In the specimens of this type of rock which have been examined, the mineral does not occur, as a general rule, in aggregates of broad plates, but in isolated independent ones, which have an approximately pai'allel arrangement, determining the foliation of the mass. Var. (c) Biotite-cyanite-gneiss. This gneiss, though somewhat re- markable in its mineral composition, in that it contains cyanite, garnet. lighter a BARLOW. ] PETROORAPHY OF THE LAURENTIAN. I -J I and graphite in addition to the biotite which chiefly characterizes it, does not present any evidence whatever, either in its inicroscopicfil structure or its field relations, of any other than an irruptive origin. It is a perfectly fresh, holocrystalline, foliated granitic rock, and possesses in its structure no features which would at all suggest re- crystallization. It seems to be a peculiar local phase of the prevalent biotite-gneisses of the region, differing in no way from them as regards origin. A somewhat similar gneiss from near Wahnapitae station, in the Uescription of Sudbury district, has recently been petrographically described by Dr. ^J!''',?** ^^ ^^^ T. L. Walker,* who, however, says little regarding its microscopical character and field relations, beyond assigning it to the Laurentian, and stating that he regards it as a " true gneiss " and not a crushed granite. Var. (d) Hornblende-granititegneiss. — The rock thus classified Hornblende- differs but little in microscopical character from the ordinary mica- ^'r'u.ntite- ceous form of the granitites, although usually darker in colour and more basic in appearance. It sliows a transition ou the one hand into granitite containing biotite alone as the coloured constituent, which is the prevailing type of these gneissic rocks, and on the other, into hornblendegranitegneiss, which latter facies is of rather rare occur- rence throughout the district. In all previous descriptions the honi- blende-granite-gneiss has been reported as the variety most commonly present in the I^aurentian, the mistake having undoubtedly arisen from tht Vequent chloritization of the biotite originally present in the pre- valent granitite, the individuals showing the more advanced stages O ^ o ni ^ ? d H M M H t- H M C -" 4) CO «| ij = y O ^ ^ L-Ll W <1 S iS I -J -p o C" w a; -^ o t: j^ r. ^ K « o 2 I w, w ?<: ;y= _4'- ,.H= :; 'c: S -=.H-.- — ■ » = 3 - ^ o ■- i i ^ ^ t i.i ■— ' ri: t; i *• 5 ic B, 1. -r o c o 5 i ■s 1 2 i fc tp^"?c: ■^ £ = Sfes * . O 35 ai ■ i^ i- M a ^''' c-Si.ss, £'£•1 0) O JB « I • 1-4 1 G? 0) M 3 HO" ^ « ^ a go lis a I- 3 • 5| l = f Elf • SB 1 '! .i:; i ,-'■*• gneis obser grouj the b diotit graiii ated i action It consec fonne( gneiss( rocks ( The action granopl Inclusic scattere arrange host, f George Orfhoi in these other fel; viduals and fresh filled wit: and zoisit In thos subjected tendency present in triclinic f( oxides of i mon with of dynami granulated *0n the Journal of Gt m •] PETROGRAPHY OP THE LAURENTIAN. 79 I Quartz. — This is, in general, a very abundant mineral in the Quartz. gneisoBS of the district. Only in a few cases were granitic specimens observed in which the absence of quartz would lead to their being grouped v/ith the syenites. It enters largely into the composition of the basic rocks, allying them to the quartz-diorites and quartz-niica- diorites. In its general character it does not differ from the ordinary granitic variety, but is, of course, much crushed, stretched and granul- ated in those gneisses which have been subjected to intense dynamic action. It appears to fill in the spaces between the felspars of the rock, and consequently, to have crystallized out of the magt f. afrer they were formed. This is especially noticeable in many of the basic or dioritic gneisses. Distinct crystals of quartz have not been observed in the rocks examined, the mineral occurring in the form of irregular grains. The quartz grains, as usual, always exhibit the efiFects of dynamic action in a much more marked degree than do the felspars. A granophyric intergrowth with felspar is of very common occurrence. Inclusions are frequent. Sometimes the quartz occurs in grains scattered through hornblende, the individual grains having no regular arrangement or orientation with respect to one another or to their host. Such a structure has been named ' poikilitic " by the late Dr. George ET. Williams.* Orfhoclase. — This is the most abundant of the felspars which occur Ortlioclase. in these rocks. It usually forms irregular grains interlocked with the other felspars and quartz, although in a few instances porphyritic indi- viduals occur, which are sometimes twinned. It is seldom quite clear and fresh-looking, but usually >:' -'^ id in appearance, and more or less filled with little scales of serlcite avA granules and crystals of epidote and zoisite, the products of iti r^.ecomposition. In those specimens representing rocks which have evidently been subjected to intense dynamic action, the orthoclaso shows a marked tendency to pass into microcline. Inclusions of the other minerals present in the rock are of frequent occurrence, and intergrowths with triclinic felspars were also noted. It is often stained with hydrous oxides of iron, giving brownish or reddish tints to the rock. In com- mon with the other felspars, it has escaped to a large extent the results of dynamic action, rocks in which the quartz has been completely granulated frequently preserving large grains of the felspars which *0n the Use of the Terms Poikilitic and Micropoikilitic in Petrography; Journal of Geology, vol. I, No. 2, jip. 176-170. jss^acT Mici'ocline. i >i Origin (if niicrocline. 80 I NIPISSING AND TEMISCAMING R TO'- show only a few criicks and a more or less pronounced undulatory extinction. Microdine. — This is a very abundant constituent of the granitic gneisses, especially of those which have been greatly crushed and granulated. Teall has recently announced that the result of his inves- tigations of the niicrocline in the older Deeside (Cairnshee) granite of the Highlands of Scotland "lend no support to the view that micro- dine may be developed from orthoclase by dynamic or any other action, but are in accordance with the theory of Michel Levy and Mallard, that orthoclase is niicrocline in which the polysynthetic twinning is on a sub-microscopical scale." The constant relationship which exists between the quantity of microcline in a given rock and the degree of pressure to which the rock has been subjected, as brought out by microscopic examination, is of too marked a character to be ignored, and instances may frequently be observed, where, when a large individual of orthoclase has been peripherally granulated, the fragments detached from the parent individual show to perfection the typical cross-hatching of microcline, whilst the centre is quite free from striations and exhibits the ordi- nary characters of orthoclase. There is not, in such instances, a grad- ual transition from ot.e structure to the other, the cross-hatching in the detached bit of granulated material next to the parent individual terminating as abruptly against the fractures which separate them from it as do the strije induced by pressure in a plagioclase individual, against cracks traversing the crystal. Where evidences of pressure are unmistakably present, but fracturing has not actuall}'^ taken place, the gradation may be seen from the normal orthoclase, through a "moire structure" to the typical cross-hatching. Plate IV, Figs. 2 it 3. Thus, whether microcline and orthoclase be identical or dimorphous (a question which cannot be discussed here) the scarcity of the former in unaltered rocks, and its marked abundance in those which have been subjected to pressure, together with the peculiar manner in which it has been observed to occur in individual instances mentioned above, .seems to prove rather conclusively that microcline structure at least can be, and is, produced in the felspar now known as orthoclase and not show- ing that structure, as the result of pressure. It seems, too, reasonable to suppose that, if orthoclase be microcline with a sub-microscopic twinned structure, we should find various gradation.'^ in the same section from the microscopically invisible structure, through exceedingly fine striation, to the distinctly visible, and sometimes quite coarse structure, characterizing; what we call microcline. BARLOW. 1 Inst( is subj( ogous t( grain oi evidentl structur many of theory tl to the cc d re-arra Cases included regarded luonoclini Plagioc tolerably -Lake, com chemical ^•■f tin":, ion eicner an c As a gei with the bi diorite-gne a labradori pressure in Alteratic tization of t sericite. P In some ( the metamo clear and "l probably p tingui.sh bet Bintitc- uent of the into the coir in two formf smaller pJatt Crystals w ■^rechanical show the gen 1 BARLOW ] PETROGRAPHY OP THE LAURENTIAN. 81 I Instead of this we find that, when a crystal which we call orthoclase is subjected to pressure, a peculiar wavy structure appears in it, anal- ogous to the strain shadows of quartz as seen in the thin section ; the grain or crystal, when carefully examined under the microscope, being evidently under strain and undergoing deiormation. This wavy structure gradually mei'ges into the typical cross-hatched one. In fact, many of the arguments advanced, and facts cited in favour of the theory thatmicrocline and orthoclase are identical, seem to point strongly to the conclusion that this is not the case, but that niicrocline represents a re-arrangement of the orthoclase molecule induced by pressure. Cases where areas of felspar with typical microcline structure occur, included in unaltered and uncrushed orthoclase individuals, may be regarded as analogous to intcrgrowths of the ordinary triclinic and monoclinic felspars. Plagioctase. — In the granitic and syenitic gneisses, plagioclase is ,,, ■ . tolerably abundant, in the case of the mica-syenite-gneiss from Cross Lake, constituting nearly one-half of the felspar present. No direct ch"'nical determinations have been made, but when the angles of ^ :■ 6 > a generally a greenish yellow ft =dark yellowish-green, and r = deep bluish-green. Twinning is a common feature of the mineral. The hornblende is always intimately associated with the biotite and epidote when these latter minerals are present in the rock. In several instances the extinction angle was measured and found to vary from \1\° to 19°. Inclusions of felspar, quartz, zircon, apatite, titanite, etc., are very common and are frequently arranged in such a manner as to give to •AKLOW ] the horn Fig. 1. . zircon art ation to by the de No inst) nor any di the formei from the fi the exteric Ejudote.- the coloun largely intc addition to duct, we ha ber of cases The manr defined outli which have of no reasonj the accompai clearly. Th< pleochroic, ai tion colours, exhibit bluisl both in crystf stated, very s The corrosi Yukon River, crystal secticr Good cleavage them being a) Twins are o cores of a p]ec but no thorou| Nondescr- )t of epidote we; epidote, freque associated with *Cau. Rec, S Can., vol. III. (]v 6i '] PETROGRAPHY OF THE LAURENTIAN. 83 I the hornblende-gneias a typical micropoikilitic structure. Plate II., Fig. 1. As in the case of the biotite, the inclusions of apatite and zircon are often sunounded by well defined pleochroic halos. Alter- ation to chloritic and epidotic material was observed, accompanied by the deposition of carbonates. .No instances of augite cores occurring in the hornblende were noticed' nor any direct evidence of the latter mineral having originated from the former ; although in some few instances this might be suspected, from the fact, that the interior of the crystal is f a paler colour than the exterior portion. Epidote. — Next to the biotite, this is by far the most abundant of Epidoie. the coloured constituents of the granitic gneisses, and it also enters largely into the composition of the more basic hornblendic ones. In addition to the ordinary occurrence of the epidote as an alteration pro- duct, we have also the strongest evidence that it exists in a large num- ber of cases as an original and important constituent of the rock mass. The manner in which the perfectly fresh crystals, possessing sharply defined outlines, occur inclosed by wholly unaltered biotite in rocks which have been subjected to only a slight degree of pressure, admits of no reasonable doubt as to their primary nature. An inspection of the accompanying plate, (Plate II., Fig. 2) will bring this point out very clearly. The mineral is usually of a bright yellow colour, very strongly pleochroic, and possessing the usual high relief and brilliant polarizs! tion colours, except in sections parallel to the orthopinacoid, whicli exhibit bluish and yellowish tints between crossed nicols. It occurs both in crystals and irregular gi-ains, the former often having, as already stated, very sharply defined outlines. The corrosion phenomena noted by Dr. Adams, in epidote from the Corrosion Yukon River,* are shown to perfection in some of the individuals. The crystal sections are usually bounded by the prism planes M, r, and T. Good cleavages were observed parallel to M and T, the angle between them being about 115°. Twins are of common occurrence. The crystals occasionally contain cores of a pleochroic brownish sub.stance which is probably allanite, but no thoroughly typical examples of that mineral were detected. Nondescr' >t cores, which may represent augite, surrounded by rims of epidote were occasionally seen in the thin sections. Secondary epidote, frequently occurs in the groundmass of the more altered rocks, associated with chlorite, as the result of the mutual reaction of the *Cau. Rec. Sc. vol. IV., pp. 344-358, 1890-91, aim) Annual Report Geol. Surv. Can., vol. III. (N.S.), Part I, ApiJendix V (N.S.). p. 237 u., 1887-88. 6| phenomena ' -t:. I 84 I NU'ISSING AND TEMISCAMING REGION. MRLOW. felspars and bisilicates. It also forms small crystals and granules in the decomposing felspars, together with zoisite, sericite and carbonates, as one of the products of their saussuritization. ]\Iany cases occur in highly granulated rocks, where it is almost impossible to say what is primary, and what secondary epidote. Frequently, however, in rocks which have sutfered extreme crushing, and are filled with secondary epidote granules, large epidotes may be observed, broken and faulted like the other constituents, proving that they existed before the rock was subjected to the dynamic action. Muscovite. Muscovite, — Both primary and secondary muscovite occur in these gneisses, and it is often difficult in a particular instance to deteriiiine to which of these two classes the mica is to be referred. Frequently broad fresh laminie of muscovite are intimately intergrown with deep- brown fresh biotite, and in such cases is undoubtedly of primary origin. The variety of the mineral referred to here is muscovite proper, occurring in broad plates or laminje, as distinguished from the fine scales of sericite resulting from the alteration of plagioclase, etc. It possesses the usual bright polarization colours and other physical characters common to the species, and no unusual features were observed in the specimens examined. CMilciritc Chlorite. — (Taken as a general group name). — This is the common ^'''^"''' alteration product of the biotite and hornblende of these rocks. It polaiizes in the usual dull bluish tints. Many of the gneisses owe their green colour to this mineral, which gives them a very deceptive appearance, acid granitic rocks very often closelj' resembling, at first sight, some massive altered basic irruptive. I'vnte. Pyrite. — Is of common occurrence in all the gneisses, particularly in the more basic ones. The red and brown oxides of iron which so frequently stain the rocks can often be traced to this source. Calcite. Calcite. — This mineral is abundant where alteration of soda-lime felspars has proceeded to any extent. In such cases it forms large irregular, brilliantly polarizing patches throughout the thin section. Its abundance in some specimens, e. g., in the hornblende-granite- gneiss from the south end of Opimika Narrows, is rather remarkable, as this rock does not seem to have been greatly altered. In such instances it may possibly be of primary origin. Seiicitt. Sericite. — This is an abundant product of the saussuiitization of the felspars, forming tine, brilliantly polarizing scales, intimately associated with zoi as serici as it is c microsco] Apatitt basic gne and slend less rounc character] Titaniti served in i size, deep usual in su colours to The mir position ho grains of vj tioned. Li and also inc grained grf nearly all tl Zircon.-^ The crystals embedded ir pleochroic h Garnet. - gneissic rock certain locali gneiss contai basic-gneissic and aggregate pinkish coloi elsewhere bet" instances, all I crystals were Magnetite.- granitic gneiss few instances H(rmatite.~ witli hexagona along the clea\ •] PETROGHAPHT OF THE LAURENTIAN. 85 I with zoisite, epidote, calcite, etc. Some of the material referrtd to as sericite in the description of these rocks may possibly be talc, as it is difficult to distinguish between these two minerals under the microscope. Apatite. — This mineral is of frequent occurrence in the acidic and Apatite, basic gneisses. It is mostly in the form of stout and short or long and slender prisms, but grains with extremely irregular, and more or less rounded outlines also occur. The large stout prisms are especially characteristic of the diorite-gneisses. Titanite (Sphene). — Remarkable crystals of this mineral were ob- Sphene. served in some of the rocks examined. They are of unusually large size, deep clove-brown in colour, and intensely pleochroic, and, as is usual in such dark-coloured varieties, exhibit their brilliant interference colours to perfection. Twinning was frequently observed. The mineral is especially abundant in those rooks in whose com- position hornblende occupies a prominent place. It occurs in irregular grains of varying size, as well as in the well formed crystals just men- tioned. Little crystals were observed penetrating the epidote crystals and also included in hornblende and biotite. It frequently forms fine- grained granular aggregates of '"onsiderable size, and is present in nearly all the rocks described, both basic and acidic. Zircon. — This mineral is also of widespread occurrence in the gneisses. Zircon. The crystals are usually well developed, and often of large size. When embedded in the biotite or hornblende it is usually surrounded by a pleochroic halo. Garnet. — This is by no means as abundant a constituent of the Garnet, gneissic rocks of this region as was formerly supposed, although in certain localities it is extremely plentiful. It occurs in the granitite- gneiss containing cyanite, and also in several of the more or less altered basic-gneissic hornblende rocks. It is usually in fresh irregular grains and aggregates, frequently of large size, much fractured, and of a light pinkish colour in thin sections. The optical anomalies which have elsewhere been frequently noted, were not observed in the present instances, all the grains appearing to be completely isotropic. Distinct crystals were very rarely seen. Magnetite. — As staced elsewhere, the scarcity of iron ore in the Magnetite granitic gneisses is a remarkable feature in their composition. In a few instances isolated grains were tested and found to be magnetic. Hcvmatite. — This is frequently present in the form of thin plates Hseniatito. with hexagonal outlines, and in irregular scales. It is often developed along the cleavage planes of the biotite. Stlfl" i'i ■••'"-'•'^"•■"''"■(*'-'1'l' 86 I NIPI8SINO AND TBMISCAMINO RBOION. Ilinenite. Ilmenu Jreiierally s[ieaking, this is the iron ore which is present in the diorite-gneisses, and is almost invariably accompanied by its alter- ation product, leucoxene. It may be regarded as one of the essential ingredients of these rocks. The peculiar brownish tints so often seen in the plagioclase, are probably very often due to dust-like particles of this mineral included in them. Leucoxene. Leucoxene. — This is always an alteration product of titanic iron ores or rutile. The grains of ilmenite are sometimes completely replaced by whitish or yellowish, almost opaque masses of this mineral. A peculiar cross-hatched structure was sometimes observed, probably due to sagenitic growth of rutile which previously existed in the ilmenite individual from which the leucoxene was derived. Limonito. Liraonite. — The irregular deep-brown stains which frequently per. meate the various minerals, especially the felspars, are probably in most cases, due to the presence of this mineral. Zoisite. Zoisite. — Accompanies epidote as the result of saussuritization of the felspars, usually in quite small individuals which present no unusual features. Talc. Talc. — In a few of the more squeezed and altered gneisses, scales were observed which seem to correspond in their general characters with this species, as distinguished from sericite, but it is difficult to discriminate between these two minerals. Tourmaline. — Two or three columnar strongly pleochroic individuals of this mineral were observed in one of the gneisses examined. AUaniie. — Whilst not particularly abundant, many good examples of this mineral were observed, more especially in those granite-gneisses in which idiomorphic primary epidotes are plentiful. It occurs in the reddish-brown pleochroic individuals in the centres of epidote crystals with which it is in parallel orientation. These occurrences are of pre- cisely similar character to those described by Hobbs in the Maryland granites. Rutile. Eutile. — This mineral was observed in a few instances in the form of very minute, slender neeuLs penetrating the biotite. Cyanite. Cyanite, — Occurs in rather short flat-bladed crystals, which rarely show sharply defined faces in the prism zone, commonly forming irregular columnar individuals. A few of the smaller crystals show terminati jns, but with very rough faces. The colour is usually of light-bluish or greenish, but occasional crystals show a deep blue centre with a white margin. Some indi- Tonrmaline. Allanite. BARLOW vidua devel( and c( rock i are ol biotite Unc colourl These ] not not parallel longitU( As is ii] Orap, gneiss, i lines. , in diamt Fihrol lected i vicinity i and thesi which aci pitie statj Augite. absent frc In certair tion prodi but this examined no certain observed 1 darker col( The nai] 1863* by extensively Ottawa in t These were Geology 1 ORENVILLE SERIES. 87 I viduala measure half an inch across and an inch in length. It is best developed in those portions of the rock which are free from biotite, and consequently of a lighter colour. In the darker portions of the rock it is frequently intergrown with the biotite. The individuals are often bent and hold many inclusions, particularly of pyrite, biotite, quartz and graphite. Under the u)icroscope the sections are transparent, and generally colourless, but patches of a light-blue colour occur here and there. These patches exhibit a pleochroism (light-blue to colourless) which is not noticeable in the colourless portions of the crystals. The cleavage parallel to M and T do not traverse the entire section as a rule. In loni^itudinal sections the parting parallel to P is also clearly shown. As is invariably the case, the cyanite is accompanied by garnet. Graphite. — This mineral occurs in some quantity in the cyanite- Omphite. gneiss, in the form of irregular Hakes, rarely with rude hexagonal out- lines. A few flakes were observed to be nearly a quarter of an inch in diameter. Fibrolite. — Only a few specimens of the cyanite-gneiss were col. FibroHte. lected from the cuttings on the Canadian Pacific Railway in the vicinity of Les Erables Rapids and Snake Creek, on the Ottawa River> and these show no fibro^:'^,', but it is almost certain that this mineral, which accompanies the cyanite in the similar rock from near Wahna- pitse station, will be found associated with it in the area. Augite. — This miner.al, as elsewhere noted, is almost, if not entii'ely, Angite. absent from those gneisses which have been microscopically examined. In certain specimens a few skeleton forms, entirely filled with altera- tion products, were observed, which may originally have been pyroxene, but this is by no means proved. The hornblende was carefully examined to see if there were any traces of pyroxene cores in it, but no certain evidence of this was obtained, although in some cases it was observed that the exterior of tho hornblende individual was of a darker colour than the central portion. GRENVILLE SERIES. The name Grenville Series was the distinctive title applied in origin of 1863* by Sir William Logan to the series of crystalline rocks so "*'"®* extensively and well exposed in the region on the north side of the Ottawa in the vicinity of the Augmentation and village of Grenville. These were referred to as Middle Laurentian and supposed to con- •Geology of Canada, (18C3), p. 83!t. ISP KM I S- 1 H; SSS !■■ 88 I NIPISSINQ AND TEMI8CAMINO REGION. ceptions. formably overlie the Lower Laurentian or Fundamental (Jneiss. The rocks thus classified comprise a great variety of gneisses with which are associated considerable volumes of crystalline limestone, and a detailed map was published showing the distribution of the component bands.* Many reasons were adduced as evidence for regarding the whole series as greatly metamorphosed sedimentary Early miscoti- strata. These proofs had reference chiefly to the banded or foliated character of many of the composing masses, believed to represent the surviving traces of the parallelism due to original sedimentation, the pi'esence of large and important beds of limestone, together with the occurrence in some of these bands of forms described as represent- ing organisms of low type. Subsequent examination in the field, sup- plemented by the detailed petrographical studies rendered possible by the recent perfection of the microscopic methods of research, have, however, revealed the fact that, while certain of the fine-grained, light- grayish, rusty-weathering gneisses are closely allied instructure and com- position to ordinary shale or slate, other rocks, representing a very much greater volume of the whole series, are undoubtedly the foliated equivalents of the ordinary plutonic irruptives.f In the area covered by the accompanying map-sheets, the line of subdivision between what has usutally been regarded as Lower Lauren- tian and the Grenville Series, was described by Sir William Logan, in 1844, as occurring somewhere in the vicinity of the Mattawa River. The supposed line of boundary was based on the occurrence at certain points of isolated masses of crystalline limestone, but these have since been found to be in intimate association with rocks which are believed, with some confidence, to be the foliated equivalents of ordinary granites and diorites. In the area under description, only one very limited occurrence of the fine-grained and evenly banded light-grayish gneisses usually associ- ated with the Grenville series was noticed, consisting of a small band interfoliated with the ordinary reddish granite-gneisses, a little over two miles east of Rutlierglen station on the Canadian Pacific Railway. The strike of this band is about N. 20° W., with a dip to the north- east at a high angle. The hand specimen represents a fine-grained evenly foliated, rusty-weathering, grayish, graphitic gneiss. Under the microscope, it is a fine-gr-^'ned admixture of interlocking grains of fels- par, quartz, and a rather pale-coloured bleached biotite, together with smaller quantities of pyrite, graphite, rutile, and a mineral closely * Atlas, Geology of Canada, (18(53), Map No. 1. fAdams. A Further Contribution to our knowledge of the Laurentian, Am. Journ. Sci., July, 1895. Logan's line of su divisiou. Rocks of Grenville .Series. ■. ■ I •] OKENVILLE SERIES. 89 I resembling zoi.site in minute prismatic crystals, arranged in nests com- posed of aggregates of crystals and crystal fragments running parallel with the foliation. The rock has evidently been subjected to intense and long continued dynamic action, the foliation being pronounired, while the recrystallization has been so complete as to mask much of its original structure. It bears a marked microscopical as well as macro- scopical resemblance to the sillimanite gneisses described by Dr. Adams.* The most important band of crystalline limestone noticed in the whole Crystallinfi district, occurs at the foot of Lake Talon, an important expansion of j^^j^^ TiJon. the Mattawa River. The presence of this band was first noted l)y Bigsbyt in 1820, and later in 1844, by Logan. Dr. Bell, in 187G, also gave a short description of its mode of occurrence. \ The rock consists of whitish crystalline limestone with small thickly disseminated specks and patches of green serpentine. It is first noticed on the south side of the lake a short distance above the outlet, occupying the points along the shore, while the massive reddish granitite-gneiss rises into rounded hills behind. The limestone, as far as can be ascertained on account of the massive texture of the gneiss, occurs as an interfoliation, (lipping S. 8° E. < 25. Farther down, towards the chute, the rock contains a good deal of serpentine in addition to some other impurities, and occurs seemingly as a large irregular rounded patch in the gneiss. At the narrows, a short distance above the Talon Chute, the contact between the crystalline limestone and massive rather indistinctly foliated red granite-gneiss is well shown, the former dipping N. 74° E. <20° while the latter, with a nearly east-and-west strike overtops or flows over the mass of the crystalline limestone, the indistinct foliation of the gneiss conforming in general with the line of junction between the two rocks. See Fig, 1. Fig. 1. Skktch mkction siiowixt; stuuctuhk of crystai.li.vk limestone (a) .-^Nn massive RED (iUANrriTK (INEISS (b) NEAU TaLON ChL'TK, ^IaTTAWA RiVEU. *Aimual Report, (ieol. Surv. Can., vol. VIII. (N.S.) Part j. tShoe and Canoe, vol. I. London, 1850. JReiKirt of Progress, Geol. Surv. Can., 1870-77, p. 207. ,.^.. IMAGE EVALUATION TEST TARGET (MT-S) k /^J^ '"^S /. ^(2 1.0 I.I 11.25 lis I. ^ HUl. 14 I 2.5 2.2 2.0 ill^ 1.4 il.6 -► V] / ">>^ ^ % //^ r '/ Photogr^hic _,Sciences Corporation 23 «VI«'' MA»N STRUT WEBSTER, N.Y. i4S«0 (716) 873-4503 m \ iV \\ rv ^\ WrS 1^ V ed what •If'^tiiptiou of ,,,,,,,, . ,, , , contact near they have called a basal conglomerate reposing upon a ruivdamental Thessalon. complex of crystalline schists and granite, as exhibited on two small islands near the north shore of Lake Huron, a short distance east of Thessalon, Ontario. A difference of opinion, however, exists concerning the interpretation of this section, and the fact th.it the granite from which the pebbles in the conglomerate are believed to have been deri\ ed pierces and alters the slaty rock overlying the conglomerate, seems to show <;learly that the correlation of this granite witli that constituting the pebbles in the conglomerate is decidedly at fault, t In spite, however, of the generally irruptive character of the line of Intmsivo con- junction between the Laurentian and Huronian, it was confidently Hj^,r,,ni'ui' i'ml anticipated by even those who believed in the intrusive character of the liininntian T . ... , 1- 1 , 11 iiotiiccesftaiily Laurentian gneisses that, in some place an undisturbed contact would universal. be ultimately found. The detailed geological examination of the region to the north-east of F^ake Huron, carried on for the last ten years by the author of this report, has furnished abundant prof)fs of the pyro- clastic character of the rocks composing the two lower members of the Huronian. The breccia-conglomerate, greywacke and slates evidently represented the graded forms resulting from the consolidation of volcanic ejectainenta showered out and spread upon the bottom of a shallow ocean, and there somewhat rounded and otherwise modified as a result of acjueous action. In many ca.ses, however, these rocks are so Huronian intimately associated with materials resulting from proces.ses of ordinary "'■"'^' "l> aqueous erosion and deposition, that, in most instances it is extremely pyroclastic difficult if not impossible to make a separation. The fragments con- '^1"'.^!!,.''"^ "*" '^ tained in the breccia-conglomerate are, as has been shown, com- posed of rocks of igneous or plutonic origin and in no way dis- tinctly referable to any Laurentian strata now exposed at the earth's surface in the same area, while the fre([uent intimate association of this coarse fragmental rock with large masses of diabase, gabbro and *Am. Journ. Sci., III. vol. XLIII, pp. 224-232, March, 1892; also III. vol. XXXIV, 1887, pp. 207-216. tAin. Journ. Sci., III. vol. XLIV., 181t2, pp. 230-23y; also Bull. (ieol. Soc. Am. vol. IV., pp. 330-332. i Kili i'in'itj smu nntrt( h \ I if ■ ^ 1 • ■ ! A true haseniunt or fundamental granite on Lake Temin- earning^. 94 I NIPIS8INO AND TEMISCAMINO REGION. granitite, cannot be regarded as merely accidental. The earlier part of the Huronian period in this district was evidently a time of intense and long continued volcanic activity, and the greater portion of the rocks representing this lapse of time are pyroclastic in character. True sedimentation on a large scale seems only to have been ushered in toward the close of the period, and the quartzite-grits and con- glomerates prevailing towards the summit of the series are very typical examples of epiclastic material. The relations found to exist between this arkose and an underlying fundamental biotite-granite or granitite, as exposed on either side of Lake Temiscaming in the vicinity of Bale des Peres, indicate its deri- vation to be a result of the disintegration and degradation in situ of the underlying granite, showing a gradual and uninterrupted passage outward and upward from the parent mass. The nature and import of this passage were the subject of an illustrated paper, prepared by the author and Mr. W. F. Ferrier and presented at the Toronto meeting of the British Association for the Advancement of Science in August 1897.* A short resume of the interesting phenomena observed has already appeared in the Geological Magazine,f but the details, not only of the field relations of these rock masses, but also of the petrographical examinations will be found in that portion of this report dealing with the geological description of Lake Temiscaming. The relations be- tween this granite and arkose are of rather unusual scientific interest, showing as they do the pre- Huronian existence of a basement or floor upon which these sediments were laid down and which in this portion at least has escaped the movements to which the Laurentian gneisses have been subjected. The petrographical studies undertaken with the object of determining the origin, composition and minute structures of the various rock masses making up the bulk of the Huronian, have been so numerous and detailed that it is impossible in the present report to give at length the description of each separate slide, especially as many of these pre- pared from specimens obtained at widely separated localities, were after- wards ascertained to represent rock^ presenting no essential points of difference. It will therefore doubtless be found sufficient to give a general description of each of the three members constituting the Huronian, at the same time pointing out the nature of the transitional sequence so frequently witnessed from one rock to the other. V( * On the Rt'lationH and Structures of certain Granites and Associated Arkoses on Like Temiscaming, Canada, Kep. B. A. A. S., Toronto, 1897, pp. ()6()-G(iO. + Geol. Mag., New Series, Decade IV., vol. V., No. 1, pp. 39-41, January 1890. MNLOW. The roc or "chlori described Lake Tern indicates n nature am is applied is usually ( ing in prop ducts whic weathers fr surfaces no a light oli layer, usual pale-yellow usual sausst quantity of massive, sh tion, while t rogeneous m, degree of cer however, it h this is in m( planes, which usually at vei the line of ou lar curving li pressure, simi resulting frott in many descr been repeated! the frequent a Although til rock occasiona is no necessar rock varies wid exceedingly ha chlorite and oth are so soft that and in its more T MRLOW. HUROMAN. 95 I Breccia-conglomerate. The rock tlius designated is identical with the " slate conglomerate " or "chloritic slate conglomerate" of the earlier reports of the Survey, described h\' Logan as following the Laurentian orthoclase-gneiss on Lake Temiscaming. The new name, as proposed, is preferred as it indicates at once what is now confidently believed to bo the true nature and origin of the large and important rock masses to which it is applied. This rock, especially where the finer matrix is abundant, is usually of a dark-greenish or greenish-gray colour, the colour deepen- ing in proportion to the (juantity of the greenish decomposition pro- ducts which may have been developed. The immediate outer coatitig weathers from yellow through brown to almost black, although certain surfaces not exposed to the continued action of the atmosphere retain a light olive-green appearance. Beneath this dark outer surface, is a layer, usually about one-eighth of an inch in thickness, composed of pale-yellowish decomposed material which evidently represents the usual saussuritic products resulting from the alteration of the large (juantity of felspar present in the rock. As a rule, the rock is extremely massive, showing little or no evidence of lamination or stratifica- tion, while the coarser fragmental material is arranged in such a hete- rogeneous manner that it is exceedingly difficult to ascertain with any degree of certaintj' either the angle or direction of dip. Sometimes, however, it has a slaty or foliated structure as a result of pressure, and this is in most cases the only structural feoture discernible. These planes, which evidence intense and long continued pressure, are inclined usually at very high angles, the strike corresponding in direction with the line of outcrop of neighbouring intrusive masses, while the irregu- lar curving lines of foliation produced by the unequal resistance to pressure, simulate in a most marked manner the uneven lamination resulting from original bedding. It is, therefore, not surprising that in many descriptions of exposures of similar rocks, such a structure has been repeatedly mistaken for stratification, the descriptions asserting the frequent and usual highly tilted character of these rocks. Although the slaty cleavage, especially in the upper portion of this rock occasionally corresponds with the original stratification, there is no necessary connection between the two. The hardness of this rock varies widely, the least altered or more quartzose varieties being exceedingly hard, while those exposures in which a large amount of chlorite and other greenish decomposition products have been developed are so soft that they can be readily scratched. Both as a massive rock and in its more imperfect forms of slaty structure, it exhibits the char- Breccia-con- glniin-rate or nlatf coii- ffloinenitf of Lugaii. Colour and structure of broccia-pon- glnincratt?. Fra(n»PHta niaking up bri'ccia-con- gloinerate. rr- 96 I NIHlSSINd AND TKMI8CAMING REGION. Not littoral in ori);in. I'yi'iL'liistic IllltlllC ..f 1 1 r 1 1 l)rfcci:l-ei)li- glciiieiiite. i'i Comin)fiti()U of matrix of hri'cciii-coii- gliiiiicrate. acter of a conglomerate, carrying fragments of various irruptive mate- rial which vary in size from the smallest pebble to some boulders a foot or even more in diameter. In some localities, the rock is so full of these fragments that very little of the finer interstitial matrix is appa- rent, while in other places only an occasional one is found. Usually the fragments are more or less perfectly rounded ; often they are sub- angular, while in some outcrops these larger individuals present sharp and often i-e-entering angles. The breccia-c (?) quartzite and fire ;;rained slaty j,'rey\\ composite fr 7i •J IIUKONIAN. 99 I still more coarsely ciystallint* luul holncrystnllint' in struetuift niuy repnv sent iiltercd galihros or diorites, but tins ferro-inagnosiaa niiiH'rals are all decomposed to chlorite. These ])el)bles luo identical witli those descriljod as composed of a "greenish t'elspathic rock '" in earlier rt'iKirts. In every case examined they were foiuui to lie niii -h decomposed. A thin section of a fine-grained peblile, also from the (iull Rock Island in Lake Temiscaming, shows the rock to have undergone great alteration, the felspar being saussuriti/ed and the original augite decomposed to a pale-greenish chlorite. In spite, however, of this advanced alteration, t!ie typical ophitic structure (jf diab.ise remains. Occasionally some of the felspar has a broad iabular habit causing the rock to approach the gabbros in structure. The irregular an.'as between the plagioelase laths are filled with a felled mass of pale green chlorite scales. Leucnxene, re>,uUing from the almost complete alteration of the ilmenite originally present in the roek, is plentifully scattered through the section. Other sections examined, ijelonging to much coarser grained fragments, were of essentially similar composition, revealing the .same advanced alteration. The laths of j)Iagif)clase, deoompo.sed to a partially opaijue gray saussuritic mass, penetrated a matted aggregate of pale-green clil')rit.e scales representing the allotriomorphic areas of augite originally present. The ilmentite has wholly disappeared, to be replaced by opaque graj'ish masses of leucoxene, showing the characteristic skeleton forms produced by the rhombohedral parting. Pyrite and occasionally pyrrhotite and chalcopyrite are constituents of these diabasic frag- ments and pebbles. In addition to these peV)bles and fragments of granitite and diabase, others representing a greatly crushed and stretched felspathic (juartzite were noticed, containing also sericite and chlorite. Occasional frag- ments of a rock in which plagioelase and orthocla.se are porphyritically develojjed in a tine-grained granular quartz-felspar groundraass were also observed. Besides the.se composite pebbles, there are very often fragments, usually sharply angular in outline, of both felspar and quartz, which when present alone give the rock a decidedly porphyrite appear- ance. Some of these pseudo-phenocrysts embedded in a dark-green chlorite groundmass were examined, the rock thus constituted repre- senting the " country-i'ock " of Wright's mine on the east side of Lake Temiscaming. Some of these individuals proved to be felspar, chiefly plagioelase, which have a broad tabular habit, well striated and very turbid owing to somewhat advanced decomposition, while others are composite fragments of some porphyritic granitic rock with the large Otiipr flagliii'llts pli'sellt iu bri "ccia. * mmmm P 1 ' 100 I NIPISSINfi AND TEMISCAMINO HKQIOV. ili-triliiitiim nf l)rcccia TrnriKitiim u|>\vnrtl to ^'^ey\Vilckt■• crystals of wol! strinted plas^ioclase surrounded l)y finely fir.inulatcd (|uartz. Tliickins.Hiinil As will bo spcn by a roft'reni'o to tlin acconiiiaii\ in;,' map slieets, this brecx-ia-conf^lonionito is of very widespread occurienco in this district. On Lake Teniiscaminf,' it rises into hills nearly five hundred feet in height, in thick, almost structureless masses, altliou^'h in large and well exposed sections, lines which evidently represent original bedtling may be distinguished. The total volume seen cannot be much less than six bundled feet, which perhaps represents the givate.«t thickness attained by this rock, although the conditions under which it must have been deposited were necessarily so unstable that at no place can the basement, upon which it originally rested, be detected. The present nature of its contact with rocks which may possibly represent re-fused portions of this original basement, shows evidence f)f a considerable sinking down of the mass of clastic material into the molten or plastic magma beneath, so that it is manifestly impossible to state the true total thickness of what has Ijoen regarded as the basal member of the Huronian. This breccia-conglomerate passes upward into a dark-greenish com- pact rock closely related in composition with the finer grained portum or matrix of the much coarser fragmental rock beneath. The transition upwards consists mostly in a gradual loss of the larger composite fragments. ComiKmitiiiii Although in certain places an occasional pebble of reddish biotite. of gnywacki.' granite may bo noticed, sections of t'lis fine-grained and compact grey- wacke or felspathic sandstone show an even-grained mixture of angular and subangular fragments, composed chiefiy of (juartz and orthoclase^ together with, usually, a small proportion of plagioclase. (Plate II, Fig. ;3). Miciocline though sometimes present is of rarer occurrence. These pebbles are embedded in a much finer groundmass relatively in- significant in quantity, originally felspathic, but which is now composed of a confused aggregate of minute scales of yellowish-gre. sericite arising from its decomposition. A large amount of chlorite is present usually disseminated in irregular shreds and fragments, althougli some- times also forming part of the finer interstitial material, while the abun- dance of this mineral gives the prevailing greenish tint to the rock. Epidote and zoisite are also commonly abundant, and occasionally calcite, all these representing secondary products of alteration. Pyrite, magnetite and ilmenite are also very common constituents, the last mentioned mineral usually showing somewhat advanced alteration to leucoxene. Zircon, sphene, apatite and brownish dichroic touimaline, likewise occur, but are not by any means abundantly represented. (JKOI.OdKAr. SlUVKY OK (.'AXADA, Vol,. X.. I'AllT I., I'r.ATK II. Vu:. 1. Vu Fi(i. 3. Fui. 4. Vu,. 1. Micropuikilitic stnictmi' in lioiiil)!i.n(lc of dioiitc West Ann, Liikt- Nipis'^iiiK'. X <>."). Vu:. 2. — I'riniury cpidiitf in l)i(itit(' of i|ii!irt/.-niica-tii()riti'-t,'n»Ms.s— Cordon Cirfk. tiim mill's troin Ldus; Sanlt, Lake 'rcniisciuiing. X ''••">. Kk;. 3.— Charni'tfr and position of in IikIimI fra^jnicnts in typical ^jrcywacki'— Little Kivir, Lakr Tt'iiiiscaining. X . Fiti. 4.— Kim of c'liliiritc, siirnmndinj,' an^jite of diabast — Fanny Lake. X •">-■ ■i.1 BARLOW In time ( bands as it I] colour duced ties is east CO Bay ail altliouf Tii(' col to the ( atlditioi striped foruiinsr ful mosf are esse finer sta dence of in places some of siurgest c in some i The St usually, t The comp coinpacte( the produ< leucoxene rock in t arranged i or areas. The mici tion of th The lighter less proport incipient se represented show a prep what exten; the prevailir MRLOW ] nURONIAN. 101 I In ascending, this rock gradually becomes finer grained, at the same Slatp or slaty time developing a marked slaty structure parallel to certain colour ^ ^' bands which represent original bedding. This slate, or slaty grey wacke as it may be called, (foi- in places large masses though exhibiting the colour striping are altogether devoid of any structure except that pro- duced by jointing), varies greatly in thickness, and in occasional locali- ties is not represented at all. The high hills found on the north- east corner of High Rock Island, as well as on the west side of Cross Bii}' and Sandy Inlet, lihow sections over a hundred feet in thickness, although in most cases the rock does not occur in such large volume, Tho colours occur in alternating bands showing a gradation from one to the other; usually of different shades of green with sometimes the addition of reddish-brown and black, thus producing a very beautiful striped rock. In some instances certain beds have been broken up, Autoclastic forming an autoclastic icjk, which, when recemented, exhibits a beauti- ful mosaic of irregular though angular fragments. The constituents are essentially the same as described above, diflfcring only in their finer state ol: division. The fragments as a rule show little or no evi- dence of water-action, l)eing irregular and sharply angular in outline) in })laces forming an intorlocking mosaic of quartz and felspar grains, some of which have evidently originated in situ, while other portions suggest considerable recrystallization which has certainly taken place in some instances. The structure in occasional instances is that of a microgranite, but Microscopic usually, the clastic origin is at once brought out by the microscope. ^[.^",^ ""^" The component fragments are remarkably uniform in size and closely compacted together, with little or no finer interstitial material, while the products of decomposition such as chlorite, epidote. sericite and leucoxene are partially scattered, somewhat promiscuously, through the rock in the form of irregular grains and scales, while many are arranged in a more or less definite manner in irregularly curving lines or areas. The microscope reveals at once the nature and difference in composi- C'onqiotiition tion of the colour-bands that so frequently characterize the rock. " '* '^^ The lighter green bands show a prevalence of quartz together with a less proportion of felspar, the latter being either fresh or showing only incipient sericitzation, while chlorite and iron ore are only sparingly represented, if at all. The darker green bands, on the other hand ]';.\iilanatiou show a preponderance of felspar, much of whiv.h has undergone some- Viamis.'"^ what extensive saussuritization, which, together with chlorite, gives the prevailing darker green shade to this portion of the rock. The il^j liil il' I ! t I 102 I NIPIS8IN0 AND TEMISCAMING REGION. ;. i 1 1 1 f^iiartzite grit or arkorio, li dark, almost black, Hues or stripings are seen to be composed of an infi- nite number of small crystals and opatjue particles of magnetite, together with a much larger proportion of ihnenite, which, despite its extensive alteration to leucoxeue retains much of its original dark colour and opacity. The reddish-brown stripes are highly fclspathic in composition and owe their colour to abundant disseminated hydrated peroxide of iron. These slates evidently in most cases represent the consolidation of what must once have been extensive beds of volcanic mud or ashes. In certain instances, as on the eastern shores of Lady Evelyn Lake and on Turner Lake, they merge into coaiser grained irregular banded or foliated tufaceous rocks, which occur in immediate juxtaposition with large plutonic masses, while in other cases, as on the east shore of Lake Temiscaming, to the north of Wright's mine, they are interbedded with coarse volcanic breccias or agglomerates made up of diabasic and quartz-felspathic fragments embedded in a paste composed largely of chlorite. In ascending, this rock gradually becomes much coarser in grain, finally passing into a quartzo-felspathic sandstone, although in certain places the latter rock was occasionally met with resting directly upon and merging downward into a basement composed of red granitite. This arkose is usually rather coarse in texture, in most places showing the characters of a grit, while certain bands or portions are conglome- Dcscription of ratio. iLany of the larger fragments in the conglomeratic phase of this rock represent very distinctly rounded or waterworn pebbles, the largest of which vary from an inch to two inches in diameter. These are composed, for the most part, of grayish-white, translucent, often much fractured quartz, and many of them are surrounded by a thin film of oxide of iron. Occasionally some pebbles of red quartz are present, and still more rarely others repiesenting a " stretched " felspathic quartzite. I3esidt'S these there are greenish, grayish and pale-brown- ish, usually angular, or at most subangular fragments of an extremely fine-grained rock, seemingly identical in compo ition to many of the chalcedonic-like fragments embedded in the vitrophyre tuff described bj' the late Prof. G. II. Williams from Onaping, Ont.* Besides these there are small, often angular fi-agments of red and yellow jasper together with smaller pieces of both reddish and grayish felspar. These are embedded in a matrix composed largely of yellowish-green sericite, which, on account of its relative abundance gives the prevailing tint to the whole rock. Tiie rock, as has been stated, represents almost altogether the consolidation of true dotrital material derived from the *Anmuil Kt'iH'rt, <^}pol. Surv. Can., vol. V. (N.^.), Part I, IHIK) !)1, (). 74k. Sections Nob. 35 and 42. frupnonts. Composition of arkose. ■] IIUUONIAN. i03 I Scvt'ral varieties of arkose. breaking down of granite, a portion of which is represented by expo- sures covering an area of nearly six square miles in the vicinity of the Old Fort Narrows on Lake Teiniscaniing, although some of the eiubed- deil fragments are rather typical of volcanic ejectamenta ; thus evidenc- ing the continuance of the explosive activity, though with much dimin- ished violence, which characterized the earlier portion of the Huronian period. The nature and detailed description of the passage of the biotite-granite into this overlying arkose, is fully discussed in the geo- logical description of the exposures encountered on the shores of the northern part of Lake Temiscaming. The least altered form of this rock is a rather coarse arkose, which upon a superticial examination bears a remarkably close resemblance to an ordinary irruptive-granite. The constituent grains, mostly an- gular in outline, consist of quartz, orthoclase, plagioclase and microcline, somewhat closely compacted together, with a very little intervening finer felspathic material which is undergoing decomposition to kaolin and sericite. The reddisl) colour is imparted to the rock as a result of tlie abundance of ferric hydroxide which fills not only the minute Jis- sures but also stains the larger felspathic individuals. Other varieties which show no great degree of alteration or attrition and assortment through aqueous agencies, are distinguished macroscopicaliy by being brownish, pale-pinkish or grayish in colour. A rather typical specimen of the prevailing greenish variety or "sea green quartzite" as it has been called, obtained from a point on the east side of Lake Temiscaming (Boat-field Point) about half a mile east of the Hudson's Bay Co.'sold post, shows the rock under the microscope to have originally been composed of felspar and quartz. The quartz is Comiwsition in clear colourless fragments, sometimes with tolerably even outlines, of iirkose on but usually presenting very irregular ones, and the larger fragments Temiscaminfr are often made up of several interlocking grains. The felspar which was originally present, is now almost altogether converted into pale yellowish-giei n sericite which gives to the rock its prevailing colour. The sericite scales are usually exceedingly minute but occasionally their presence can be detected macroscopicaliy. There can be little doubt that much at least of the felspar has been altered in situ. This alteration of the felspar to sericite is shown in a beautiful manner in the section. It has l<, however, could not be positively ascer- tained, as the covering of clastic rocks, if originally present, has been removed by subsequent denudation. These rocks, in the area here considered, uuially possess a medium texture, although in many instances they are so coarsely crystalline that most of the principal constituents are plainly apparent. In general they vary from greenish -gray, through dark-green to almost black in colour, although in many of the coarser phases the prevalence of felspar with a distinct flesh-red colour, gives a prevailing reddish tint to the whole mass. In most places they have a massive much jointed character, and this, together with the extensive shearing action to which these rocks have been subjected, makes it exceedingly dithcult to secure even a hand specimen of well shaped outline. In occasional Basaltic localities, as at Manitou Rock on the west side of Lake Temiscaming, «tnict\ire. the rock shows a rude columnar or basaltic structure. Under the microscope, these rocks present a remarkably uniform inineralogical composition in the several separated masses, while the specimens obtained almost invariably exhibit, in a very typical manner, the ophitic structure which belongs essentially to diabnse, although in some other areas, as well as in certain portions of the same mass, it sometimes shows the holocrystalllne or granitoid structure of gabbro. The least altered variety of the rocks of this class, is made up Com position essentially, and almost wholly of phigioclase and augite, the former '^'^ ''.'"''"*''''*"" mineral being present in the usual idiomorphic lath-shaped individuals penetrating the allotriomorphic augite. From the extinction-angles, the plagioclase is near the basic end of the series — labradorite and bytownite. The mineral is sometimes rather fresh and glassy, although frequently it shows a marked turbidity, owing to the development in it of the usual saussuritic products of decomposition, while the augite, which when fresh is of a distinct reddish-brown colour, is as a rule partially decomposed to green trichroic hornblende. A few rather broad tabular unstriated individuals of felspar are usually present, and may possibly represent orthoclase. lleddish-brown, lilt!: V>\ \ ;. I i > 106 I NIPISSINO AND TEMISCAMINO REGION. ill ■1 Diabase of (^uinii Point. (i.ibbro of Houth-west arm of Lake Tcmagaini. strongly pleochroic biotite is found in irregular plate.«, but not in any excessive amount. Quartz is likewise a rather cdnstant constituent, occurring in small clear irregular areas filling in the lesser interspaces between the felspar and augite. The ilmonite present very often shows the characteristic "gridiron" alteration to leucoxene. In cer- tain instances, as at Quinn Point on the east side of Lake Temisca- ming, the rock has unflergone considerable decomposition, the augite being completely altered to green trichroic hornblende (uralite.) Most of this uralite is the usual compact dark-green variety, but some of it has assumed the actinolitic habit. In other localities, as oa the Quinze liiver, the diabase has undergone still more advanced alte- ration, the whole rock-mass being converted into a rather typical hornblende-schist or amphibolite as a result of intense pressure. Tra- ces of an ophitic structure still remain, showing clearly the original character of the rock, altliough in places this is masked by the extreme deformation to which the rock has been subjected. The process of the uralitization and decomposition of the augite is very interesting and instructive, showing first an alteration to the compact green ti'ichroic variety of hornblende, the indiviu'^als presenting deep-coloured bor- ders with pale interiors. This, with an increase in deformation, assu- mes the fibrous or actinolitic habit, which, in turn, is decomposed to chlorite, the individuals of the last-mentioned mineral retaining much of the marked pleochroism of the hornblende. Some of the plagioclase seems remarkably fresh, although the greater proportion is altei'cd to opaque greyish masses of saussurite, the resulting epidote, zoisite and sericite being especially al)undant in those portions of the rock which have yielded most to pressure. The ilmenite originally present, is often almost wholly converted to a brownish sphene wliich occurs in grains or aggregates scattered through the rock. A section prepared from a specimen representative of a small mass of highly altered gabbro that protrudes through the breceia-con- glomerates and slaty greywacke on the east shore of the south-west arm of Fjake Temagami, shows that the rock is now composed of fel- spar, quartz, pa'e-green fibrous chlorite, biotite and zoisite. The mutual reactior. of the felspathic and feiro-magnesian constituents has been so pronounced, and the resulting decomposition products have in many cases wandered so far from their former positions, that the ori- ginal structure is to a certain extent masked. Zoisite is a very abund- ant constituent of the rock as an alteration product, occurring in irre- gular grains and crystals. Sphene is also quite abundant and has resulted from the decomposition of ilmenite originally present. Small P •AHUM) cores of brownis The 1 Beaver designat ture is v planes o greenish scope, tli( The plagi of the s( of the im position presence c site result augite is a the laths r variety fie are characi (schilleriza ent alterati able quanti scales. A opaque iron grains tliroi irregular ai pentinuous dotted with dote, the wl ii-regular ma in serpen tin( small residue refraction th Besides th( ciated with ti trusives incot clearly do not have been pre ration than tl tive statemeni conjunction h '1 nUHONIAK. 107 I cores of the unaltered ilmenito .still renmin. The biotite is of a pale- brownish colour as a result of the leaching out of a portion of its iron. The rock composing the upper and more precipitous portion of Diabase of Beaver .Mountain, or the "King of the Beaverh" as it is sometimes \i,'„„,taiii. designated, is a dark greenish-gray diabase, in wliich the ophitic struc- ture is visible to the naked eye. It is much sheared and broken, the planes of cleavage and jointing being plentifully coated with dark- greenish minerals belonging to the chlorite group. Under the micro- scope, the rock is seen to be composed mainly of plagioclase and augite. The plagioclase, which from the extinction-angles is near the basic end of the series (probably bytownite), is usually pretty fresh, but some of the individuals are rather turbid, owing to the presence of decon'- position products, while considerable areas are characterized by the presence of light-greenish sericite and yellowish-green epidote and zoi- site resulting from tiie saussuritization of the felspar substance. The augite is as a rule fresh and occurs in allotroraorphic masses pierccl Ly the laths of plagioclase. It is reddish-brown in transijiiuced light, a variety fiecjuently met with in diabases, and many of the individuals are characterized by the presence of innumerable rod-like interpositions (schillerization products.) Frequently it is noticed untlergoing incipi- ent alteration to compact pale-green trichroic hornblende. A consider- able quantity of reddish-brown biotite is present in irregular plates and scales. A little qucartz was also noticed, while both pyrite and an opaque iron ore, probably ilmenite, are present, scattered in irregular grains throughout the section. Besides these, comparatively large and irregular areas may be seen composed of a pale yellowish-green ser- pentinuous substance, associated with secondary caleite and often dotted with strongly refracting grains and elongated fragments of epi- dote, the whole showing aggregate polarization. Very oiten these irregular masses show the characteristic net-like structure so common in serpentine derived from the decomposition of olivine, altliough the small residual cores still remaining, in some cases have a lower double refraction than is usual in this mineral. Besides the masses above referred to, which ire so intimately asso- ciated with the elastics of the Huronian, there are also similar basic in- nuAc intru- trusives incorporated with the Laurentian gneisses and granites, which re,)^';^^'," " clearly do not belong to the same magma from which these latter rocks have been produced, In most cases these appear to be of earlier gene- ration than those associated svith the Huronian, although no very posi- tive statement can be made on tliis point. The gneiss in immediate conjunction is often more basic and hornblendic, seemingly showing •• I, ^ 1 Ml 11 ■ J 3 I' : ; ii ^ !» [ i;] Diabase of Expectatioii Lake. Adjacent rock. 108 I NIPI.SSIXO AXn TEMISCAMING REGION. a commingling l)y actual fusion of the two rocks along their line of junction. Outcrops of a uralitic diabase marking the occurrence of a small urea of this rock, were noticed apparently cutting and altering thegra- iiitite-gneiss exposed on t!ie north-west shore of E.'cpectation Lake near the south-west end. The diabase is much finer grained near the junction with the gneiss. The specimen obtained showed the rock to be a medium-gniined, dark-green, basic eruptive, the diabasic structure of which can be seen in the hand specimens. The microscope shows it to be a remarkably good instance of a diabase in which the bisilica- tes have been almost entirely decomposed, while the plagioclase remains in a comparatively fresh, unaltered condition. The minerals now pre- sent are plagioclase, hornblende and chlorite (doubtless representing augite originally present) ilmenite accompanied by leucoxene, apatite and sericite. A few of the plates of chlorite look as if they may have been derived from biotite. The plagioclase is in rather broad lath- shaped .sections whicii interlace, giving a coarse ophitic structure to the rock. It is well striated (both alhite and periclino laws being represented) possesses \ery uneven extinction and has evidently been suiijected to a coii'-i lerable degree of pressure, many of the crystals being shattered. The augite originally present is now almost entirely altered to a pale yellowish-green chlorite. It has evidently passed through an intermediate st i;e of alteration to hornblende, as that mineral, of a pale bluish-green colour and librou-f, in which the altera- tion to chlorite is so far advanced as to almost entirely obliterate the optical characters of the hornblende, surrounds lighter, still more alterel cores which douljtless represent the original augite. Magnetite result' ig from the decomposition of the bisilicates, a little apatite, sericite and epidote occur as secondary products. This diabase is in contact with a dark green, fin?-grained, compact, foliated rock, sprinkled with little crystals of pyrite. Under the micro- scope, the ground mass consists of a fine-grained mosaic of clear quartz and felspar, through which run little strings of a brown biotite, in fine brightly polarizing scales which are evidently of a secondary origin, and in places show an alteration to chlorite. Throughout this fine-grained material, larger grains of quartz and felspar (principally microeli^) are distributed, which by their granulated appearance and very uneven extinction bear unmistakable evidence of the dynamic action to which the rock has been subjected. Large irregular grains of pleochroic epidote, colourless to pale yellow, frequently showing good cleavage, are abundant, as are also large clove-brown crystals of sphene. Crys- « ■ARLOW. 1 HURONIAN. 109 I tals of zircon, fairly large, and frequently showing marked zonal structure are plentiful. Some pyrite and iron ore were also observed. Another niiiss of these b.asic eruptivcs that may he mentioned in Basiu this connection, is woll expose'! on tlie shores of McDiariuid Lake, the .Mciiiarmid southern part of Breadalbane Lake and the isUiniis and points chiefly I"»l<'- in the central portion of Fanny Lake. The rock is dark-creen, almost black in colour, weathering rusty '•"><>»• or brownish owing to the oxichitinn ot the large amount ot jiynte finely disseminated through it. Atmospheric agencies have likewise produced a rough, though somewhat finely pitted surface, owing to the decomposition and removal chiefly of the coloured constituents, leaving a reticulated surface formed by the felspar standing out in relief. The relations with the surrounding gneissic rocks of the Lau- rentian series seem to show its earlier genesis, and these foliated and much more acid rocks are rendered relatively more basic or hornbleudic in the immediate vicinity of the line of junction, apparently as a result of the free interchange, through actual fusion, of the material of both rocks. The basic rock has usually a rather well miuked foliation, which corresponds in general with the strike of the inclosing ,<;neissic rocks. On McDiarmid Lake this strike is 8. L't° E., tlie rock being nearly if not quite vertical, while on Fanny Lake the strike is X. 35° E. with a dip to the north-west of 85°. Under the microscope, this rock is seen to be a rather fre>h diabase Micki^oI'ic . . structures. ; composed chiefl}' of plagioclase and augite. The plagioclase is unusually fresh and glassy, and well striated, both aibite and i)ericline laws being represented. It occurs for the most part in ratlier broad, lath-shaped crystals penetrating the irregular individuals of aus'ite. As a result of pressure, it usually exhibits a wavy extinction, is sometimes bent or curved and occasionally fractured and dislocated. The augite is of the reddish colour so often noticed in diabase and occurs in irregular polysomatic areas. These composite individuals or masses are sur- rounded by a narrow rim, of remarkably uniform width, composed of fibrous and I'adiating scales of pale-greenish chlorite, each separate scale being approximately at right angles to the outline of the unal- tered portion. (See plate IL, fig. 1.) The augite is rather frei?h, while the line of division between these "reaction-rims" and the unaltered portion of the individual is very sharp and abrupt. Associated with the augite and freciuently com- pletely inclosed by it are irregular plates and scales of a reddish-brown strongly pleochroic biotite. Sometimes it is considerably bleached while occasionally it is altered to chlorite. 'Annual Report, Geol. Surv. Can., vol. I. (N. S.), 188788, p. 155 v. \U ! !!il': I 110 I NIPISSINQ AND TEMIHCAMINC RK(ilON. . ' t Ba8ic- rooks On tho west side of Lnko TemiscuiiiiiiL; nearly fjpposite Lalours "ni '^'^ """ ^li"*^) l>l!it'k, irregular, rou<,'lily weathering masses of a very liasic rock may Ijc noticed cauglit up in and penetrated by the assoiiat«!d graiii- tite-gneisses mapped as Laurentiun. The liand-spccimen examined is black in colour with glistening scales of mica abundantly developed through tin; mass. The weathered surface is rough and pitted, resembling a pumice-stone. I'nder the microscope, the component minerals are seen to be hornblende, l)iotite plagioclase, garnet and iron ore. The hornblende is green in colour, trichroic, and occurs in large areas composed of an aggregate of suwill individuals. Occasiunally these aggregates show a pale inteiior with a dark-green bordtir surrounding the nuisses, !t is undoubtedly sec- ondary in origin and .some of it isactinolitic, and is the most abundant mineral in the section. The biotite is rather pale in colour owing to the removal of a part of the iron, and freipiently shows pleochroic halos surrounding embedded fragments of the other constituents of the rock. The plagioclase is not nearly so abundant, and is very f recpienlly almost opiujue, from the inclusion of dark-brownish dust like particles. The gainet is in irregular grains as is also the iron ore, which is prob- ably magnetite. A some.vhat rude ophitic structure can still be detected in the rock. Occurrence of Besides the foliated diorites that occur as integral and extremely dioritcs. basic portion of the prevailing Laurention gneisses, there aie occasional and comparatively large irregular areas of massive diorite, which are apparently of earlier genesis than the foliated rocks with which they are associated. One of the largest of these masses noticed, occurs on the southern mountains to the south-west of the west point of Maski- On Bear Bay. nonge Island, on Bijar Bay in Lake Nipissing. The mass has, roughly speaking, a diameter of a little over four hundred feet. A border of black mica-schist (probably a mica-diorite-gneiss) nearly three feet in width, separates this massive basic rock from the gneiss, the foliation of the diorite gneiss curving lound the outline of the mass. The whole mass is penetrated by reddish quartzo-felspathic masses and dykes which are evidently extremely acidic portions of the same magma from which the gneisses have solidified. Fragments of the basic hornblen- dic rock are embedded in gneisses near the line of junction. Microscopic character. Under the microscope, this rock is seen to be a garnetiferous granite, being composed of plagioclase, orthoclase, quartz, hornblende, an ortho- rhombic pyroxene and garnet with smaller quantities of sphene and iron ore. It possesses a holocrystalline structure and shows only slight evidences of pressure in the uneven extinction of the quartz and felspar ■ARLOW individii; is usua!l\ pleocliroi Excellcti a. H. \\- occupiecl crowded ence to oi complete structure, interpene The ort parallel c roism, wit' ant and ov usually in luby-rcd ii irregular g iron ore is The rock most part, i classificatioi are to be fo lakes formii across these give a very these separa: coarsely eryj distinguish;) 1 very massivi foliated text tSpawning an this rock pres crysts being felspathic gi Orthoclase is inicrocline an^ while quartz, * Journal of G, (iHANlTK. Ill I ■ ^ '\ individiiuls. The felspars as a rule are quite fresli. Tlie horriblondf is usually in massive irre_'ulai- indivitluals (if a {jrccii colour and stioiiKly plcocliioic. t)ccasional individuals siiow f,'o()d ci ystaliui^'raphic outline Kxcelh'rit examples of tlio niicropoikilitic siiut'ture described by Dr. G. II. Williauis * were observed. Thus certain nrcus of the rock are occupied by cumparativcly lar},'o individuals of hornblende which aro crowded with irregular /^nains of (piart/ arran^^ed without any refei- ence to one another or to tin* matrix, and, which neithei- possess tin* complete independence of optical orientation characteristic of granular structure, nor the entire continuity of the separated portions of two interpenetratingciystal individuals. The oi'tliorliombi'-" pyroxene, which is probaV.ly hyjiersthene, has a parallel extinction, is rathei" liidit in colour and has a feeblt^ pleoch- roism, with light-yellowish to pale reddish tints. It is somewhat abund- ant and occurs in individuals having ii regular outlines. The garnet is usually in large individuals full of irregular ciacks. It is pale ruby-red in colour with characteristic high relief. The sphene is in irregular grains frecjueiitly imbedded in the hornblende. An opaque iron ore is rather abundant in the section examined. t OR.XNITE. The I'ock to which this general name has been applied, is, for the fj i most part, a biotite-granite or granitite according to Kosenbuch's ^',' classificati(m. As the details of the numerous exposures of this rock are to be found in connection with the geological de.scription of the lakes forming the series of canoe-routes which atlbrd an access to or across these mas.^es, it will only be necessary, in this connection, to give a very geneial notice of this rock, applicable alike to most of these separate occurrences. It is of a prevailing reddish colour, rather coarsely crystalline, the principal constituents being usually readily distinguish.ible with the unaided eye. In some localities it presents a very massive structure, while occasionally it shows a very distinct foliated texture. In several cases, notably in the area adjoining Spawning and Young Loon bays of Lake Temagami, occurrences of this rock present a very coarse, often porphyritic, variety, the pheno- crysts being Carlsbad twins of orthoclase developed in a quartzo. felspathic ground-mass rather poor in ferro-magnesian material, Orthoclase is the most abundant felspathic constituent, although microcline and plagioclase are both present in considerable quantity, while quartz, which is as a rule proportionately less in amount than •Journal of Geology, Chicago, vol. I., No. 2. i.i'. tir (if ^riMiiites. ■; L 112 I NIPlHSINfJ AND TKMISCAMINd RKfilON. ■aRloa i 1 It 1^ I I H 1 ic .structure. lU I NIPIS81NG AND TEMISCAMING REGION. present are l)iotite and gfirnet, with abundant iron ore, some acces.sory augite, a little hornblende (?) and nm8.se3 of calcite, etc., which may represent in part felspars originally present, though none are now observ- able. Apatite is abundant in good-sized long prismatic crystals. The section of the tiner-grained portion contained no garnet, while in the coarse-grained phase of the rock this mineral is exceedingly abundant. The garnet is of a peculiar yellowish-brown colour and re.senibles the melanite variety, while the coarse portion of the rock might be described as composed es.sentially of biotite and melanite garnet with some little accessory augite and perhaps hornblende. The rock is a most remark- able one and further investigation of fresher material might prove it to be a hitherto unobserved member of the mica-peridotite family. Another interesting and rather rare species of ^^ke-rock was noticed on the most southerly of the Manitou Islands in Lake Nipissing. Near the southern extremity of this small island, dykes as well as irregular masses of an alnoite-rock cut the dark reddish and greenish granitite-gneiss representing the Lauren tian. One of these dykes is about ten feet in width, running in a direction nearly east-and-west and inter.secting the foliation of the gneiss almost at right angles. Another occurrence showed a fissure about six inches in width filled with the same material. Muiray**^ mentions the occurrence of intrusive masses of the same rock as .seen on one of the islands in East Bay opposite Callendar station. The specimens of this rock consist of a fine- grained greenish groundmass in which are embedded large phenociysts of biotite and augite, together with rounded greenish masses, which at first sight seem to resemble concretionary or pebble-like inclusions. On examination, these simulate rude prismatic crystals, but only the skeleton forms remain, filled with decorapo.sition products, chiefly calcite, and that may possibly repiesent olivine, originally present. In the hand-specimens the large plates of biotite and phenocrysts of a.gite are especially noticeable, at once suggesting its probable close affinity to the alnoite first described by Tornebohmf, in 1882, from the island of Alno, in Norway. The thin section, under the micro- scope, shows an exceedingly fine-grained and decomposed groundmass consisting of an intricate mixture of brightly polarizing scales of bleached biotite, chlorite, spicules and crystals of hornblende (actinolite), calcite, pyrite, iron ore and leucoxene, in which are em- bedded larger individuals of augite and biotite, the former almost wholly converted to hornblende and calcite, although the chai-acter- • Report of Progress, Geol. Surv. Can., lG.53-56p. 122. t A. E. Toniebohm : Melilit liiwalt friii Alno, (Jeol. Forn. 1 Stoekliolni Fiirli. 1882 p. 240. ■A mow ] P ST-ARCHiEAN ERUPTIVES. 115 I istic skeleton forms remain. In this matrix are developed large though somewhat rude phenocrysts of biotite and augite. The large, individuals of augite show a perceptible, though somewhat indistinct pleochroism and are traversed with a network of cracks mort or less filled with hornblende and calcite, products of its alteration and decomposition. They are as a rule surrounded by a rim of variable width composed of the usjual hornblende (uraiite), showing beautiful deep-bluish polarization colour between crossed nicols. The biotite is rather fresh, althougU some of the iron has been removed, and, as a consequence, exhibit brilliant chromatic polarization colour. The pleochroism, is strong from deep brownish-red to pale-yellow. The individuals have a hepidiomorphic outline, occurring in elongated plates and scales which show considerable optical disturbance as .. result of pressure. The rock doubtless belongs to the group Type of the which includes the alnoites, monchiquites and fourchites but it is now so decomposed that its exact position cannot be determiiied. Closely related rocks have been described by C. H. Smyth, jr.,* from Central New York, and by Adams, t from Ste. Anne de Bellevue, Quebec, and from a point on the road between Ashcroft and Savona, British Columbia, three miles east of Eight-mile Creek. About five chains north of the last occurrence of this rock, on the j)yko west side of the same small island, beds of pink crystalline limestone c.""'»S '_ . . limestone. occur containing more or less epidote, biotite and hornblende as impurities. The strike of the rock is abouo N. 80° E., while the dip is at an angle of 65°. A dyke varying in width from 9i to 1 1 inches, of fine-grained, dark-greenish, almost black rock was noticed intersecting this limestone in a direction N. 4° W. Under the microscope the rock is seen to be greatly altered, con- ]\[iL,,.„j.coi)ic sisting chiefly of microcline and horni)]ende, the latter evidently second- Lluiracter. ary in origin. The original I'ock, unaltered, was probably an augite- tuicrocline one and thus allied to the vogesites. The hornblende occurs in elongated pale yellowish-green individuals considerably altered to chlorite and frequently forming shc-af-Iike bundles of crystais. A close study of the section reveals numerous examples of comparatively unaltered cores of the original augite. The felspar of the rock giving generally elongated sections appears to be principally microcline, although some plagioclase wa- also observed. It is turbid, being full of inclusions of hornblende, sericite, etc Brilliantly polarizing secondary epidote is abundantly distributed throughout the rock. •American Journal of Science, April, 1892, August, 1893, and October, 1896. + Ibid., April 1892; also Annual Report, Geol. Surv. Can., vol. VII. (N.S.), p. 38811. No. 79a. fit I i-\- i.wgw il6 NIPISSING AND TEMISCAMING KEGIOX. Hi li! m Dyke on Goo8<> Islands. Dykes near Buntiekl. Siniiku- (iykcs ni'iir Sudliury. Kocks near Cjillander. On one of the smaller of the Goose Islands, at the extreme west end of the group, the pinkish granite-gneiss strikes N. 70° E., with a dip to the south < 50°. Near the nortli-west end a greenish dyke of fine-grained material about \\ feet in width, cuts across the whole end of the island running in a direction N. 58° E. About three miles and a half north-east of Bontield station (formerly Callander) a rock-cutting made during the construction of the Canadian Pacific Railway shows a good section of a massive granitoid gneiss pierced Fig. 2. North-east. South-west. Dykes ok Coxcrktionahy Diahask 3i Milks N. E. ok Bonfikld. by several dykes of a rusty-weathering medium textured diabase. The rock has a marked concretionary structure, which is revealed as a result of ordinary weathering, the successive thin concentric layers of rock peeling oflf much like the coats of an onion. The dykes cut across the indistinct foliation of the associated gneissic rocks. Near the walls the dykes are very much decomposed and schistose, while the gneiss is baked and altered to a slight degree in the immediate vicinity. The largest of the dykes, near the south-west end of the cut, is six feet across with a branching arm about two feet in width. Another dyke near the north- east end of the outcrop is four feet in width, while the third is only about one foot in width. The rock composing these intrusions is readily attacked by atmospheric agencies and is more or less hollowed out in the adjacent hard gneiss. Dykes and masses of precisely similar material are exposed along the line of railway between Sudbury and the Murray mine, which in a thin section under the microscope is found to be a rather typical and fresh oli vine-diabase. No petro- graphical examination was however made of the rock from the locality above described, as the specimens secured were lost in transit. Along the line of the northern division of the Grand Trunk Railway, in the vicinity of Callander station to the east of Lake Nipissing, the various rock-cuttings show good exposures of a mas.sive granitite-gneiss. As a rule, this is a medium-grained distinctly foliated granitic rock, in which the dark-coloured irregular strings and layers composed of the ferromagnesian constituents, (principally biotite), alternate with BANLAW. ] POST-ARCH-EAN EUUPTIVES. 11 t I Dyke.-i cutting tlu'Ul. broader reddish bands of coarse-grained felspar and quartz in which lie little patches and strings of the darker material. Frequently the gneiss has a very distinct augen structure, the lenticles composed almost wholly of reddish felspar being sometimes as tnuch as six inches in length Vjy two or three in breadth. The strike of the rock varies from N. 20° W. to N. 20" E. with a prevailing dip to the east at a high angle, usually over 60'. In some instances the rock is quite mas- sive, showing little or no evidence of foliation. These reddish grani- toid rocks are intersected in several places, almost at right angles to the foliation, by irregular often branching dykes of comparatively line- grained dark greenish-gray, sometimes almost black rocks. In the immediate vicinity of the line of contact, the gneiss exhibits a narrow selvage of much liner grained rock, showing the intrusive action of th»> dyke, while in some instances fragments of the gneiss have been caught up and incorporated in the body of the dyke. At the first cutting, about a quarter of a mile south of Callander, the rock is very massive and granitoid, but at the second, a well marked foliation has been devel- oped, running N. 10' W. with an easterly dip at a high angle. This rock is intersected by two dykes, daik-green to almost black in colour, containing porphyritically embedded individuals of a black, bright, glist- ening mineral. The walls of the dykes are more or less irregular, often Hclations of serrated and frequently presenting re-entering angles of fine-grained \^^ suucfure^ material which penetrates the mass of the neighbouring granitic I'ock. At the widest places the larger of the two dykes is about seven feet thick, while the smaller is about two feet. The dyke interrupts the folia tionof the gneiss and near the contact both rocks are much finer in tex- ture, while fragments of the gneiss are embedded in the dark-greenish rock. Under the microscope, the rock possesses a peculiar irregular granular structure, and the intergrowth of hornblende and felspar gives to the section a pseudogranophyric appearance. The section is filled with a dense mass of little shreds of hornblende in a groundmass composed ohiedy of broad plates of orthoelase. There are numerous large phe- nocrysts having centres composed of a pale-green diopsedelike pyrox eue, altered t)n the outside to a green hornblende. Biotite is also plentiful in large fresh irregular plates full of inclusions. Titanite and apatite also occur. The whole section is sprinkled with iron ore, pyrite and granules of epidote. It is a very basic rock, near the syenite end of the peridotites and between these and the vogesites. It might be termed a hornblende augite-minette. The next cutting, situated about A mile south of Callander, runs branching through a hill of a deep-reddish granititegneiss. At the north end of *'>^''^'''- the cutting the foliation is quite distinct, this structural feature strik- m i llh <.\ ;br liTW i i :;3: 118 I NIPIS8ING AND TEMISCAMING REGION. ing about N. 10^ E. with an easterly dip . "iitceous limestone. The whole section exposed is of small ! ' an i thickness, the beds lying in nearly, if not quite, horizontal suc.i. The shore is strewn with large angular blocks of the *Report of ProgrosB, Geol. Surv. Can., 1853-56, p. 125. •] CAMBKO-SILURIAN. 121 I coarse-grained, yellowish-gray, arenaceous limestone, containing many weathered and waterworu fragments of obscure oephalopod-like remains. These fragments, according to Dr. H. M. Ami, who has examined them, resemble the Eudoceras multitubtdatum (Hall) from the Trenton and Black River. McDonalds Island, or the Little Manitou, is about half a mile in ,, ., .^ ' ' On ^icDon- length from north to south and of no great breadth. At the south- alrls Ishuid. west corner is a small patch of yellowish -gray limestone, occurring in beds which have little or no inclination. The only fossil remains visible at this locality were fragments representing chiefly the siphuncles of orthoceratites together with crinoid stems and casts of suppof^ed worm-burrows. Small outlying patches were also noticed beneath the surface of the water. About the middle of the island, on the west shore, the thickest expos- ure of the whole of these outliers is exposed. The total thickness is about thirty feet, the beds showing a gentle inclination to the west. At the base is a greenish or yellowish arenaceous limestone holding decomposed fragments and pebbles of the gneissic rocks beneath. This is overlain by a yellowish, arenaceous limestone, comparatively free from coarse fragmental material, which in turn gradually passes up- ward into gray limestones and shales holding numerous fossil remains. The orthoceratites are characteristic and numerous, and one specimen obtained must have belonged to an individual over six feet in length. The following lists of fossils have been prepared by Dr. H. M. Ami from collections made by myself and my assistant, Mr. A. M. Camp- bell :— Palceophylliim or Columriaria, imperfectly preserved. Amplexopora, sp. Coscinopora (1) sp. Monotrypella qiiadrata, Rominger. Pachydiclya acuta, Hall. Plectamhonites (?) sp. Zygospira recitrvirostra, Hall. Orthis tricenaria, Conrad. Rajinesqidna Cf. R. alternata, (Emmons). Trochonema umhilicatum, Hall. Small exposures of the basal conglomerate and overlying arenaceous i,\,^j,ils from limestone occur on the west side of the Great Manitou Island, these <'i«'at rocks dipping south < 5", while on the south shore, near the old wharf, island, is a small outcrop of arenaceous limestone dipping east at a low angle. t ■:■ ■ i' ! i If "'-'""■""•" 122 NIPISSING AND TEMISCAMING REGION. I'.'' Iff i!i sl !l J i i; Trenton outliers. Fossils. From these expo.sures the following fossils were obtained : — StronMtocerium rugosum, Hall. Columnaria Ilalli, Nicholson. Fragments of crinoidal columns not determinable. Ptilodictyafalciforinis, Nicholson, Kafinesquina Cf. R. alternately (Emmons). Zygospira recurvirostra, Hall. Zyyospira (?) sp. undet. Lophospira bicincta, Hall. " sp. type of L. helicteres, Salter. Maclurea (?) sp. undet. Actinoceras sp. Cf. Actinoceras Bigshyi, Stokes. Endoceras, sp. Orthoceras, sp. Probably a new species of the type of Orthoccras rapax, Billings. This may be referable to the genus Cameroceras. Trenton. Between Deux Rivii'res and Mattawa, are several small comparatively flat-lying exposures of sandstones and limestones resting upon the Laurentian gneiss close to the edge of the river, that are com- pletely covered during times of freshet. The sections exposed are of no very great thickness or extent, the beds dipping in a southerly direc- tion at a low angle. The most important of these outliers is the one situated on the north side of the river about four miles above Deux Rivieres. The basal or sandstone beds formerly furnished material for the manufacture of grindstones of an excellent ({uality while local limekilns utilized certain portions of the higher beds exposed in this escarpment. About six miles below Mattawa, two small outliers of a light- yellowish and purplish, gray-weathering arenaceous limestone are seen in the north bank of the Ottawa River, containing abundant fossils characteristic of Lower Trenton period. Besides the rock in situ, the beach in the vicinity of these outliers contain a large number of somewhat water-worn blocks of these fossiliferous strata. Thr following list of fossils has been prepared by L»i. Ami from a collection made at this locality. Receptacnlites occidentalis, Salter. Crinoidal fragments too imperfectly preserved for identification, but may belong to Glyptocrinns. Prasopora Selwyni, Nicholson, (J'rasopora lycoperdon, Vanuxem.) Streptelasma corniculum, Hall. Frondose monticuliporoid (section required for identification.) ■ARLO)*. Bra Obs cornpat Stro Hafi Orth Orfh ^ygo Your Tjagi The : the nor tional ir by Logai separatee to exist, of marini strata of connecte( previousl trough c( outlier, a bordering Although exposed o exposed fi of this out analogy w It has lithologica Winnipeg Hudson B both prese earning out in which tl Bay were arated fron *RfIK)rt of ] pp. 334-33(!. t Geology of ■ARLOW ] siluria:?. 123 I Branching form of monticuliporoid. Obscure monticuliporoid form, probably related to Solenopora (Cf. S. conij)acta, Billings.) Strophomena incurvata, Shepard. Jtajiesqnina alternata, (Emmons). Orthis, sp. Cf. 0. tricenaria, Salter. Orthis (Dinorthis) proavita, W. and Sch. Zygospira recurvirostra, Hall. Young of Murchisonia (possibly Lophospira hicarinata, Hall.) r.'agment of trilobite too imperfectly preserved for identification. Silurian. Clinton and Niagara. The rocks of this a"e, exposed on the shores and islands of Clmracter and . . t e athuities of the northern portion of Lake Temiscaraing, have been of excep- tlu- Silurian tional interest to geologists ever since their discovery and description '"" "^'^ *' by Logan in 1845*. (Jeographically, this outlying patch is so widely separated from any locality where rocks of similar age are now known to exist, that it has been a question whether it is indicative of an area of marine submergence connected with that in which the fossiliferous strata of Hudson Bay were deposited, or whether it was in some way connected with the Niagara basin to the south-west. It has been previously asserted that these rocks belong rather to the great northern trough connected with Hudson Bay, of which they are probably an outlier, and the absence of all strata of Niagara age in the region bordering the lower Ottawa has served to strengthen this belief. Although in lithological character and colour the rocks of similar age exposed on Temiscaming exhibit a marked similarity to the Niagara exposed further to the north, the rich and varied fauna characteristic of this outlier presents no corresponding resemblance, but rather a close analogy with the Niagara formation of south-western Ontario. It has been shown that a pronounced similarity exists both in Fauna tuilike lithological character and fossil remains between the Niagara of the ,^.n'J'^siluri-in Winnipeg basin and that exposed in the vicinity of the Churchill on Hudson Bay, although these areas are now widely separated, while both present organic forms that are entirely lacking in the Temis- caming outlier. These facts, therefore, seem to prove that the seas in which the Niagara sediments of the Winnipeg basin and of Hudson Bay were deposited were practically continuous, while both were sep- arated from the Teraiscjiming basin and the region to the south west. *RejK)rt of ProgreBs, Geol. Surv. Can. 1845-40, pp. ti9-70. pp. 334-33(i. t Geology of Canada (18(13), p. 334. Geology of Canatla (1803), ' 124 I NIPIS8INQ AND TEMI8CAMINO REGION. ill I 'J II .strata in HyiiLliniil iuriii. Possible area of Cainbro- Siliu'iaii. Conditions of deiwsition. The stiiita forming the Temiscaming outlier occur in the form of a shallow synclinal trough, occupying somewhat more thnn the breadth of the lake, which is here about six miles, and extending from the northern end of Moose or Bryson Island, north-westward beyond the confines of the present map. On both sides of the lake the rocks incline towards th« water at varying angles, de- pending on the character of the shore-line ; although in general the dip does not exceed 10', and angles of lesser amount are far more common. On Mann or Burnt Island, as well as on the peninsula to the north, the limestones show a very gentle westerly inclination of between one aiid two degrees, while on Percy Island,* near the west shore, the rocks are very nearly if not quite horizontal. It is thus evident that any section made must of necessity be more or less ideal and any thickness based on the observed angles of the dip is sure to be misleading. The whole thickness exposed in any one section is somewhat less than 150 feet, and it seems certain that the total amount of the Niagara exposed on this lake cannot be groa''^?r than 300 feet, and may be considerably less. The occurrence of loose angular fragments and slabs of grayish dolomite, resembling that exposed in the vicinity of Lake Huron and Nipissing and containing characteristic Trenton fossils, has been noticed.! These are distributed at several points on the shores of the lake and specimens were collected from the north-east shore of Chiefs Island. Although their source has not yet been ascertained, the angular character of the fragments and their abundance shows clearly that this cannot' be far distant. The lake is here over 200 feet in depth and it is just possible that below the Niagara limestone and concealed beneath the waters of the lake there exists an area of Carabro-Silurian rocks. This, however, can oniy be ascertained by boring, as no exposures of these rocks were encountered, although a diligent search was made with this object in view. The relatively smaller quantity of conglomerates and sandstones, characteristic shallow water deposits, and the rapid alternation from these coarser elastics to the fine-grained limestones indicative of deep water deposition, point to a rather sudden marine invasion ; while the comparatively great volume of strata remaining shows a prolonged submergence. The fine-grained character of most of the limestones show that their deposition took place in a quiet arm or extension of the sea, not affected by the open ocean, while the abundance and char- * So called in honour of Captain Walter Percy of the steamer Meteor plying on this lake, t (.Jeology of Canada (18()3), p. 335. BARLOW. acter c of its As of the coherei gioiner, have a consist] adinixt the und yards in relation; pact an( occurs in arenaceo at an an At Ha edge and yellow fii north-eas of the coi Niagara e perhaps tl underlying be benoatl Further and is sep narrow chi senting a weathering from yellov Shells of V number of Ami, as foil Clathrodi Favosites Syringopi Crinoidal Leptcena r Atrypa rei Meristella Anoplothet ] SILURIAN. 125 I acter of the fossil reinaias are ample testimony of the genial character of its waters. As exposed on the west side of Wabis Bay, in tlie north-west corner ('"ubIkuiii-- of the lake, the lower portion of this formation is composed of a loosely «toneH. coherent sandstone or grit alternating with thinner beds of a fine con- glomerate, with pebbles chiedy of Huronian quartzite, most of which have a thin coating of yellowish or brownish iron oxide, while the matrix consisting of similar material in a finer state of division, contains a slight admixtuie of calcareous matter. The actual contact between this and the underlying slate of the Huronian is not seen, although only a few yards intervene between the exposures of the two rocks. The existing relations can, however, be made out pretty clearly, for while the com- pact and rather massive slaty rock which here represents the Huronian occurs in exposures with more or less rounded or hummocky outlines, the arenaceous strata of the Niagara dip off or away from these hillocks at an angle of 5°. At Haileybury, on the western shore of the lake, close to the water's Limijstone edge and cropping out from the shingle is a small exposure of light- i',',,,".. yellow tine-grained limestone, without visible fossil remains, dipping north-east 25^ The discovery of limestone with the general contour of the country in its vicinity, seem to suggest that a small patch of Niagara extends northerly along this shore towards Wabis Bay, being perhaps three miles in length by about a (juarter of a mile in breadth, underlying the clay which here eflfectually conceals any rocks which may be beneath. Further south, on Percy Island, which is only a few chains in length Foshils from and is separated from the western mainland by a very shallow and narrow channel, the rock exposed is a light-yellowish limestone, pre- senting a very uneven or cavernous surface as a result of unequal weathering. The strata are nearly if not quite horizontal and weather from yellow to brown or almost black, as a result of the iron present. Shells of various species of brachiopods are somewhat numerous. A number of the fossil remains collected, have been determined by Dr. Ami, as follows : — Clathrodictyon fastigiatum, Nicholson. Favosites Gothlandica, Lamarck. Syringopora verticillata, Goldfuss. Crinoidal fragments. LepUena rhomboidalis, Wilckens. Atrypa reticularis, Linnseus. Meristella, sp. Anoplotheca hemiapherica, Sowerby. in ffl: • ! ll . Jl I ; ; 1 126 I NIPI88INO AND TKMISCA.M1NO REGION. MRLOW. J Cdinjldiiiilatf on ( /'liit'fs I Inland. i la ' m Pterinea, sp. Also branches of obscure Monticuliporidu'. Thia fauna represents the Clinton or base of the Niaj»ttra or lower part of the Silurian. The northern and western points of Chiefs Island, rise into compara- tively high ridge.s of massive (juartzose sandstone or (juartzite-grit which present the usual rounded and glaciated outlines. Sheltered in the bay intervening between these two points is a small patch of boul- der conglomerate, composed of sub-angular masses derived from the underlying quartzite. These aie imbedded in a calcareoarenacoous matrix composed chicHy of pebbles and finer material, the whole repre- senting evidently a boulder-strewn beach covered by later sediments of the Niagara formation. The surface of the quartzite on which this con- glomerate rests, presents the humniocky character so common in the case of the hard Archa-an .strata, the irregular cracks and depressions being filled by the conglomerate. Subsequent glaciation has removed much of the material, .so that the exposure now presents a plane surface with a more or less net-like structure, the framework being represented by the finer arenaceous cement while the meshes or interstices are occupied by truncated sections of quartzite boulders as well as of the rounded hillocks of the solid rock beneath. Some of the boulders present in this conglomerate were evidently large concretions, as they exhibit concentric structure and weather very rusty owing to the disintegra- tion of the large proportion of iron present. The finer cementing material, whil(> relatively much smaller in amount than the peebles and boulders, is always of a greenish or yellowish colour and frequently contains corals and orthoceratites. The action of the weather has par- tially obliterated the glacial strife on this finer matrix, but the sections of the quartzite boulders and hummocks exhibit these markings in great perfection. .^ ., , On the south-western shore of Chiefs Island, is another small patch r ossils from ' _ '^ Cliiifs Island, of a finer grained conglomerate, the pebbles of quartzit^^ being less numerous and of much smaller size, while the matrix conrai is much more calcareous matter. The rock dips south-east < o\ A number of rather badly preserved fossils were secured at this locality, which have been named as follows by Dr. Ami : — Halysites catenularia, Linnieus. Columnaria, sp., with very irregularly disposed horizontal tabula\ ZaphrentiSf sp. Streptelasma or Caninia, sp. Rhynchonella, sp. Murchisonia, two species. Euomp Discoso The ab( of the Ni On the within le.s! occupied I of the Nil! already de gular fragi of the expi cement of corals and This bot in turn re rather frial closely foil with a gen< action of t unevenly le distance no deposits. In the Wright's si light-yellow erly directi small patch On the there are tw at the shore dipping in these small On Burnt between thi well as on t the northerr that represe is of a pale- in thickness Mmowc 1 SILURIAN. 127 I Outliers on cM-^t -idc of lakt'. ]'>asal con- ^'liiiiienkte. Eiiomphalus, very large species. Dlscosoru8. Cf. D, conoideus, Hall. The above fauna represents the Clinton formation or lower portion of the Niagara. On the east side of the lake, from the point south of Chiefs Island to within less than a (juarter of a mile from Piolie Point, the shore is occupied hy a narrow fringe of the basal conglomerates and sandstones of the Niagara. The coarser beds are of the Ijoulder conglomerates aheady described, representing simply a talus of angular and sub-an- gular fragments detached from the elevations in the immediate vicinity of the exposures, consolidated together by a finer grained arenaceous cement of a yellowish colour in which are also embedded fragments of corals and orthoceratites. This boulder conglomerate passes upward into a tine conglomerate in turn replaced by a coarse grit, and becoming finally a yellowish rather friable sandstone. These beds run in long ui^dulating curves, closely following the general outline of the underlying quartzite with a general westerly dip at angles varying from 10' to 15\ The action of the waves has in places caused this to disintegrate very unevenly leaving a rough pitted surface. At Piche Point and for some distance north, the Huronian quartzite is left entirely denuded of these deposits. In the bay to the south of Piche Point and between this and Aienact'ouN Wright's silver mine, there are two small patches of thinly bedded ""^'' ""'' light-yellow arenaceous limestone dipping in a southerly or south-west- erly direction < 5°, immediately south of Wright's mine is another small patch of similar arenaceous limestone dipping south-west < 9°. On the east shore of the lake, nearly opposite Bryson Island, there are two more small patches of the arenaceous limestone exposed at the shore, wrapping round the hummocks of Huronian quartzite and dipping in a southerly or south-westerly direction <5°. None of these small patches of limestone contained any visible fossil remains. On Burnt or Mann Island, as also on the two smaller islands >iaiii Imu'- between this and Bryson Island (Oster and Brisseau islands), as ^^'^^^' '^^^'^' well as on the high promontory separating Wabis and Sutton bays in the northern part of the lake, are exposed the limestones and shales that represent the deep-water deposits of this period. The limestone is of a pale-yellow or cream colour, weathering whitish, and varies in thickness from a few inches up to two feet or over. Some of the r , .^ Biiildinp wtunt'. ■I Fossils from Mann Island, illf 128 I VIPISSINO AND TEMISCAMIXG REGION. beds are very fine-grained and of rather even texture, and it is possible that some parts may prove to be sufficiently uniform for use as lithographic stone. Asa building stone it is of excellent quality. These lime, tones, on the north shore of the lake at Dawson Point, dip a little south of west at an angle of between one and two degrees, rising into cliffs of over a hundred feet in height on the west side of Sutton Bay, and forming a somewliat elevated rocky plateau with a gentle westerly slope, corresponding mainly with the angle of dip t observed throughout this district seems perfectly explicable on the theory of differing phases of one great glacier, with comparatively short interven- ing lapses of time during its temporary recession and subsequent re-advance. ■] PLEISTOCENE. 131 I As the position of these first-formed ice-masses would of recessity be Where glac- 11.1, . n,,. • "'•''* were nrst largely determined by the position of the highest land then existent f.unud. in this region, it is probable that very early in the Glacial period there were two main gathering grounds or centre.s of dispersion for such ice. These would be situated respectively in the area to the north-west of Lake Teniiscaming, in the vicinity of the " Great Bend " of the IMontreal River and the high quartzite ridges to the west of Lady Evelyn Lake, and on the high rocky hills known to exist in the vicinity of the height-of-land to the north-west of Lake Temiscaming. It is probable that early in the ice age these local centres sent out T'"|ct's of _ "' ° I'iirly glaciers . glaciers which flowed over the lower lands and valleys to the south and may have been the cause of some of the striie observed on the rock-surfaces exposed in the valley of the Montreal River, as well as on the shores of Lake Temiscaming. Although it is possible that all such evidences may have been so obscured in the profound general glaoiaticii which followed as to render their recognition and correlation, mdters 'v" (»x,reme difficulty. We may suppose that local glaciers of tliii \dnO above referred to, increasing under favourable conlitions, eventually coalesced as parts of one great ice-sheet, of which the distributing centre may have been gradually shifted eastward towards the neighbourhood of Opasatika and Labyrinth lakes on the canoe- route to Lake Abitibi. There is likewise sufficient evidence, afforded by a study of the later striations, that must have been caused by temporary re-advances in the waning ice-sheet, that this eastward shifting of the main gathering-ground must have slowly continued, while the final recession was almost directly north-east. Tt is now a well ascertained fact that the motion of ice is one result- Conditions « . , . . , ,. , . 11 1 11 iit'terniining ing from its phi: ' city, resembling substantially the movement which (Hnction of obtains in an extrHi-iely tiiick and viscid fluid when spread upon any "'"''•"" surface and a H!.;i}>ly ft' froah material constantly added. It is there- fore obvious t' at *»\j. mclination, however slight, of the underlying surface or the interp>>. '♦:ion of natural barriers at or near the sources of supply were ii the u Vit instances the deteniiining causes of the general direction of the ice flow. This onward motion once imparted, was continued and depended subsequently not so much on the nature of the land surface on which the glacier reposed as upon the general slope of the upper surface of the glacier which inclination was imparted as a result of the unequal accumulation of material at the centres of dispersion. Y- the north nnd north-east of Lake Temiscaming the various passe:.. ' . valleys leading northwards across the height-of-land are a little lesstji-:. iOOO Ceet above the sea, although thb ^ncky ele- K\ 132 I NIPISSING AND TEMISCAMING REGION. > Pf illli Differential uplifts. Transjxjri- ation of material. Distance of transix)rt. Direction of transix>rt. Stratified deposits. rations in the immediate neighbourhood rise in general from 200 to 500 feet heigher, while some of the hills in the vicinity of Labyrinth and Opasatika lakes show an ele.ation of over 600 feet above the surrounding lakes. If added to the general slope thus obtained be taken, the rise consequent on a diflferential uplift gradually increasing in a northerly direction, the resulting slope would be sufficient to compel a somewhat rapid south-westerly flow in any glacier formed in this vicinity, while in addition it is probable that an ever increasing supply of icy material to the north-east, might so accelerate this onward motion that even the interposition of such formidable natural barriers as the deep gorge of Temiscaming must have been, with its steep opposing slope, only served as temporary checks. This great ice-sheet acted as an important agent of transportation, catching up and carrying forward 1; :.;;" quat titles of clay, sand, gravel and boulders from the higher elev. ; "^ the north to fill up the various inequalities of contour existiu. ither south. The drift material, though varying very much in thid region, is as a rule very coarse on the higher levels and on the hill-sides facing towards the south and south-west. On these higher levels the ground is very much encumbered by more or less rounded or subangular boulders which usually do not show transportation from any great distances ; although by a careful comparison of the material of this drift, it was ascertained that many of these loose fragments had been carried as much as fifty or sixty miles, in a direction closely corresponding with the striation marking the maximum extension of the ice-sheet over this district. Thus, loose fragments of the buflF-coloured limestone with characteristic nodular cherty matter, known to occur in a patch of somewhat limited area in the vicinity of the northern part of Lake Temiscaming, were found on Marten or Crooked Lake in the town- ship of Gladman, a distance of over fifty miles from where such rock is now found in place. The distribution of these characteristic frag- ments which are an especially valuable criterion of the direction of ice- flow, on account of the known limited extent of this Silurian outlier, shows that the agency which aflfected their transportation had a direction of movement varying from S. 7° W. to S. 18° W., thus agreeing very closely with the most abundant and pronounced striae. On Lake Nipissing, the various shales and grey wackes characteristic of the Huronian exposed in the area of the Lake Temiscaming map-sheet, are rather pl'-atifully represented among the loose boulders fringing the shores. The stratified sands and clays SvO abundant in the area to the north of Lake Nipissing, as well as those in the vicinity of the Veuve River, •J PLEISTOCENE. 133 I were probably deposited very rapidly from streams issuing from the margin or front of the retreating glacier, as was likewise no doubt the case with the thick and widespread deposits of stratified clay which forms such extensive flats in the region bordering the northern portion of Lake Temiscaming. The terraces characteristic of the occur- rence of these clay deposits to the north of Lake Temiscaming, merely serve as mark accentuating the various stages or baitings in the ice- sheet, of which the margin was buried beneath the rising waters, thus permitting and even favouring such a mode of deposition of the englacial detritus. Especially along the course of the Ottawa and Temiscaming Moraines. valley, the region exhibits frequent great accumulations of morainic dflbris marking the recession of the ice-lobe occupying this deep and important depression. These deposits from the drift-laden glac'&rs are described in some detail in the geological description covering the area immediately bordering these topographical features. Besides the removal and transportation of boulders, gravel and ( Jlaciation of other material, there is abundant evidence everywhere of considerable '"''" '''"'^ ^^' abrasion of the surface produced by the passage of the ice-sheet across this district. Throughout the whole area covered by the accompanying map-sheets, most of the rocky elevations have been smoothed and in many cases even polished, while scratched or striated surfaces are also common. These striie are usually long, more or less parallel scratches, varying in size from extremely tine lines which can often only be detected by very close scrutiny, to furrows several inches in depth and width. They have in general a somewhat constant direction except in the vicinity of deep and narrow valleys, where they frequently show con- siderable divergence from the average direction of the district. Many of these striu» consist of a series of irregular, curving and often faint scratches, as if occasioned by an uncertain or intermittent action while some of the deeper and more pronounced furrows exhibit irregular broken cavities at intervals in their course as though produced by d, that early in the ice age glaciers of the alpine type occupied the high hills of diabase and gabbro in the vicinity of the height-of-lanJ 'r .Tiediately west of the canoe-route between Lac des Quinze and Abitibi, ps well as on the high ridges of quartzite-grit to the west of Lady Evelyn Lake, of which Maple Mountain is the most prominent eminence. The striae which have the closest correspondence with the general trend of the valley of Lake Temiscaming and the Ottawa River were possibly caused by such a local glacier, as these markings are earlier than those which trend to the east on the one hand or to the west on the other. The striaj marking the main advance of the- ice-sheet in this region show a general trend of about S. 14° W., but many of the observations noted present a marked divergence from this general direction, especially those made in the vicinity of lakes and streams where these ice mark- ings show an unfailing tendency to conform very closely to the direction of the inclosing valleys. The earliest of these south-westerly ice markings are those which run nearly south, the direction of ice-flow showing a gradual change in the direction of successive re-advances, following temporary recessions, from a little west of south to almost directly south-west. In the area covered by the northern and central portions of the Lake Temiscaming sheet, there are many lakes whose general trend makes but a small angle with the average direction of ice-flow while their containing valleys are narrow, rocky and steep. The northern part of Temagami, Waibikaiginaising and Wakemika lakes BARLOW. ] LIST OF GLACIAL STRIiE. 135 I may be cited as examples where the glacial strife show a general direc- tion of a little east of south, in this respect showing the marked influence of topographical outline. In the subjoined list, which is necessarily brief and incomplete, con- List of striae, aisting of observations made during an exploration whose primary object was to map out and report upon the various subdivisions of the Archwan rocks, an attempt has been made wherever possible to tabulate in regard to their age the various striic observed. "Where two, three, and even four sets are noted as occurring on the same rock-surface, the order in which they appear is believed to represent, with approximate accuracy, their relative ages from the oldest to the most recent. List of Glacial Strict. Lake Temiscaming. Wabis Bay, west shore of, on lot 10, con. V. Bucke Township ... - iiAk^-m Wfibis Bay, east shore of, on lot 2, con. I. Harris Township S 19° E Sutton Bay, north-east shore of, on lot 8, con. V. Harris Tp .S 51" E East shore, west of Abbika Creek, on lot .38, con. I. (iiiigues Tp. . S HI" E Chiefs Island, east shore of a ,.,.o -t^. Chief.s Island, north shore of S (ifi^ E rs 14° E Chiefs Island, west shore of -^ S 48° E U 54° E East shore, on lot 31, con. I. Guigues Township S 32° E ( S 33° V Piche Point, south of, on lot 12, con. I. Guigu(!8 Township ' S 4(j° F East shore, north of Wright's mine, on lot 7, con. II. Guigues Tp. - L T.jo v Wright's mine, (Lake Temiscaming Silver Mine) on lot 62, con. I. . Duhamel Township "Block A" ^ f S *^H° E Joanne Bay, east shore of, on lot 58, con. I. Duhamel Township.. • 'tjf^^^y ( S *'fl° E East shore, on lot 54, con. I. Duhamel Township g " j.jj East shore, at Narrows with Bryson Island on lot 44, con. I. Duha- mel Township S 21'' E East i-hore, opposite Drunken Island, on lot 31, con. I. Duhamel Township S 4° W West shore on lot 14, con. IV. Lorrain Township S 4° W West shore on lot 12, con. VI. Lorrain Township S 21° E ( S r'°W West shore on lot 11, con. VII. Lorrain Township • • I S 18°W r S 1 8° E West shore, on lot 15, con. 1. Bucke Township -I y 2(i°'VV Laperri^re Bay, north shore of, ^ a mile east of old H. B. Co's ( S 21° E post, on lot 7, con. II. Duhamel Township I, S (1° W r S IT^W Islet near east shore about 1 mile south-east of Roche McLean ^ ^ 32°W Boche McLean, near west shore S 10° E V/'est shore opiwsite Roche McLean S 4° E West shore li miles north of Montreal River S 4° W f S 21° F West shore 1^ miles south of Montreal River | g j^yoyy ■' ;i ( : I 11:, 1 ■■: \\ i 1 I :^ List of striae— Cont. 136 I NIPIS9INO AND TEMISCAMINO REGION. Quinzft River. Islet opposite North Teiniscaiiiing, P.O. Near south-east shove I S 21' E I S 31° K At second rapid abovu Lake Teiniscaiiiing H 50" E On new roaci to Lac des Quinze, (5 miles east of First Rapid on River des Qiunze S 47' E Lake Temagami. North East Arm, west end of portage to Caribou Lake , rs 4 W JS14 W ts l'J"W North East Arm, Island in south narrows, two miles west of jiortage to Caritou Lake S WW North East Arm, Islet near south shore, h mile south-east ofjSlfi'W Ferguson Island " IS 20 W Nortli East Arm, island east of IJroom Island S 14'\V North East Arm, iM)int on south shore A mile south-east of Broom | S 9'W Island . . . . : t S 24 W Ko-ko ko Bay, East shore of, Ih miles south of north end H O^W Kuko-ko Bay, Islet near centre, 2^ miles soutli of north end S 14 \V Ko-ko-ko Bay, Islet near west side, S^ miles south of north end. ... S S°\V Ko-koko Bay, East shore of, 3A miles south of north end S G"W Ferguson Bay, east side, near southern end S 1'^ E f S (r F Ferguson Bay, point on west shore 1^ miles south of Ferguson Point ^^ «" w I S 1° F Sandy Inlet, point on south-east shore h mile east of Ferguson Point | a -.^o y ' ' E E Whitetish Bay, east shore, Ih miles south of creek from Whitefish / S 11"" E Lake : \S 4\V Whitefish Bay, p.-uit on west shore ^ mile south-west of creek from Whitefish Lake S 28° E Whitetish I5ay, islet in, nearly 1 mile south of creek from Whitefish / S 1° E Lake i S 1(5° E i S ^^ F North Arm, Point on west shore, ^ mile south of Deer Island i S 14° F South West Arm, island near north end of S 1!)^ W South West Arm, east shore of, 2 miles south-west of Narrows f S !>^W Island "I S 19° W I S 4°W South-west Arm, east shore of, 5 miles north-west of south end • • • • " ci i- \y is 1 ° Sandy Inlet, north-east shore, near mouth of Annima-nipissing River | ti i qo Islet, IJ miles south-west of fS 4 VV ■^sir Hudson's Bay Cos iwst -^ S 11°W tS29'W Islet Ij miles east of Hudson's Bay Co.'s post S 9° W Islet near north end of Island Bay Portage near south end of McLean Peninsula S 4° W f S 24° W High Rock Island, south-east shore of i S 2<»° W Cross Lake. West shore of lake, IJ miles south of Temagami River inlet S 5° W North ixiint of island, Ij miles south of Temagami River inlet S 3° W f S 2° F East shore of same island, 2 miles south of Temagami River inlet. . -I S 7'> w West shore, J mile north of Temagami River inlet S 13° W {S 2° F S 8° W Small island near west shore IJ miles north of Te»iagami River inlet. I a i k» w Point on west shore Ij miles north of Temagami River inlet S 5° W MRLOW. LIST OF GLACIAL STRI^. 137 I Area South-east of Lake Temagami. Island near south-east end of .Tniuping CarilK)u Lakt' S 14' W Marten Jiuke, acmth-west shore of, i mile nurtli-we.st of north town line of McLaren S 20' W Islet in Red Cedar Lake, lot (i, con. VI., Thistle Township i S l'"" W Tomiko Lake, north-west shore of, on lot .5, con. I., Fell Township S 1.5^ W rS 4'W Moxam Lake, north-east shore of ■! .S 22' NV ts 2!)' W Exiiectation Lake S 22° W Simpson Lake, at outlet ot S 22" W Sinijjson Lake, islet near north-east end of S 22" W Mackenzie Tjake, islet near east end of S 22° W Mackenzie Lake, east end of S 14' W Breadalbane Lake S 21 ' W Bush Lake (near headwaters of Ottertail Creek) S 30" VV Poplar Lake, west .shore of, on lot 2, con. III., Gladman Township S G' W Kaotisinewaning Lake, south shore of, in Xotnian Townshiii S 7° W Red Water Lake, west side of, nearly ^J mile from outlet S 20' W Lake Nipissing. Goose Islands i u oj.j \y Manitou Islands, must easterly islet of South Small island in Goulais Bay S 1.5" W Goulais Point S 25" \V Small island opiX)site lot 3, con. C, Caldwell Township S 19" W North shore of, on lot 7, con. C, Caldwell Township S 25" W North shore of, on lot 11, con. C, Caldwell Township S 25' W Point on west shore S 30" W South-east shore of Bear Bay, opposite Maskinonge island S 10' \V Deer Bay, south shore of (west arm) S 20" W North shore of, on lot 6, con. C, Springer Township S 14" W North shore of, on lot 5, c(m. C, Springer Township S 12' \V North shore of, point 3^ miles east of Dukis P jint S li)' W North shore of, point 4 miles east of Dukis Point S 14" W Clark (Sandy) Island, near western end ' p^' S" ' W Hardwood Islands, west end of S 20" W Island east of east end of Hardwood Islands S 25' W Scuth Bay, east shore of S 23= \V List of striuj — Cant. Lady Evelyn Lake and vicinity. Point on north side of largest island in Lady Evelyn Lake, 3 miles south-west of Obisaga Narrows S 4' W Island in Lady Evelyn Lake, 3A miles south of Obisaga Narrows. . S (5" W f S 5" \V South-west shore Nonwakaming Lake, 3 miles west of inlet ' S 21" \V Island near east shore Nonwakaming Lake, about 2 miles north- / S 3' W west of inlet 1 S 20" W I S H" V West shore Wakemika Lake I S 22' E r s ^^ 1*^ South shore Wakemika Lake ' S 1"" E Turner Lake, south-east shore of S 10" W Area north-east of Lake Temagami. Net Lake, east shore of, near north end ; S 4" W Loon Lake, south end of S 3" W Ko-ko-ko Lake, east shore of, i mile north of outlet S 18" W {S 2" V s vw ii 138 I NIPI88ING AND TEMISCAMINO REGION. T^iHt of Tetapaga Lake, north shore of, 1 mile eaut of outlet S 1° W Htrie- CojK. Turtle Lake, north Hhore of {s 26° W v.' Vermilion Lake. I' i -f 1 \ ■ 3 s s s {i "IS s Island in Vermilion Lake, A mile so>ith-\vest from north-east end. . S Turtle Lake, small island near north sliure of Waibikaiginaising Lake, island near east shore of, 3 miles from J south end East end of portage between Summit and Friday lakes Friday Lake, west shore of, IJ miles north of outlet. . Bear Lake, east shore of, 2 miles north of outlet 10^ W 15- \V 30° W 52^ W rE !t°E 29° E 8°E 18^ E f)°E 16= E 4°W 8° W Wickstead (or Shabosaging) Lake. On rocky islets, 1 J miles south-west of inlet On south-east shore, IJ miles so\Uh-west of inlet On north-west shore, 2 miles south-west of inlet. On Rocky islet, 4J miles south-west of inlet At Narrows, 2^ miles north-east of outlet On islet near west shore, 4^ miles south-west of inlet On islet near west shore of big western bay, 4 miles south-west of inlet On west shore, 1 mile north-east of outlet Annima-nipissing Lake and vicinity. West shore of bay on route to Mountain Lake t S 14° W \S27°W S27°W S 240 W S 27" W. f S 14° W I S 24' W /S24 W IS34^W fSlSPW \S24' W / S 23° W (.S3rW {| Island near centre of lake, 4 miles from north end . - ^ Is (Jull Rock Lake, north-east shore S Carrying Lake, south shore of - o Diabase Lake, south shore of - u West shore, 3i miles from north end 10° E 2°E 3° W (i° W 37° W !»° W 20° W 29° W 20° W 7°W 20° W 3°W 18° W Rabbit Lake and vicinity. f S 1° W Rfibbit Chute on Matabitchouan River, at outlet of lake -^ a g° w West side, i mile south of Rabbit Chute S 3° W rs 3°w Is 8° W Burnt Point, on west side of south end of Outlet Bay -I u 330 -^y Is 38° W South-east shore, 1 mile north-east of Rabbit Point S 13° W /-S 2°W I S 13° W Point on east shore, i mile north of Rabbit Point -! ^ 3.0 -^y U 42° W »*«"'«'] ECONOMIC GEOLOGV. 139 I iHland in Rabbit Lake, op|)o.site Rabbit Point 9 "fi^^W List nf rS 4' W striie— Cont. RosH Lake, soiith shore of "ze, north-east end. Chalcopyrite and quartz. Pyriti^ .and pyrrhotite and (luartz. Pyrite in (piartz with ferric hydrate. Trace II M None Trace Quartz aHsay.s, In addition to these, samples of cjuartz containing in some case pyri- Nipis.sing and ^^^ material were sent to the Director of the Geological Survey, but vicinity. their assays by Dr. Hoffmann did not afford any encouraging results as far as regards their gold and silver contents. These samples were from Lake Nipissing and the region adjacent and the results of their exami- nation in the laboratory of the Survey may be referred to as followst : — Locality. Description of Specimen. Weight. Gold I Silver per ton. 'per ton. Sturgeon R. (branch of) N. of Badgerow Tp. Small island in Lake Nipis- sing. Vein crossing inlet, W. end Lake Nipissing. Great Manitou Island, Lake Nii)issing. TwonnlesW.N.W.ofN Bay. Finelv crystalline galena and cfialcoi)yrite with a little (juartz. Chlorite-schist, inica-schi^t, gneiss and calcite with a little pyrrhotite and py- rite. Rust-stained quartz & gneiss. Felspar and quartz with nio- I lybdenite and pyrite. North] Rust-stained quartz with py- rite. (52 oz. 8 t, i -1 4i lbs. very dis tinct traces. 15 ■ 75 oz. ■IIG ., Character of In the area characterized by the presence of Huronian rocks and oniaii rocks, their associated eruptives, a large quantity of whitish or grayish ♦Annual Rei^rt, Geol. Surv. Can., vol. III. (N. S.), 1887-88, part T, analyses Nos. 11-13. fAnnual Reix)rt, Geol. Surv. Can., vol. II. (N. S.), 1886, part t, analyses Nos. 53. Vol. IV. (N. S.), 1888-89, part h, analyses Nos. 82, 84 and 86. ■ARkOW ] ECONOMIC GEOLOGY. 141 I foiinrl in them. translucent quartz h an almost invariable accompaniment of any extended exposure of rock. This cjuartz is seen to represent segregations of secondary silica filling in the various cracks and fissures caused by the profound orograpliic movements through which these strata liave passed. Sometimes this vein-quartz is in the form of lenses or eyes occupying various small gaps or openings in the rocks, these gradually increasing in size until lenticular masses of ([uartz of considerabledimeu- sions are formed. In some cases these masses run for considerable dis- tal 1^' approximate in character to true fissure veins, although large am, J jiical examples of such veins are exceedingly rare in this region. Both in their horizontal and vertical extensions these " gash-veins " are exceedingly irregular, and in no case noticed can any great reliance be placed on their persistence in any direction. Calcite and dolomite often occur in association with the quartz of such veins, with varying quantities of pyrite, chalcopyrite and galena ; while sphalerite and hiematite (micaceous iron ore) are occasional constituents. The quartz is very often more or less cavernous or cellular, owing to the ox- idation and partial removal of the sulphides originally present. Where pyrite has been abundant the quartz is more or less rusty, while the various cavities are partially filled with ochreous material. On the other hand, where copper-pyrites is the more abundant, the quartz is more or less stained and coated with green and blue carbonates of copf Occasionally the galena shows a thin coating of carbonate of ?erussite) where exposed to atmospheric action, and Dr. Hoflfmann makes a note of its occurrence at the Macinac lead-vein on Haycock's location, east side of Lady Evelyn Lake, one and a quarter miles south of the outlet.* In origin, many of these quartz veins, and especially the larger ones, '|'i,^.jp origin are connected with the eruption of the large masses of diabase and granite that invade the stratified slaty rocks, and often they are either on the line of junction between these two rocks or occupying breaks and fissures in its immediate vicinity, produced during the eruption of these igneous rocks. Occasionally, such secondary veins of quartz occur in irregular fissures in the diabase itself. Some of the most important of such veins noticed, occur on the ,r • _ _ •^ Veins on " Mattawapiki," as the last stretch of Lady Evelyn Lake before Lady E^Nclyn reaching the Montreal River, is called. The western shore of this * *^' portion of the lake is composed of diabase, that rises abruptly from the surface of the water and often from steeply sloping or perpendicular clifis. The contact between this rock and the slates is concealed for * Annual Report, Geol. Surv. Can., vol. IV. (N.S.), 1888-89, part r, analysia No. 60. ir 1 I r £S'.:i:M '{I jj ^ii^ Haycock location. .\!says. 142 I NI PISSING AND TEMISCAMING REOToN. the most part by the lake, the eastern shore being altogether composed of a very distinctly banded greenish slate, which also rises into rather important elevations, having apparently been protected to a consider- able extent from denudation by the proximity of the more unyielding diabase. The contact, for a short distance, runs inland along the western shore, leaving a comparatively narrow strip composed of the slates, which are seen to have lieen much shatterea and broken up liy the intrusion of the diabase. Some considerable masses of segregated quartz were here noticed filling irre'^ular cavities and fissures produced during the eruption. Associated with the quartz is more or less calcite, and in this gangue were noticed galena, copper-pyrites, iron-pyrites and zinc-blende. The banded slates on the eastern shore dip in an easterly direction at an ani,'le of about 18°, and associated with and cutting these are similar segregated masses or " gash-vein," in which galena is the prevailing constituent. The property on which these veins are situated is owned by Messrs. Klock and Haycock, and is locally known as the Haycock mine or location. A considerable amount of development work has been done, looking chiefly to testing th.e quality and extent of the ore-bodies, but the inaccessability of the locality would be a sufficient hinderance to any further operations, unless the deposit should prove of an exceptionally rich character. Assays of representative samples from these and similar veins exposed in the immediate neighbourhood, have been made in the laboratory of the Survey, which may be summarized as follows* : — Locality. Description of Specimen. Weight. 1 lb. ooz. Gold prton. Silver per ton. W. side Lady Evelyn Lake, Quartz v.ith a little calcite Traces 204 near outlet. and chalcopyrite K. side Lady P]velvn Lake, (laleiia with a little quart/. 6ibB. 12oi:. ti 875oz. 1:^ nnles S. of outlet. and calcite. \V. side Lady Evelyn Lake, Quartz with a little chalcopy- 2 lbs. None. OllToz. 14 miles tS. of t)utlet (north rite, galena and zinc blende W. side Lady Evelyn Lake, Quartz vatli chalcopvrite 2 lbs. M None. H miles S. of outlet (south vein). W. side outlet Lady Evelyn (Juartzwithcalcite.dolomite, 1 lb. 12 oz. ,, II Lake (west vein). serpentine and chalcopyrite Island at Narrows, 3 miles S. Quartz with chlorite 13 oz. :l II of outlet of Lady Evelyn L Oocklinrn The Cockburn location or mine covers several small islands in location, Cross Lake. Cross Lake, near the inlet from Temagami Lake. On these islands, •Annual ReiKirt, Geol. Surv. Can., vol. IV. (N. 3.), 1888-89, imrtit, analyses Nos m-VA. •ARLOW. ] ECONOMIC GEOLOGY. 143 I several masses of segregated quartz are exposed, but these apparently have no great regularity or persistence. The largest of these so-called veins is situated on the west side of an island about a quarter of a mile in length, about half a mile south-west of Temagami River. The island is composed of a greenish-gray, greywacke, slaty in structure^ which has undergone considerable alteration, and sericite is rather abundantly developed, especially on the planes of cleavage. The pressure or foliation planes, which are here apparently the only structural features displayed by these rocks, have a strike N. UV E., and an inclination eastwards <7V. The quartz fills an irregular fissure in the slates, is about five feet in width, has a strike of N . 38' E., and nn underlie towards the south-west <45°. Galena, iron-pyrites, copper- pyrites and malachite were all noticed imbedded in the quartz. Samples taken to represent the average of these were examined in the Assays. laboratory of Survey with the following results* : — i- Locality. Island in Cross Lake iiear outlet Cross Lake Cross Lake (same loc. as last) Description of Specimen. Weight. Quartz with galena and chal- copyrite Quartz with chalcopyrite . . . Quartz with galena lb. oz. 1 10 !) 3 Gold per ton. none .058oz. trace Silver per ton. •175oz. •0.58OZ. 2:i.3;ttoz. Mr. p. A. Ferguson of Mattawa owns three mines or locations on Fergvistui loca- Lake Temagami, known respectively a^ A, B and C. At location A, Temagami. situated on the east side of Sandy Inlet in the northern part of the lake, the rook is for the most part a massive dark-green medium- textured diabast, much of which is broken up ; the irregular cavities being filled with quurtz and calcite, with which are associated yellow epidote and small dodectedral crystals red garnet. One of the veins from which considerable Material had been taken was noticed near the water's edge and contains in. addition to the minerals mentioned above, a little iron-pyrites and copper-pyrites. The vein is very irregular and only about a foot in width and thus too small to constitute a workable deposit. At location B, situated on the north shore of the north-east arm of Lake Temagami, about two miles east of the portage into Caribou Lake, the rock is a pearly grayish-green sericite-schist, striking N. C8" E. and dipping northwards <70\ Associated with this is a lenticular mass of light-gray rusty weathering dolomite, containing reticulating veins of quartz, that stand out on weathered surfaces. Chiefly at the contact between these two rocks, is a considerable deposit of iron-pyrites, *See Annual Report, lieol. Surv. Can., vol. IV. (N. S.), 1888-89, jmrt u, analyses Nos. 54, 57 nnd 58. i 'M! ! I ' I ^^m 144 I NIPISSING AND TEMISCAMING REGION. i ' AMsays. Veins on I)('n«hi« Island, Lake 'rt'inaKiinii. Assays Veins on TeniaKanii iMlanu. with a little copper-pyrites and arsenopyrite (1) Location C, is on an island now known as Ferguson Island, to the south-west of this point and consists of iron-pyrites in association with sericite schists. Assays of specimens taken as representative of these three deposits, ffave the following results in the laboratory of the Survey* : — Locality. Description of Specimen. Weight. (Jold Silver per ton. (ler ton. Ferfrnson Location A, Sandy (Juart/. with little pvrite and Inlet fi. Tcniapann chalcom'rite lllbs. trace trace Ferffuson Location B, north (inart/. with finely disseniin- east Ann L. Teniajranii. ated pvrito filbs. none .2330Z. Ferguson Location C, Is'd. in Rust-stained sericite schist N.E. Arm L. Teniagaini with i)yrite 15o/.. trace •II60J!. The Denedus Islands near the entrance to M uddy- water Bay on Lake Tomagami, and so-called after a well-known member of the Temagami band of Indians, is another mining location, owned by Mr. James Holditch of Sturgeon Falls On the two large islands composing this group, the rock is a dark greenish-gray felspathic sandstone or grey- wacko, sometimes slaty in structure but usually massive. The rock is much broken up in places, and the irregular cracks and cavities thus formed are filled with gray translucent quartz, with which is usually associated more or less pinkish dolomite. Occasionally these fissures are so large as to include considerable masses of quartz On the west island a quartz vein about two feet in width, occurs with a south- easterly strike containing both iron- and copper-pyrites. A some- what larger segregated mass of quartz occurs on the island to the east, with similarly disseminated grains and fragments of iron- and copper- pyrites and occasionally a little galena. Assays of specimens from both these islands were made in the laboratory of the Survey with the follow- ing resultst : — Locality. Denedus Islands (east vein). Denedus Islands (west vein). Description of Specimen. (Quartz with a littlt^ chlorite and dolomite Quartz with chlorite chal- copyrite and pyrite Weight. (4old l>er ttm. lbs. oz. 2 (> none » C trace Silver jwr ton. none trace Large masses of iron-pyrites, associated with pyrrhotite, copper, pyrites and magnetite, occur on the east side of Temagami Island in •Annual Rei^rt, Geol. Surv. Can., vol. IV. (N. S.), 1888-89, part K, analyses Nos. (i9-7L fAnnual Report, (!eol. Surv. Can., vol, IV. (N. S.), 1888-89, jiart H, analyses NoH. 79-80. i 'i 1 ECONOMIC GEOLOGY. 145 I Lake Tt'inagami and on the south-east shore of YermiHon Lake, to the nortli of the north-east Arm of Lake Teniaijami. Samples of these were assayed for goUl and silver, but with negative results in both cases. Subse(]ueiitly Mr. E. V. Wright, who had located the Vermi- lion Lake property had the ore assayed for nickel, but less than one per cent of this metal was found. The follovviny; statement yivesthe results of the assays made* : — As.siiya. T.doiilitv. Di'scription of Siiec'inion. NVeight.i HoUl ! iiwr tim. 'rt'iiiiiKatiii Is"(l. (('list sin >ro). i I'y rite, clialco|)yriti', iimgue-; j i titt', «itli cliloritc 4 2 | iiinif N't'niiilioii Livkc I'yiittMii clilDritc-.scliist imil; i ([iiartzito I 13 " Silver per toil. Ill On Matthias Island, about two miles north-east of the Hudson's 15ay On Muttliiiis Co.'s post on Bear Island in Lake Temagami, a (juartz vein with a S(ime- what uniform width of about eight feet was noticed. The quartz is white and translucent, filled with rusty cavities and a little copper- pyrites, ii'on-pyrites, malachite and aidverite were noticed Although 80 promising in appearance, assays made in the laboratory of the Sur- vey show neither gold nor silver, f At the (.uay mine, in rear of the Township of Fabre, on the east rt'usonT3ay, Lako'Cak'ite with a little chlorite Tem;igaini. I and elialcopyrite. Small islet in Wliitefish Bay, (Quartz with jiyrite in fels Lake Teniagami. | jiathic sandston(>. Islet ij mile AV . of Temaganiiitjuartz with a little dolomite Po>t. and chlorite. Twt) miles N.-\V. of Tema- ( hiartz with chlorite and a gami Post. Island neai' S. end S.-W. arm Lake Teniagami. Mountain Lake, ^Montreal River. Portage near S. end of Lake Temagami. Island Ij miles N.-E. Tema- gami Post. little pyrite. Rust-stained quartz with a little ))yrite. Rust-stained quartz with py- rite and elialcopyrite in diabase. CJuartz with chlorite and dolomite. Rust-stained quartz with a little ilmenite. :we ght. 1 lbs. 7i 2 10 1 14 1 3 14 1 11 ■I 3 H 1 1 h 2 11 1 7 Tri'ce I None. I I None I II Trace l'2!)0oz. I None liNone. Distinct! n trace. I None ! II I Ti-ace i Trace. Ni )ne i None. Trace None Trace Trace. None. little explor ation as yet. Comparatively Although the results given in the above tables are not very encourag- ing, it must be remembered that the assays were made from material obtained during the progress of an exploration over a wide stretch of country in which only limited opportunities were aifoi-ded for exfimina- tion and selection while only those quartz masses were visited which were noticed exposed at or near the shores of lakes embraced by the survey or in localities otherwise accessible. No systematic attempt has ever been made at prospecting throughout the greater portion of the dis- trict, although a few enterprising individuals have looked over part of the area in the hope of finding some unusually rich mineral deposit. A large portion of the area covered by the Huronian rocks in the north-western part of the region, is thickly covered bj' forest, composed chieily of evergreens, which conceals much of the surface, rendering *Annual Report, (Jeol. .Surv. Can., vol. III. (N. S.), 1S87-H8, i)art T, analysis No. 32. fAnnual Report, (Jeol.Sinv. Can., vol. IV. (N. S.), 18.S8-89, part K, analyses Nos. 10, 72, 73, 75, 77, 05, 07, 08. 87 81 (iij •] ECONOMIC GEOLOGY. 147 I any attempt at prospecting difficult. The inaccessibility of the region has also generall)- prevented any extended examination by prospectors, but the recent survey of the Nipissing and James Ray railway and the proposal to run this line northward from North JJiy to the east end of Lake Temai,'ami, has again drawn attention to this region as a promising mining field. The Huronian bolt of rocks is tiie same that Coiiditions traverses the Sudbury mining district to the soutli-west, while similar yii-'jiju'ly' '^'' associations of slate and greyvvacke broken tlirough by diabase, gabl)ro and granitic intrusions, furnish conditions eijually favouraVile to the presence of metalliferous snlphides or gold-bearing quartz-masses now known to exist in the vicinity of Wahnapitae Lake, immediately adjoin- ing the Temiscaming sheet to the south-west. One of the most important of the mineral deposits in this district, Wiight mines both on account of it-; comparative accessibility and the character and ^'^^y 'iVinis- size of the ore-bearing body, is wliat has usually been known as the Lake Temiscaming silver or lead mine (Wright's mine) comprising portions of lots 61, 62 and 63 of range I., in the Township of Duha- mel, in what are called Blocks A and B, on the east shore of Lake Temiscaming. Although, this deposit was brought to notice by Mr. E. V. Wright, of Discovery, Ottawa in 1877, the existence of ore at this place was known long before, for on a " Map of North America,"* based on D'Anville's map, and published about 1778, the small bay on which it is situated is named " Anse a la Mine." In the vicinity of the mine, the rock is the breccia-conglomerate form. Association. ing the basa! member of the Huronian in this district, the pebbles or fragments of which are chiefly of granite, diabase or other eruptive rocks, embedded in a greenish, chloritic, slaty matrix, which owing to pressure appears to curve around or enfold the inclosed fragments. The deposit occurs in a brecciated or shattered belt of the rock, ch.iiactcr composed of angular or subangular fragments, the interstices being of deposit, filled by galena with occasif)nally a small quantity of iron-pyrites together with more or less pink dolomite. Although this zone is about eighty feet in breadth and contains a varying quantity of galena throughout, only about six feet can be said to carry the mineral in workaVjle quantity, and even this with considerable admixture of gan- gue and rocky matter. The rock immediately adjoining and inclosing the deposit, has a decidedly porphyritic appearance, crystals and frag, raents of white felspar and grains of transparent quartz being embed- ded in a fine-grained greenish matrix. Under the microscope, this fine. *See Map No. 5, Mills' Reixirt ou Boundaries of Ontario, Torontmtinuity through the Temaganii and Temiscam- pyi'it««- ing districts. Diabases and gabbros apparently identical in their com- position and appearance are present over large areas, but so far no very large deposits of pyrrhotite and copper-pyrites have been found. On the west side of Tema;;ami Island, as well as on the south-east shore of Vermilion Lake, considerable masses of these sulphides are present, but the assays made show only a very small percentage of nickel. Copper-pyrites is an almost invariable constituent of the diabasic masses and in places pyrrhotite is equally abundant, and it is highly probable that systematic prospecting may develop large deposits con- taining nickel and copper. At the Guay mine, in rear of the Township of Fabre, the specimens of copper-pyrites gave, according to Mr. Obalski, 72 per cent of copper, and -OS per cent of nickel. The inaccessibility of the region, however, and the abundance of these nickel and copper bearing sulphides in close proximity to the main line of the Canadian Pacific Railway, in the Sudbury mining dis- trict, many excellent deposits of which have not yet been developed, prevent any extended search in the Temagami and the Temiscaming districts. I !ii I I f I \ I 150 I NIPISSIJrO AND TEMI8CAMING REGION. In oil. OcourriTicc.s of iron ore. At Ket'pcwa Lake. On Iron Island, Luke Ni pissing. Ore not abundant. No depcsits of iron ore of economic importance have as yet been found in tins district, although both niaj,'netite and hannatite are ratlier abundantly di.stributetl. Wherever nuticed, the (juantity has been too insignificant, or the as.sociati(jns tiucii that the material seen could not be utilized with any degree of profit. Magnetite occurs in patches and small masses in the red granitoid-gneiss exposed in the neighbour- hood of the Chute des Paresseux vi\ the Mattawa, in the township of Olrig. On the west side of Keepawa Lake, a short distance north-west of Cordon Creek outlet, a dark-gray gneiss containing a consider, able proportion of magnetic iron ore occurs, and a (juantity of this ore was mined and taken to the Wright mine on Lake Temiscaraing for use as a ilux in the smelting of the galena. The ore, however, is too lean and silicious to be of commercial importance. On Iron Island, according to Mr. Murray,* " small masses of specular iron ore are common to most of the rock in the island and in the crys- talline limestone, there is a very great display of it. For a breadth of about forty yards along the cliil on t'ie east side, the rock holds masses of the ore of various sizes, sometimes running in strings of an inch thick or upwards, elsewhere and at other times accumulating in huge lumps, someof which probably weigh over half a ton. Thebeach near the outcrop is strewed with masses of all sizes, from great boulders weighing several hundred pounds to small rounded pebbles not bigger than marbles. The limestone with which the iron-ore is associated is frequently cavernous, and the crevices and smallerfissuresare thickly lined with crystals of blue fluoispar and red sulphate of barytes or cockscomb-spar. Crystalline limestone crops out on the opposite or west side of the island, and, judg- ing by the strike of the north side, it must correspond with that holding the iron-ore on the east. The same minerals were found disseminated thi'ough the rock and strewed upon the beach. At the extreme south- west point of the island the rock is again crystalline limestone, and a long leach running out from it to the westward is perfectly covered with I)oulders of specular iron-ore. Iron-ore occurs also at the south- east point of the island, although not in such great abundance and only in detached masses strewed upon the beach." Several parties have searched rather thoroughly over this island and most, if not all, of the iron has been carried off and shipped away. The interior of the island is a veritable jungle, and the shore is lined with an almost impenetrable thicket of scrubby cedar. Several small pits were noticed which had been sunk near the north-east corner of *Keport of Progress, Geol. Surv. Can., 1853-50, p. 123. magnetic r •] ECONOMIC GEOLOGT. 151 I the island, l)ut the amount of ore s' cured apparently did not warrant any further outlay of time or money, and it seeuis pretty certain that this ore is nowhere present in workable (juantity. At the time ot the writer's visit early in the spring most of the beach was submerged. Magnetic iron-ore, interlaminated with bands of red, gray or black silicious, .slaty rock was noticed in several localities, and in such con- siderable (juantity as to constitute depcsits of workable size, but the abundance of intermixed silicious matter is probably such as to render them practically valueless. One of these deposits is situated on the south-eastern end of a group of three islands near the eastern shore, about three miles from the southern extremity of the South-west Arm of Lake Temugami. The exposure seen consisted of alternate bands of light- and dark-gray quartzite^, the dark bands being composed almost wholly of grains of magnetite. It is curiously contorted, but has in general a dip N. 7" K. <45°. In immediate contact with this to the south, is a band of disintegrating greywacke and chlorite schist, dip- ping N. 9° E. < 55°. This is tilled with pyrite, which has evidently been the chief cause «)f its decomposition. The local attraction of the magnetic needle was so great at this point as to render the compass practically useless. Near the west end of Tui'tle Lake, to the north of the north-east arm of Lake Temagami, there is a somewhat similar deposit, consisting of alternating reddish and black bands of hanuatite or jaspery iron ore and magnetite, with some olive-green shale. The strike of the deposit accords with that of the sericite-sehists in the immediate vicinity, being N. 74° E. with a dip northwards < 70. In this neighbour- hood also the compass was much affected. A third locality in which magnetite in similar association occurs, is on the Quinze River, on the tenth portage from Like Temiscaming. Mr. W. McOuat thus describes the deposit : *" The portage is on the south, or left hand side of the river, running in a direction about south-east to a small lake in a narrow ravine, and is not more than a quarter of a mile long. The iron ore crosses the portage near the upper or south end. It occurs in the form of layers from the thickness of paper to about an inch, and is interlaminated with similar layers of whitish, gray and dull-red fine-grained quartzite. The iron-ore constitutes prob ably from a fourth to a third of the whole, and as the thickness of the whole band is about thirty feet, the whole thickness of the layers of iron ore would probably not be less than eight feet. The band was traced along the strike for about a hundi-ed yards. Magnetic oxydeof '■ Re|)oit of Pr()gre.s», (ieol. Surv. Can., 1872-73, p. 131-132. Iron nil couth-west arm, Lake Teinagaini . On Turtle Lake. On < Quinze River. ^ !■ ! i ! ■ i- I i I : 152 I NIPI8SING AND TEMISCAMINO HKCilON. m \ I li iron was observed under similar conditions at several points on this portage, and on the next above, but in much smaller quantity." On Vermilion Magnetic iron ore also occurs, but mixed with sulphides, on the * ''■ south-east shore of Vermilion Lake and on the east shore of Teniagami Island, in Temagami Lake. HiiMuatite (as micaceous iron ore) occurs as a rather common constituent of the many quartz veins cutting the Huronian throughout the northern part of the area, but it has nowhere been found in deposits of sufficient extent to be of economic value. Occurronrc (if Although of no economic importance, it will be of inteiest in this pertlihe'^' " '" connection to note here the presence of native iron imbedded in the crevices of some specimens collected on Mr. McMeikin's farm, about 4^ miles east of Mattawa. This occurrence of native iron, to which Dr. Hoffmann's attention was lirst drawn by ]Mr. 31. L. Droadbt-nt, was observed in some specimens collected as samples of perthite and araazon-stone on lot 7, con. B, of thj township of Cameron. The fol- lowing is a description by Dr. Iloil'mann : Description byriJr. Huff mann. Analysis. ■"■"The perthite, consisting of interlaminated brownish-red to red- dish-brown orthoclase, and reddish-white albite, contained here and there inclusions of a grayish-black, massive, pebbly magnetite, partiallj'^ altered, manganiferous magnetite, affording a dark reddish brown streak. " Portions of the felspar showed marked signs of weathering, the albite more especially being more or less kaolinized. Imbedded in the kao- lin, also in the dark reddish-brown limonite in immediate proximity to it, were observable numerous spherules of a steel-gray colour and metallic lustre. These spherules varied greatly in "-^e, a few measur- ing as much as a millimetre in diameter, the greater numbei-, however, being of far smaller dimensions, and many of microscopic minuteness. They were almost perfectly spherical in shape, strongly magnetic, very hard, indenting and scratching a hardened steel mortar ; brittle, when pulverized emit a distinct phosphoretted odour ; immersed in a solution of cupric sulphate, become coated with a lilm of metallic copper. They were readily attacked by hydrochloric acid with evolution of hydrogen and a strong odour of phosphine, leaving an insoluble residue consisting of light-brownish coloured spherules which on ignition become perfectly white. These spherules, which form tl\e nuclei of the metallic-looking grains, have, apparently, a concretionary structure. " Mr. Johnston found the metallic spherules to have a specific gravity at 15-5° C. of 7*257 and a composition as follows : — * Annual Reiwrt, Geol. Surv. Can., vol. VI. (N.S.), 1892-93, p. 23 n. ■ARLOW. I ECONOMIC nEOLOGY. ir)3 I Iron 9045 Miuiffniicse 075 Nickel trace Sulphur "j l'lii>s|ihi)nin ^ iindet. Organic nuittcrj Insoluble, non-metallic, residue 7 '21) tl.S-4() ■ \ / LinieKtdiir Lake Teui earning. "Cobalt and copper were sought for and found to be absent. He fuumi the insoluble non-inetallic residue to contain 88'77 per cent of silica, a little alumina and ferric o.xide — not estimated, a very small quantity of lime and possibl}' some magnesia. " This occurrence recalls to mind that observed by me in a specimen of Iluronian quartzite from the north shore of St. Joseph Island, Lake Huron, Ont.* Limestone and Lime. On Lake Temiscaming, the Niagara formation so abundantly exposed on the islands and shores of its northern portion affords an unfailing supply of excellei\t building stone, in blocks of large dimensions if required, while its fine and even texture as well as its colour recommend it strongly for such purposes. The Anglican church at Haileybury, on the west side of Lake Temiscaming, is being wholly constructed of material procured from exposures of this limestone on the east shoi'e of Mann or Burnt Island. For purposes of making quicklime, the more thinly bedded fossiliferous portions seem to be most suitable as furnishing the purest and best lime with least expenditure of fuel. The Manitou Islands, in Lake Nipissing, especially Macdonald or On Lake Little Manitou Island, have furnished limestone which was used to 'l*^''*'"^- advantage during the construction of the Canadian Pacific Railway. An excellent lime-kiln was noticed on Macdonald Island, which had evidently been used extensively. To the east of Mattawa, and between this place and Deux Rivieres, a good deal of lime has been manufactured for local consumption, as also near the foot of Talon Lake on the Mattawa River. In the former instance the various out- liers of Trenton limestone have supplied the material, while in the latter a band of crystalline limestone has been made use of by the incoming settlers. This band of limestone would furnish a very pretty serpentine marble or ophicalcite. When calcined, the deposit of marl covering the greater portion of the bottom of Emerald Lake to the west of the Opimika Narrows, on on IS- Jll i m m Trans. Royal Soc. Can., vol. VIII., sect. III., p. 3!), 1800. :f ' l')i 1 NIPI.SSIN(i AND TKMISCAMINO HEOION. Huilding stones. Lako Tciiii.^c.iiiiiii^', would furiiLsli ii iioarly puro and vt-ry wliito limo well a(lii{)tufl for luoriar ami oIIkt purposes. For such purposes the marl should bo inoulchnl into bricks which, after drying, may he Imrnt in a kiln. It might also ho omployiHi for whitowashing farm and other buildings. Granite tind (ineix>t. During tho construction of tho Canadian Pacific Railway, tho gray- ish evenly foliated gneissic rocks, often easily procurable in large blocks, were used for bridge-piers and culvert work with satisfactory results. Many exposures capable of yielding both gneiss and granite of excel- lent (juality mi'v Vie found at intiirvals along the lino of railway. On Temis^ aing L; '.e, in the vicinity of Baie des Peres, there is a very befiutiful deep llosh red granite, in which the more or less rcAinded outlines of the disseminated grains and fragments of grayish translucent quartz give the rock a fine conglomeratic or prophyritic aspect. It is not known, however, whether this granite can be obtained sutdci- ently fr'ce from joint's. Throughout the entire area the frequent and large masses of griinite exposed, as well as tho more massive and granitoid portion of the rocks classified as Laurentian, would furnish building stones of good quality, but only the more readily accessible localities of such rocks can be supposed to possess any importance. Flagstones and Slates. Flags. The better qualities of slate do not occur extensively in this region, but some portions of the strata constituting the slaty or middle mem- ber of the Huronian, present very line-grained and fissile beds which are firm and strong : although most of the specimens seen are rather thick for I'oofing purposes. Search might reveal some localities where suitable material occurs in sutHcient abundance to be of economic im- portance. Many portions would however seem to be well adapted for flagging. On the east side of Lake Temiscaming between McMartin Point and Latour's mills, the shore-line for several miles is formed of vertical cliffs of very evenly banded or foliated micaceous gneiss. The layers are extremely regular, fissile and of suitable thickness to yield flagstones of the very best quality and of almost any size. Litliographic Stone. Lithographic Some of the finer-grained beds present in the Niagara outlier on stone. Lake Temiscaming, exposed on Mann or Burnt Island as well as at 1 ] ECONOMIC OEOLOOT. inr, I Dawson (Wain) Point on the mainland to the north, exhibit portions wiiich wore thought to be suitable for lithographio purposes. .Some ([uairying waa done on the west shore of Mann Islnnd, iit.fl lately a company with heaihjuarters at Vankleek Hill comnu iu'wl operations in the vicinity of J)awson Point with a view to yi-ouring suitable material if possible. So far, however, the specimens ptocureil are not sutlicicntly uniform in texture, but it is still pot^siblo that litliographic stune of economic value may be discovered. Further examination of theso beds with this object seems desirable. t- v: Felspar, Although this mineral is abundantly distributed as one of the F.l^pir. most iu)]iortaiit and characteristic constituc^nts of these crystalline rocks, only a very small proportion is found pure enough antl in sulKciently large masses as to be employed for industrial purposes. To be of value, the deposits must be readily accessible and must con- tain the mineral in large cleavable masses easily freed fi'om other associated minerals or impurities by a rough cobbing before shipment. There are many large pegmatite dykes close to the line of the Can- adian Pacific Ptailway throughout this district, which might bo examined with a view to obtaining supplies of felspar. Some of these near Nosbonsing station seemed to furnish abundant and very suitable material. Felspar is chiefly employed in the manufacture of porcelain and pottery. Shell Marl. Deposits of this kind are frequently found below accumulations of peat, the marl in these instances being, therefore, 9l not very recent formation, but in other cases it is found to be still in process of deposi- tion, covering the bottoms of shallow ponds or lakes. Emera' 1 T.ake, about five miles west of the Opimika Narr »ws, is at tl head waters of one of the branches of Opimika Creek, which ■aches Lake Temiscaming from the west immediately above the Opimika Na \vs. This creek, as well as the lakes which it empties, are ' narkable for their clear water. Emerald Lake itself is corn- pa: lively insignificant in size, being only about half a mile in length, by a quarter of a mile in greatest width at the .southern end, gradu- ally tapering towards its lUtlet at the north- rn exti'emity. The lake is in a small valley from eighty to one hundred feet in depth. At the Slipll mnrl on Kiiii^ralel L;.k-. ■ii ■ill. ■).; i 1 I \ . I lira n 156 I NIPlSSlXil AND TEMISCAMING IIEGI05. m Analysis. south-east corner is a very shallow bay, affording entrance to a stream which is fed by a number of large cold springs that rise at the base of an amphitheatre-like gully, at the base of steep banks composed mainly of sand and gravel. The water of the bay, although so shallow, is very cold even during the hottest days of summer, while the whole bottom is covered witii a deposit of shell marl of unknown depth. That tins depth is considerable there is no reason to doubt, as the soundings made with long poles failed to reach the bottom of the deposit. Besides this bay the whole lake contains marl deposited o.i the bottom, while the pobljies and boulders near the outlet show a coiisidorabie coating of this loosely coherent, earthy carbonate of lime. Tlie wa r of these springs is evidently calcareous, and is found to be slightly aperient. According to Mr. J. F. Whiteaves, who has examined the speci- mens of fresh water shells obtained from this locality, the species represented are Sphceriwin snhatum (Lam.), and Planorhis trivolvis (vSay) var. m.acrosto)nus (Wliiteaves). A sample of the marl examined in the laboratory of the Survey was found to liave the following composition* :- - Hygroscopic viiter (iifter drying at 100' C). . I'Od per cut. Lime tS ' 82 h Magiu'sia 04 n Aluiiiinr, 07 « y<'rric' oxide O'OS n Manir iHous oxide Traces I'otassa Traces Soda Traces Carbonic acid liSOl h Suli)Iun'ic acid 07 m riiuspiit.ric acid 002 „ Silica, soluble 0" 10 n Insoluble niiii(#al matter 8' 02 n Organic matter, viz. ; vegetable fibre in a state of decay, and products of its decay, such as hunuis, liuuiic acid, etc., and ix)ssil)ly a little combined water 4 ' 70 n Total 10012 I. " Assuming the whole of the lime to be present in the f,.irm of carbon- ate, trilling quantities of which are, however, present in other forms of com')ination, the amount found would correspond to 8G • 28 per cent of carbonate of lime. The insoluble mineral matter was found to con- sist of " :— •Annual Report, Ueol. Sur\. Can., vol. VII. (N.S.), 18',I4. p. 81 it. BARLOW. ECONOMIC GEOLOGY. 157 I \ ' 'i\ .Silica fi • 24 per cent. Aluiiiuia and ferric oxide lal it Lime OS!) M: ■rnesiii 008 Alkalies (•;) 050 Total S(;-2 Marl is often used as a fertilizer, and deposits such .is that exposed at Emerald Lake should be of value locally for this purpo.se. Grindstones and Whetstones. Some of the matei'ial contained in portions of the beds of coarse Grim; itones. sandstone and grit, found near the base of several of the Palu'ozoic out- liers, would probably be suitable for the purpose of making grindstones. A quarry was opened many years ago on one of these arenaceous beds exposed above Deux Kivieres which furnished some excellent grindstones. Where the layers are not thick enough for this purpose, they would fuinish whetstones of very fair (juality. Where too hard and compact, these stones answer only for a short time, when first used, soon becoming too nmch polished. Portions of the very fine-grained, banded slates and greywackes so frequently met with throughout the northern and north-eastern part of the district may probably allbrd material suitable for hones and whetstones. Clay for Bricks and Earthenware. Cliiy suitable for the manufacture of bricks, extends over a very Clay, large area in the northern part of Lake Temiscaming, from the vicinity of the combined mouths of the !Montre.al and ]\Iatabitchouan rivers, northwards far beyond the conlines of the present map. The bricks for the large convent and church built V)v the missionaries of the Oblat order at Bale des Peres were made there. In the vicinity of North Bay, and extending thence some distanrie bej'ond Verne, brick clay is readily accessible, although sometimes concealed by the presence at the surface of varying thickness of yellow sand. A brickyard was in successful operation at North Bay for some years, and if the local demand were sufficient it would no doubt be re-opened. Some of these beds of clay might also furnish material applicable for the manufacture of coarse earthenware, but so far no clays fit for the finer kinds of pottery have been found in this region. Mica. Both biotite and muscovite are among the con)monest constituents Mica, of the various Laurentian gneissic rocks, but although thus widely dis- I : 'r I I i! 158 I NIPIS8INO AND TEMISOAMIXO REGION. tributed their presence in this association is not of economic import- ance. The numerous and often large pegmatite d^'kes tliat cut these Laurentian rocks give promise, in places, of affording a supply of mica in sheets sufliciently large and in such quantities as to be available for economic purposes. The southern portion of the Township of Calvin is peihaps the most important of these localities, but so fai- the musco- vite obtained, represenling the material exposed at or near the surface, has been too inferior in quality to command a price commensurate ■with the cost of mining. The opening up, however, of a large portion of the south-eastern portion of the area of the Lake Nipissing sheet for settlement, may bring to light other masses of {)egmatite producing good mica. AsJ>ei-(ufi. Asbestus. This mineral has been found in the district. One of these localities is situated near the west shore of the " Mattawjipika" on Lady Evelyn Lake, on the Haycock mining location. It is also known to occur to the north-east of Baie des Peres, but the deposits thus far discovered are not very extensive. G'i-aphite. Graphite. This mineral, .so abundant in the Laurentian area further to the south-east, is of rather rare occurrence in the region under descriptions and although doubtless present as an occasional constituent of some of the gneissic rocks, its {)reseuce was only noticed at one locality, where it occurs disseminated in minute grains and scales throughout the biotite cyaiiite-gneiss exposed near the shores of the Ottawa in the vicinity of Les Erables llapids and Snake Creek. Its presence in a rock-niMSS has oft-n been referred to as evidence of its sedimentary origin, but in this instance there seems to be no doubt whatever that the rock containing it ia a rather unusual phase of the biotite- gneiss, and as such is to be considered as a foliated plu tonic mass. 4 Apatite. Apatite. This mineral, though abundant as an accessory or accidental con- stituent of many of the crystalline rocks occurring in this region, has not yet been found in deposits possessing any commercial value. The only locality where it was noticed in such quantity as to be recognizable without the aid of the microscope, is on the property of Mr. Emery llacicot, on lot 4, con. VI., of the township of Ferris, a short distance from Nosbonsing, a tlag station on the Canadian Pacific Rail- BARLOW •J ECONOMIC GEOLOGY, 159 way. A pegmatite dyke is here exposed, composed chiefly of very pure and coarsely cleavnble llesh-red orLhoclase, with which is associated a much smaller ([uantity of black biotite often in large cleavable frag- ments. The dyke is about six feet in width, has a direction a little west of north, according with the foliation of tlie garnctifcrous horn- blende-gneiss with which it is associated. The apatite occur.5 very sparingly, generally in small well developed prismatic crystals imbed- ded chiefly in the biotite. Some of the crystals noticed presented the following comVjination of faces : oc P. P. OP. oo P2. Most of the crystals were too fragile, on account of their long exposure, to admit of their being liberated without breaking from the material in which they were inclosed. The felspar in this and other dykes in the near vicinity is very pure, and large pieces, many pounds in weight, could be readily secured without any admixture of foreign matter. Fl'uorite. Fluorite or fluor-spar is found in large cleavable masses, associated Fhiorite. with orthoclase, niicroclino and perthite in the large pegmatite dykes that cut the biotite-gneisses in the township of Cameron, about four miles and a half east, of Mattawa. The fluorite is of a light-greenish colour, but like the felspathic constituents of these dykes, is very much stained and infiltrated with ferric hydrate, which fills the numerous cracks and fissures present in the mineral. Molybdenite. The presence of this mineral, as an occasional constituent of quartz Molybdenite, veins, has been noticed in the district immediately surrounding Lake Nipissing. It is stated to occur in considerable quantity to the north of Talon Creek, on the Mattawa River, although its presence there was not verified during the progress of the examination of the region. Steatite, This mineral, usually a decomposition product of basic pyroxenic or Steatite. hornblendic rocks, is not very commonly met with, but specimens were obtained of tolerably pure material from the west shore of Luke Tem- iscaming, about four miles south of the Montreal River. Amazon-stone and Perthite. These two minerals are intimately associated with one another, con- Oiiiaumntal stituting much of the felspathic constituents of some pegmatites which stones. i I 160 I NIPISSING AND TEMISCAMING REGION. Openings made. cut a readily disintegrating biotite-gneiss, that outcrops on lot 7, con. B, of the township of Cameron, about four miles and a half east of Mattawa. Four openings have been made, of the nature of small pits or shallow trenches, extending only a few feet below the surface. The largest dyke is about five feet in greatest width, running north- east and south-west. The railway line is about 200 yards to the north, while the Ottawa River passes about 500 yards to the south of the exposure. The openings were made for apatite, and work on the pro- perty was abandoned when this material was not found. The aniazon- stone, when fresh, is of a very beautiful deep bluish-green colour, but owing to its proximity to the surface much of the material is more or less stained, and the minute crevices are filled with ochre. This defect would doubtless soon disappear in depth. Some of the material secured at the insignificant depth reached by the present workings is remarkably good, and is suitable for cutting and polishing. The perthite which is intimately associated with the amazonstone at this localit)', is a pale flesh-red aventurine felspar, shown to consist of a fine interlamiaation or parallel intergrowth of albite and orthoclase. The alternation of the darker-coloured flesh-red orthoclase with the paler albite, and the accompanying brilliant aventurine reflections pro- duces a beautiful stune when cut and polished. Cyanite. The occurrence of this mineral in situ in Canada was first noticed by the writer in 1890, in a cutting on the main line of the Canadian Pacific Railway, about half a mile east of Wahnapita; station. Here Cyanito. it occurs in flattened blade-like crystals and fragments, in association with a reddish alniiindine garnet in a mica-diorite-gneiss. The crystals usually conform to the foliation, but sometimes they occur in groups and clusters disposed at varying angles to the schistosity. In the more basic portions of the gneiss, the crystals are darker in colour, and have undergone in places ratlier extensive cracking and deforma- tion as a result of pressure. In the more acid or pegmatitic portions of the rock, the cyanite is much lighter in colour and occurs in stouter prisms. Fibrolite (siilimanite) also occurs in this locality, developed chiefly along certain crevices in the gneiss. It is fibrous or finely columnar in structure, and is traversed at right angles to the fibres by numerous fine cracks. Sometimes it occurs in curious irregularly radiating or plumose aggregates. The colour when fresh is of a pale bluish-gray. ECONOMIC GEOLOGY. 161 I During the examination of the Ottawa River above Mattawa, cyanite was again noticed as a constituent of the biotite-gneiss exposed in the cuttings on the Temiscaming branch of the Canadian Pacific Railway in the vicinity of Les Erables Rapids and Snake Creek. Here also it occurs in long, thin-bladed crystals in association with red garnet, and is in many places so abundant a constituent of the gneiss as to characterize this rock. The crystals are usually light- bluish or greenish, but some show a beautiful deep azure-blue centre with white margins. Fossil Corals. The particularly fine fossil corals of the Niagara outlier exposed on Fossil corals, the shores and islands of the northern portion of Lake Temiscaming, which have undergone in most cases complete silicification, would doubtless not only command a ready, though somewhat limited sale as specimens, but when polished would form an attractive ornamental stone for certain purposes. The west side of Mann Island exhibits abundant specimens of this kind. Springs. The region, as a whole, is not characterized by abundant springs, Springs, although occasionally some large ones are encountered. Opimika Creek, reaching Lake Temiscaming from the west immediately north of the narrows of the same name, is chiefly fed by springs, as is also Latour Creek, which enters the same lake on the west side about four miles above the Old Fort Narrows. Both these streams are remark- able for the coldness and clearness of their waters, and for the fine specimens of brook trout to be found in them. A fine large spring rushes down the hill immediately behind Thompson Bay, below the Opimika Narrows, on the east side of Lake Temiscaming, about half a mile east of the old Hudson's Bay Co.'s post. Another spring of good water flows down at the head of Les Erables Rapids on the Ottawa. As the country becomes settled many new springs will be found, but the abundance of good water contained in the many lakes and streams of the region, renders the presence of springs much less important, although as a rule the water in these lakes is rather warm for drinking purposes during the summer months. During a consider- able portion of the summer, the presence of a large number of minute greenish or yellowish particles, often so abundant as to form a scum at the surface or around the margins of the lakes, renders the water of many of them more or less unfit for drinking purposes. The waters 11 ' ,ii ' .! ': i}i.: 1(J2 I NIPISSING AND TKMISCAMINO REGION. of the springs that feed Emerald Lake, at the head of one of the branches of Opimika Creek, have ah-eady been referred to. They are the only ones known to possess therapeutic qualities. Lfiiptli cif river included. Its course .ind lakes uii it. RE(aONAL DESCRIPTION. The Ottawa River and Lake Temiscaming. General Features. As may bo seen by a reference to the accompanying map-sheets, a considerable length of the Ottawa is included by them. From the north-east bay of Lac des Quinze, where it enters the Lake Temisca- ming sheet, to the mouth of the jNIattawa (which for convenience has been included in the southern sheet) the distance is about 142 miles. Three large Jakes occur in this distance, which may be regarded simply as expansions of the stream. The most northern of these expansions, known as Lac des Quinze, is very irregular in outline, with several long arms or Ijays running in various directions, but the most direct line of comTuunication through the lake measures about twenty-two miles. This lake is separated from Lake Temiscaming by a short stretch of water known locally as the " Quinze River," noted for its wild and dangerous rapids, and which in its eighteen miles of length falls a distance of two hundred and sixtj' feet. Lake Temiscaming, into which this stream empties, is sixty-seven miles long from the mouth of the Quinze to the head of the Long Sault Rapids, while Seven-league Lake, which commences at the foot of these rapids, adds a further length of seventeen miles. While it would thus appear that the river, strictly speaking, embraces only about thirty-eight miles of this whole distance, it may be stated that a considerable proportion of that generally included as lake should in reality be considered as portions of the river proper. A large part of these water-stretches exceeds but very little, if at all, the average width assumed by the river when not obstructed by rapids, while at several points a swift current is present, denoting a small though appreciable change of level. Thus Seven-league Lake, in its lower portion, is only about a lake stretches, quarter of a mile wide, while in the upper part it never exceeds half a mile. In this lake a light current can usually be detected, showing a total fall in the whole length of about a foot during the ordinary low water of summer ; but during times of freshet this current is aug- mented, and the total fall is increased to a little over two feet. River-like ■] Tin: OTTAWA A\D LAKK TRMISOAMIXr,. 163 I Lake Tomiscaming itself, as noted in the appendix, shows a differ- ence in level of ii ioot from the head of the Long Sault llapids to tlie wide portion above tlie Old Fort Narrows, while the lower portion of the lake south of the mouth of the Montreal River, is quite river-like. This diiference in level is maintained by three \evy pronounced con- tractions. The most northerly of these is at the Old Fort Xari-ows, where the lake is pinched in between two bold hills of gravel, leaving a channel a little less than 800 feet wide at oi'dinary stages of the water. At the Opiinika Narrows, about thirty-tive miles further, a .still more pronounced current Hows through a strait which at one place is less than 200 yards in width. This current, formerly kno'vn tc the old voyageursas "La (^abre " shows a descent of fully half a foot. At Presquile, about a mile north of the head of the Long 8ault, the third contraction occurs, and here again a consider- able current may be noticed, but not so strong as at the Opimika. The Ottawa, from the north-east bay of Lake des Quinze, has a general ( Joneral direc direction a few degrees south of west as far as the head of Lake Temis- '"" " "^''-''' earning. At this point, however, it suddenly changes, and from the head of this lake, as- far as the luouth of the INIattawa River, the sti'eam flows about S. 30° E. In places there is a decided divergence from this general course, caused by local bends, which are especially char- acteristic of the upper portion of the ri^■er, but from Lake Temiscaming to the jNIattawa, the river follows an unusually uniform and deep valley, and any bends which do occur are in the nature of large curves. The upper part of the river, above Lake Temiscaming, occupies a ch.aracter of very pronounced valley, and the hills around Lac des Quinze present ^""■H'^y' the usual rounded or dome-like outlines so distinctive of areas under- lain by the Archa\an gneissic rocks. Except on the northern portion of the lake, where they are unusually bold, ranging from 200 to 300 feet in height, the hills are as a rule low, averaging less than 100 feet. The Quinze River, which usually breaks across the strike of the inclosing rocks, occupies an original, but not very pronounced depi'ession. When Temiscaming is reached these conditions undergo a decided change ; and the valley, especially in the lower portion, is fiord-like in aspect. From the Mountain Rapid to the mouth of the Mattawa, the river brejiks across irregular ranges of hills, which rise very abruptly from the water to heights of from 400 to 600 feet, while the shores on either side of Seven League Lake, which are as a rule bold and rocky, preserve a rather constant elevation of from 200 to 300 feet. In the construction of the Lake Temiscaming branch of the Canadian Pacific Railway along the rocky Hi I'r 15 ! i illhi ,1 , :hi. 1 m > ,i ' 164 I NIPISSING AND TEMISCAMING REOIOX. Illlf Montreal Kivcr to Lons Sault. - West shore. eastern bank, this was so steep and abrupt that it was found necessary in most instances to make large rock-cuts, the road skirting the shore. From the mouth of the Montreal River to the Long Sault Rapids, the banks on both sides of Lake Temiscaniing are extremely bold, and, as a rule, rocky, and frequently for several miles present unbroken cliflfs. The hills on both the Ontario and Quel)ec sides of the lake rise very steeoply from 3-")0 to GOO feet, with but few minor and unimport- ant breaks where some of the larger streams flow in. Throughout the whole of the distance from Mattawa, the tributary streams all show a very abrupt descent tf) this valley. Above the mouth of the ^Montreal, the topographical outline changes somewhat suddenly, and the shore, though still in many places steep and abrupt, is not continuously so ; while wide and open valleys covered with drift separate the still high hills. The west shore of the lake is especially steep and regular, and until Haileybury is reached no ilat of any appreciable extent occurs. Near the north-west corner of the lake, large and comparatively level tracts exist that extend far beyond the boundaries of the accompany- ing map, and are fast being opened up for settlement. East shore. The eastern, or Quebec shore, presents many deep and important indentations and although numerous high and exceedingly rugged hills occur, they are for the most part separated from one another by flats of clay. These have in many instances been cleared and are at present occupied by prosperous farmers, the soil being good and yield- ing abundant crops. Head of Lake The depression occupied by Lake Temiscaming extends in a north- 8 aming. ^gg^gpjy direction, but becomes divided into two subsidiary valleys by the flat limestone promontory terminating in Dawson or Waljis Points. These valleys are occupied by the two important tributaries known as Wabis Creek and the Blanche or White River. Soundinps by T. thierin. It has always been known that the Ottawa River is, in many portions of its course, very deep, but no accurate information regarding its depth was published until Mr. Thos. Guerin, C. E., examined that part of the river above Mattawa.* Those soundings were, however, few in number and confined chiefly to Seven League Lake, although a few were obtained in the vicinity of Chiefs Island on Lake Temisca- ming. Mr. Guerin states that Seven League Lake was sounded in several places, the depth obtained being generally about sixty feet. In one place it was 397 feet, but in no place was it found to be less than thirty feet deep. The sounding-line on Lake Temiscaming was unfor- *Annual Reiiort, Minister of Public Works, 1884-85, pp. 106-107. ■MLOW. J tunatelj Chiefs Durii nights V were coi was foui liere stei bouldeis greatest Fou. showing bottom. About m channel shore is ( considera of which the culm From < soundings feet and 1 211 feet 200 yards again appi centre was it shallows shallow po which Mel All of tl gravel or s rapidly anc Keepawa 1 noted was mid-stream tained clos( of the west from the e« lake is 423 Rock it is 4 little over s lake, the de A!;iAi.- ■] THE OTTAWA AM) LAKK TEMISCAMING. 1G5 I tunately only 120 feet long, and on continuing the soundings south of Chiefs Island it soon failed to reach the bottom. During the progress of the (Jeological Sui-vey several calm moonlight Soundinprs hy nights were spent in sounding Lake Icmiscaming. iliese soumungs Smvty. were commenced at the Opimika Narrows, where the deepest water was found to occur in close proximity to the westei'n shore which is here steep and rocky. The bottom is composed of coarse gravel and boulders, and the lead showed a narrow and tortuous channel whose greatest depth was forty-five feet • Four more soundings were taken in going north, in the next mile, Opimika showing a gradual deepening with a gravelly and ultimately a sandy M'L•^lal■till bottom. These soundings were respectively 55, 47, 75 and 111 feet. l'"'i't. About midway between Main Channel Islet and the west shore, the channel is 65 feet deep, while that between this island and the eastern shore is only 55 feet. It is evident that there exists at this point a consideral'e bar, due to the deposition of inorainic or drift material, of which Main Channel Islet (wholly composed of boulders) forms the culminating point. From this place to within half a mile of McMartin Point, three soundings were taken, showing an increase first to 95 feet, then 139 feet and 183 feet, while three soundings taken at this point showed 211 feet in mid-channel, and 198 and 127 feet, the latter being within 200 yards of the western shore. Opposite McMartin Point, the lake again appears to shallow somewhat, and the deepest sounding near the centre was 157 ^'f-et, while half way between this and the western shore it shallows still further to 130 feet. Again it would seem that this shallow portion is caused by an accumulation of morainic debris, of which McMartin Point forms the shoreward extension. All of the above soundings showed a bottom composed of very fine ^McMartin gravel or sand. To the north of McMartin Point, the lake deepens J*"'"t to , , . , Keopawa. rapidly and maintains a very uniform depth as far as the mouth of the Keepawa River. About a mile north of McMartin Point, the depth noted was 425 feet, while still further north, opposite Latours mills, in mid-stream, the depth found was 460 feet. This great depth was main- tained close to either shore, for a sounding taken within ten chains of the western shore showed 455 feet while one taken an equal distance from the eastern shore was 320 feet. About a mile further north, the lake is 423 feet deep and again in mid-channel opposite the Buffalo Rock it is 430 feet deep. The deepest sounding made was taken a little over a mile south of the Keepawa River, about the middle of the lake, the depth being 470 feet. Going northward, the lake shallows, r-{ ■■ 16G I NIPISSING AND TKMISCAMINfi KKGION. Ko('pawa to Montroal Uivor. J Montreal River to Old Fort Narrows. Morainio deposits at Narrows. and oj)posite the mouth of the Keepawa is only 362 feet deep. Through- out this interval of great depth, from IMcMartin Point northward, the whole bottom was found to be covered by a soft, unctuous, gray clay or ooze into which the lead sank a foot or more. The depth ascertained at the mouth of tlie Keepawa remains uni- form to within a mile of the combined mouths of the Montreal and INIatabitchouan rivers, where it is 317 feet. Northward, the lake gradually shallows, and opposite the mouths of these streams has been partly filled up by an extensive deposit of sand and gravel that forms the bottom in this neighbourhood. These streams cannot, however, account for the vast accumulation of loose material which is here evidently jiresent, for the lake is over a mile wide, and for more than a mile in length has been filled up by a deposit varying from 100 to 150 feet in depth. Further, the lake shallows considerably to the north of these streams, while the reverse would have been the case if the whole of the material had been brought down by them. This extensive bar has probably been deposited in the first place as a lateral moraine, in the shelter of the bay in the rocky hills that occur at the mouths of these rivers, while the material subsequently transported and laid down by the streams, has reformed and modified these depo- sits, producing the somewhat wide delta now found. Opposite the mouth of the Montreal Ptiver, the depth of the lake in the middle is 275 feet, while about three-quarters of a mile further north this again decreased to 2.")6 feet. Still further north, the lake deepens rapidly, and two miles north of the ^Montreal River the sound- ings showed a somewhat uniform depth of 400 feet. A little over half a mile south-east of Roche McLean, the lake is 378 feet deep, while opposite the north end of Quinn Point it is 370 feet. Here again a bar composed of boulders and clay with a little sand extends from the north-east end of this point for nearly a quarter of a mile, with only about five feet of water at ordinary summer level. In the centre of the large open space to the north of Quinn Point, the lake is 348 feet deep, while in the middle of the Narrows, opposite Pointe a la Barbe, it is only 170 feet deep. In the open space opposite the mouth of the Little River it is !'< 5 feet deep, thus showing a rather uniform depth in this portion. The Old Fort Narrows is a very decided contraction occasioned by two bold hills of sand, gravel and boulders. The deposition of the material at this point was evidently determined by a pre-existing rocky narrows, the higher portions of which may be seen protruding from the surrounding mantle of sand and gravel. During the retirement of the •] THE OTTAWA AXD I.AKK TEMISCAMINfJ. ir,7 I ice-shect up the valley of the luko, a large amount of moniinic material was deposited at this place, thus still further reducing the channel. In the oliannol, immediately opposite the Hudson's l>ay Co.'s old store, the first sounding showed a depth of 31 feet, which was gradually in- creased to about sevonty-ti\ e yards from the west shore ; while less than thirtj' yards from the west shore tlie depth was found to he 46 feet. To the north, the lake gradually deepens, first to 88 feet about an eighth of a mile north of the Narrows, and finally to 120 t'eot about half a mile north. In the opposite direction, or southwards, on the other hand, the lake deepened first to C.J and then to 1.30 feet within less than an eighth of a mile. There seems, therefore, to be no warrant for the supposition that this barrier of sand, gravel and boulders p-:tended at one time com- pletely across the lake, for, if such had been the case, it appears probable that the removal of this material would have resulted in the accumula- tion of a considerable deposit immediately south of the Narrows, which is not found, as the descent on the south side is nmcli steeper, in fact nearly as steep as the angle of repose, under the conditions, for gravel and sand. Our soundings did not extend further to the north, and 'ilthough x^ gomjjii„„g the western shore-line is still very steep and abrupt, it is not probablt; '" "ortliorn that tlie great depth characteristic of those areas to the south of the Narrows is maintained in this direction, although occasional localities with considerable depth may doubtless be found, presumably in the neii'hbourhood of the western shore. The highest water in this part of the Ottawa is in general occasioned Times of by the melting of the snow in spring, and occurs usually about the "^S^' ^"'' '"^''' latter part of May, while the time of low-water is during kSeptember or October, according to the setting in of the autumn rains. During the summer months, the Ottawa is remarkably and quickly affected by very heavy or long continued rainfalls. In ordinary seasons this ditierence in level varies from twelve to fourteen feet, but in 1887, and again in 1894, Lake Temiscaming and this portion of the Ottawa showed the astonishing difference of twenty-one feet between the two extremes of high- and low-water. Both of these years were, moreover, remarkable for an extremely heavy snowfall during the preceding winter, thus furnishing conditions for an extraordinary spring freshet, while the succeeding summers were notable for excessive and long continued drought, and the lowest water occurred during the month of September. i - i iiiji' !ii ^^[.-■i iii'i 168 I NIPI.SSINO AND TEMISCAMINO lUXlION. Differnncp in full I if lion^' Hivult KapulH One of the most marked oll'ects occasioned by this difference in Inv el, is the corresponding difl'erence in the fall of the Lont,' Hault llapids that separate Lake Teniiscaminj,' from Seven League Lake, and the accompanying increase in the fall of the rapid at \\w outlet of the latter, known as " The Mountain.' During times of low-water the fall in the Long Sault Rapids is almost lifty-livo feet, wliilc at high- water it is only forty-nine feet. On the other hand, during tinvs of freshet, the Mountain Rapid has a fall of seven feet, while at low- water there is only a fall of a little over three feet. During the same time Seven League Lake has a total fall of two and a-half feet in times of high-water, and at low-water there is only a fall of half a foot from the noith to the south end. These seeming anomalies are thus Exiilanatic'ii explained by Mr. Thomas Guerin :* — •" The Long Sault * * * is y. 1. nim . jj^j^ig,] jj^ j^g head by an island into two channels, tlie level of the bottom of the eastern channel being about seven feet below that of the bottom of the western channel which becomes dry at low-water. * * * The outlet from Seven League Lake is at the ^Mountain Rapid, and the capacity of the channel here is less than the united capacities of the two channels, which constitute the outlet from Lake Temiscaming. Hence the latter channels during high-water pour a greater (juantity into Seven League Lake than the outlet of the latter is able to dischai'ge, thus causing Seven League Lake to rise, while Lake Temiscaming falls so that the difference of level nmst be least at high-water. Again when the level of Lake Temiscaming falls so low as to render the western channel dry then the outlet from Lake Tem- iscaming will be confined to the eastern channel, which is nearly of the same dimensions as the outlet of Seven League Lake, but as the area of the latter lake is many times less than that of Lake Temiscaming, its level must fall faster and the difference of level must be greater at low-water than at any other time." Discharge. Trend of Ottawa Valley. The rate of discharge from Seven League Lake was measured by Mr. Guerin at the current immediately above the Mountain Rapid, on . the 21st of August, 1884, and found to be 16,383 cubic feet per sec- ond. From a comparison of the levels then prevailing, it was calcu- lated that the rate of discharge during times of high-water would be 25,100 cubic feet per second, and during low water 14,800 cubic feet per second. The trend of the Ottawa Valley, from its confluence with the Mattawa to the foot of Lake Temiscaming, is nearly north-west, mak- ing a considerable angle with the direction of the foliation of the * Annual Report, Minister of Public Works, 1884-85, pp. 107-108. •ANLOW 1 THE OTTAWA AND LAKK I KMlSCAMINfi. 1G9 I gneissic rocks ulong its hfinks. At the mouth of tho Miittawa a .sharp elbow is formed, the valley below that river turuiiij,' nearly cast, in close correspondenoo with the foliation of the gneisses and coinciding in direction with tho depression occupied by the ]\[attav\a Hiver. The sharpness of this elbow is further accentuated l>y the fact that, for several miles above this point, tho course of the Ottawa River is nearly north-and-south. The river from IMattawa to the foot of Lake Teniiscaming is inter- ijaimls, riipted at intervals by hea\y rapids, three of which occur f)n the lirst i,,|i<,.''|','.t„i8. fourteen miles, while the Long Sault, seventeen miles further up, is «-!'ii""g. six miles in length. The first rapid, four miles above the Mattawa, is now known as La j,,, Cave. Cave. It is about half a mile in length, and is divided into two leaps, the lower of which was formerly known as La Cave, while the upper portion was called the Demicharge Chaudron, or Chaudicre. The The combined fall is nearly ten feet, divided into two nearly equal parts. The river between the Mattawa and La Cave llapitls a\erages about a quarter of a mile in width, although in one or two places where bays are present, this width is nearly doubled. Antoine Creek is the main tributary in this interval, coming in from the west and draining in its course the larger portions of the townships of Mattawa and Olrig, its source being in some small lakes situated in the south-western part of the township of Erench. From La Cave to the next rapid, known as Les Erables, is a little Les Erables. over three and a half miles, while the width averages about a third of a mile, aud occasionally somewhat less. Les Erables Rapids are a little over half a mile in length, with a descent of nearly thirteen feet. Latour Island, at the foot of this rapid, and almost in the middle of the current, shows a large number of pot-holes worn out in the rock. All stages in the process may be seen from the incipient canals, where the eddies have commenced to wear down along the jointing planes that cut the rock, to holes ten feet in diameter. In a few instances several holes are seen to liave been so greatly hollowed out that they ultimately joined at or below the surface. Cotton Creek enters from the east a short distance below the foot of Les Erables Rapids, forming a beautiful cascade as the water tumbles over the rough ridges of gneiss which impedes its progress. This stream drains a number of lakes, of which Lake Memewin, situated about four miles to the east of the river, is the largest, being four miles long, and very irregular in outline. Scarcely three miles and a half intervenes between Les Erables and The Mountain, where the , I ! 170 I NIPISSING AND TEMISCAMIN(i REGION. Tlic Arouiitain wliole volume of the river flows throuah n narrow ch.annel, obstructed by rocky reefs and islets. About a mile above Les Erables Rapids anotlier stream enters from the east, with a steep descent into the Snakf Crook, valley of the Ottawa. This stream, now known as Snake Creek, drains a nuinV)er of small lakes, the largest of which is Snake Lake, while the head waters are in a small lake, from M'hich only a short portage is necessary to reach Obasking Lake. It thus formed a portion of the old winter route, which left the Ottawa River at the mouth of this creek and reached Lake Temiscaming a short distance below the Opimika Narrows. About a mile below the Mountain Rapid one of tlie highest hills was ascended and found by aneroid barometer to be 520 feet above the surface of the water. The average height of the hills on either sitle would, therefore, be little less than 500 feet. Seven Loa{,'uo Lake. Streams entering East Crook. Jocko River. Its southern branch. Seven League Take, is a stretch of navigable water nearly seventeen miles in length, extending from the head of the ^lountain to the foot of the Long Sault Rapids. The banks in most jjlaces are steep and rocky, and one or two places, perhaps, deserve special mention. Devils Garden Bluff, on the east sid presents a sheer precipice of gneissic rocks, and receives its name from the fact that a patch of wild onion grows near its summit. Above this, on the west .side and only a short distance below the foot of the Long Sault Rapids, there is a sharply accented hill thickly overgrown with small pine trees, which, from its niaiked resemblance to the characteristic headgear of the Canadian "habitant," has always received the designation of "La Tuque." This is a rather important and well known land-mark. Three important tril)utaries enter Seven League Lake. The first of these, known as East Creek, has its source near the eastern limit of the southern map-sheet, and is thus not more than seven miles long, reaching about six and a half miles below the foot of the Long Sault. The next stream, however, which enters on the west side about half a mile further north, is much larger, and named Jocko River, after a half-breed of that name. Formerly the stream was known as the Siconaguisipi or Blackstone River, a name appearing in Sir William Logan's report on the region, although on his manuscript map it is designated as the Porcupine River. The main branch of this stream heads in a lake about two and a half miles long, bearing the same name, and situated about the centre of the township of Osborne, a little over twenty p^iles in a straight line from the outlet. Its northern blanches drain the northern parts of Osborne and Garrow townships, and also a considerable area of unsurveyed land between these townships and Nevins base-line. The southern branches drain almost the whole of ■1 THK OTTAWA AND LAKK I'UMISCAMINC!. 171 I the townships of Stewart anaring N. 2G' W., with an area of about 125 S(]uare miles. From the head of the Long Sault to the Narrows the lake is about a quarter of a mile wide, but at the foot of the Narrows it increases in width to about a mile, on account of Thompson Bay, situated on the east side. Both shores are steep and high, and in several places there are almost perpendicular clifls over 200 feet in height. On the Ontario side especially, the hills are covered with a good growth of pine, almost to the water's edge, which eftectually conceals the rock l)eneath. A portion of the Quebec side, between the Narrows and Schooner Island, has, however, been almest denuded by fire of its ori^anal forest growth, and exposes the rough and broken ridges of gneiss, SchoDner or Ship Island evidently represents the apex of a bouldery shoal, as no evidence of a rock in situ could be found. Presquile, about a mile above the head of the Long Sault, has been designated as an island, and although com- paratively deep bays approach close to one another on the north and south sides, a small neck of land unites the so-called island with the eastern shore. It evidently I'epresents an older accumulation of morainic material which in so many places block the channel of the river. The Opimika Narrows, are about two miles in length, and very crooked and contracted towards the northern end. High rocky hills form the immediate coast-line on tlie west side, but on the east side the shore is composed of sand, gravel and boulders, forming a flat over a quarter of a mile wide to the base of the rocky hills. The greatest conti-action is towards the north end, where the shore-lines are only a little over a hundred yards apart. Two creeks enter the Ottawa at the Opimika Narrows. The largest one, now known as White Creek, drains two or three small lakes between this point and Keepawa Lake, the largest of which, White Lake, is over half a mile in width, and two miles in length ; the eastern end approaching within about three miles of Keepawa Lake. The other creek is known as Green Creek, and enters from the west side, draining some small lakes in that direction. •] THE OTTAWA AND LAKK TEMI^CAMING. 173 I ii Above the Opimika Narrows the lake widens almost iiumediately, Narrows to and from this point as far north as tlie mouth of tlie Monti eal i^iv"i.'^'' River it has an a"erage width of from three-quarters of a mile to a mile. The shores are very bold, often exhibiting nearly vertical pre- cipices of rock for many miles at a stretch. Occasionaliy small portions of the shore-line are composed of sand and gravel, but high trees rise almost immediately behind. MciMartin and Ouellette points are small, low, projections running out a small distance into the lake and are composed wholly of sand and gravel except in the case of Mc- ^lartin Point, where some of the solid rock projects through this loose material. In the vicinity of Mc^lartin Point, a considerable amount of stiff grey clay was noticed, and a bank of this contains a large nura- ])ov of very irregularly shaped calcareous nodules, but no fossil remains were found in them. The hills on either side of the lake are from 300 to 500 feet above the surface of the water, and the highest, known as the King of the Bea\( rs, rises to a height of about GOO feet. These hills evidently form the edges of an undulating plateau which extends inland on both sides, and in which the valley of the lake has been excavated. P)uffalo Rock is another well known topographical feature, consisting of •; r ,\y precipice on the west shore of the lake, and so named from .., .iiass of vegetation upon it, which has a fancied resem- blance in outline to a buffalo. Six tributaries may be mentioned which (low into the Ottawa Trilintaries between the Opimika Narrows and the mouth of the Matabitchouan ''"[''",'? ,"" River. The first of these is Opimika Creek that enters a beautiful sandy bay on the west side, known as McLaren Bay, about half a mile Oi imil'iii north of the Narrows. The water of Opimika Creek is extremely clear and cold, abounding in speckled trout. Although its actual source is in a small lake about nine miles to the south-west of the Narrows, it derives most of its water from two lakes some four miles to the south- west, which are supplied by a series of large springs. One of these lakes is called Emerald Lake, and is remarkable for containing a deposit of shell marl which is described in that portion of the report treating of economic geology. The small pond at the head of the stream is 580 feet, by barometer, above Lake Temiscaming. About thi-ee miles further on, Ottertail Creek reaches the lake from Ottcituil the west. This stream forms a poi-tion of a route to the west. The main or southern branch takes its rise in a small lake, some twenty miles to the south-west in the township of J-lammell, within a mile of Spruce Lake, at the head of the Tomiko River. About a mile above McMartin Point, a small stream enters from the east, draining White Beaver Lake, i I .; I I ' 1 , ! '!H 174 I NIPISSING AND TlCMISCAMIXfl REGION. n Kc>('))awa Kiwr. SliniTs north of .Montreal Kiver. and three miles south of the mouth of the Keepawa lliver, another small stream enters whicli is notable as beitij,' the old Indian jiortage-route to Lake Keepawa. The next .stream is the Keepawa liiver, forming the outlet to a great number of large lakes, many of which are outside the boundaries of f'.ie present map. The largest of these lakes is of course Lake Keepawa, which is nearly thirty-two miles in a straight line from north to south and, with its intricate shore line of bays, covers an area of 120 square miles. The Keepawa River is nearly nine miles in length, with a total fall of about 300 feet, and has a number of powerful rapiils and chutes in its circuitous course. At the mouth is a very fine chute. The Matabitchouan and Montreal ri\'ers, which enter the lake at the same place, are elsewhere separately described. North of the [Montreal Kiver, Temiscaming Lake gradually widens. The western coast-line continues to be ratluM- even aiid unbroken and is also as a rule steep and rocky. At the Crows Nest liock, opposite; Bryson Island, as well as at Manitou Jlock opposite Mann or Burnt Island, there are sb.eer precipices, that extend for several miles vary- ing from ir)0 to 200 feet in height. Tii.e east side of the lake shows more irregularity in outline, and large areas of level land exist, from which, however, bold hills rise in places. There is much more culti vable land in the aggregate, than the often rocky character of the lake- shore would indicate. Islands. Below the Old Fort Narrows there are only a few small and insig- nificant islands. Roche McLean, so named after an old North-west Company fur-trader, as well as the island north of Pointe a la Barbe, are both connected at low-water with the western mainland by narrow bars of sand and gravel. Moose Rock is a huge boulder of breccia- conglomerate, about thirty feet in diameter, situated some four miles south of the Narrows. North of the Narrows, there are several islands, of which the mo.st important are Bryson or Moose Island, Burnt Chiefs Island. Island and Chiefs Island, the latter being a well known topographical feature. It is high and rocky, and at low-water is connected at its eastern end with the mainland by a bar composed of boulders and clay ; although, during the early part of the season, there is often sutlicient water to permit of the passage of the steamer. To the north- west of the island a similar bar exists, which, at low-water, prevents the steamer proceeding any further, although the channel inside is quite deep. The presence of this boulder barrier is probably due to its deposition, in part at least, in a crack or rift in the glacier, that evi- dently occupied the valley of the Blanche River towards the close of the glacial period. ■ARLOW THE OTTAWA AND LAKK TE.MISCAMIXG. 175 I Tlie northern part of the lake, from the Old Fort Narrows to the mouth of the River des Qiiinze, has more tlie appearance of a lake than any portion further south. The deepest water is to the west of Mann and Bryson ishmds, and is the route usually followed by the steamer. At ordinary summer level it is impossible for a steamer drawing six feet of water to pass between iJryson Island and the Quebec main- land, and the lake for a long distance outward, opposite ^\'ri^■ht's mine, is comparatively shallow. Kelly, or, as it is no'.v called, Priests ]^ay, where the chief settlement of the disti'ict is situated, pre- I'lMcsts Bay. sents a long stretch of gently sloping clay ilats, extending out from the shore opposite the village of Eaie des Peres, and, usually, towards tho end of August and in the month of September there is not more than five feet of water at the end of the long wharf, so that for a consider- able portion of the season the steamers ai'e compelled to anchor fully half a mile from shore, and lighter their passengers and cargo. The north shore of the lake is divided into two deep bays by the Noitlicrn high rocky promontory termiiaating at Dawson or Wabis Point. The high limestone tat lv.'-land of which this forms a part, is over two miles in width, presenting a very steep escarpment of light cream-coloured limestone facing eastward and running in a N. Is . W. dii-ection beyond the borders of the map. Wabis Bay is a little over two miles wide Waliis I'ay. and three miles in depth, receiving at its head the waters of Wabi Creek, at the mouth of which is situated the promisii>g settlement of Liskeard. Wal)Is Creek is a stream of considerable importance, rising beyond the north boundary of the map and draining a large area of arable land to the north-west, most of which has recently been laid out in townships and sulidivided into lots. The borders of Wabis Bay are in general low, with a marshy fi-inge along its north-west shore, while the water is extremely shallow and the shore difficult of approach except by means of the very crooked and narrow channel which the stream has hollowed out on the hard clay bottom. The north-eastern part of the lake is North -eastern divided into two bays known as Sutton and Paulson bays, separated ^^^' from one another by the low uuirshy delta marking the mouth of the Dlanche and Quinze rivers. The greater portion of Sutton Bay is a low sandy flat almost completely dry at low-water. When the lake is at its ordinarx' summer level, there is scarcely a foot Shallows near of water covering the extensive clay flats in the vicinity of Chiefs Island except in the various channels which the steamers entering in this vicinity have hollowed out. During low-water, occurring in Septem- l)er of 1887 nnd 1894. the greater part of these clay flats was exposed, the water being confined to these comparatively narrow channels. Three 'hi !' 1 • i: ' 17G I NIPISSINC. AND TEMISCAMING HKGION. BARLOW. ] Rivers Blanche Kivt'i'. Navigable part of ri\ The large tributaries enter the lake in this neighbourhood and a fourth, known as AVibika Creek, about eight miles in length drains the western portion of the township of Guigues. The largest of these streams is the one which really constitutes the upward extension of the (.)ttawa River, now known as the Rivitre des Quinze or (Juinze River, The other two, in the order of their importance, are the Blanche or White River and the Otter River, often also called Ottertail River especially on the maps issued by the Crown Lands Department of Qut;bec. Only about five miles of the lower portion of the Blanche River is shown on the Lake Temiscaming map-sheet, the source of the stream being in Round Lake, is situated about fiitti 'inmcli. River, drains the larger portion of the township of Duhamel, rising in a small marshy lake about the centre of the township. Tliis stream i,s rather crooked, even in its larger bends, while it meanders in a very tortuous manner through clay flats. 'r\ ill Geological jDescription. The village of Mattawa is built upon a bouldery terrace of raorainic Bouklerv origin, which, subsequent to its deposition, has been modified to a Muttuwli. considerable extent by the scouring action of water. This boulder, covered field or plateau has a somewhat uneven contour, but in general * Reiiort of Progre.ss, Geol. Surv. Can., 1S72-7S, p. 134. 12 ■'iii- /:U ' if ! I Character liMiiUlers. Terrace. Mattuwa Mountain. Peguiatitf dyke.s. 178 I nip:ssing axd tkmiscaming kegion. it may be .«aid to ri om thirty to severity feet above the river. It is only one of many similar occurrences to be found in the neighbour- hooil of the Ottawa River, all of which seem to owe their accumulation primarily to deposition from a melting detritus-laden glacier. This bouldery terrace begins nearly a mile up the Mattawa River and extends a little over half a mile down the southern bank of the Ottawa. In the angles formed by the junction of the two streams, it has its ma.ximum development, producing a bar consisting almost wholly of boulders and coarse graA^el, which stretches nearly across the river, leaving a deep though nari-ow channel near the Quebec shore. The boulders about jNIattawa vary in si/e from a few inches to as many feet in diameter, while man}' of them measure from ten to fifteen feet across. By far the larger number of these erratics consist of very evenly folioted gneiss, and have not been carried far from their original positions. iSome are f>f red and gray granite, while a few are of greenish gabbro or diabasa, Recent cuttings show that the bouldery layer overlies silts and other fine deposits. A well defined old river-channel occurs, running through the rear portion of the village between the main street and the railway station, which has evidently been followed by the jNIattawa or its antecedent stream. It leaves the Mattawa about a mile above the mouth, and reaches the Ottawa at the foot of the rapid, nearly three-quarters of a mile below. On the north side of the river, a steeply scarped though somewhat narrow terrace rises to a height of nearly eighty feet above the level of the river. Near the junction with the Ottawa this terrace is com- posed of well-rounded fragments or small boulders with coarse gravel and sand, this material being in a much finer state of division than that on the south .side. Oppo^:ite the village of Mattawa, on the north side of the Ottawa, is " Mattawa Mountain," about GOO feet high. It is composed of a grayish granite-gneiss, consisting of the usual alternation of lighter and darker bands, causing a distinctly marked foliation. The strike of this folia- tion corresponds closely with the trend of the hill, being nearly east- and-west, while the dip is about 20° to the south. In places it con- tains an abundance of rather smiill garnets, especially numerous in the darker or more basic portions of the rock. At many points this gneiss is cut by dykes of pegmatite, varying irregularly in breadth from a few inches to several feet. These pegmatites are compo.sed usually of a flesh-coloured orthoclase or microcline and (juartz. Occasionally a white i)lagioclase, probably oligoclase, was noticed in the same dyke with the orthoclase, while the v.] ness. .] Till'; OTTAMA AM) LAKK TP.MISCAMINT;. 179 I ferro-magnesian constituent is sparingly represented, if at all, and is usually l)iotite. The quartz is a;; a rule segregated in the centre of each dyke, leaving an almost pure felspathic margin of varying thick- ness. Many of these dykes cut the foliation at considerable angles, running from S. 40' W. to S. 55° W., while others, especially the smaller ones, conform very closely to the foliation. It is quite apparent, from the many conflicting local dips and strikes ( jneissos observed in the area to the south of tlie Ottawa River, and extending f<"'"i'"K ^i""-'! for a few miles east of Mattawa, that the gnoissic rocks rise into a series of small domes, each presenting quaquaversal dips ; while, on the other hand, the complete examination of this small area has also shown that the grander structural features of these rocks exhibit a rather constant dip at low angles, varying in direction from south to S. 10° W. These gneissic rocks are well foliated and of a dark-gray colour where the bisilicate material is present in relatively greater quantity, while a pre- vailing reddish tinge is usual where felspar present increases. Some bands exhibit the " augen " structure in great perfection. About a mile east of Mattawa, the main line of the Canadian Pacific Railway has cut through the axis of one of the most perfect of these dome-shaped bulges. The gneiss occurs in alternating light- and dark coloured bands which exhibit very sh «rp lines of demarcation one from the other. The main axis of this dome runs in a direction S. 80° E the dips on the north side of the railway track thus turning from N 80° W. all around to S. 80° E.; while on the south side of the track dips exactly the opposite of these may be noticed. The gneisses contain a large percentage of pyrite, and all the joints Character of and fissures arc plentifully coated with brown hydrous oxide of iron K"^'''*'- due to the decomposition of this mineral. The rocks crumble and fall to pieces when exposed to the action of the atmosphere for any length of time, giving rise to a coarse brownish sand that constitutes much of the soil of the region surrounding Matta'va. About a mile and a-quarter oast of Mattawa, the gneiss has a dark Suiierficial reddish-gray colour, the reddish tinge being due to the presence of felspar, which is in reality much more abundant in certain bands than in others. On the surface the gneiss presents a smooth hard crust, that is evidently merely the result of weathering, while beneath this thin coating the rock has undergone somewhat advanced decomposition, being yellowish in colour and comparatively soft and friable. This outer in- duration is very frecjuently chai'acteristic of the exposed surfaces of both gneisses and the Huronian sandstone and greywackes, and, as has been 'i i Hi ! ! I i 180 I Nll'ISSIXfi AN'I) TEMISCAMING UKOIOX. iiock s bitw ■I'll M It tiiwu iUK ( :i vili. Sti ike \VC.~t I tiiwa. Strike Rapids shown Ijy Trviiif,' and Van Hiso, is caused l)y the secondary onhirj,'e- meut of the i|uart/ and felspar individuals, the interstitial material constituting interlocking areas which arc optically continuous with tlie original grains. To the west of ^Nlattawa, the railway follows up the valley of a creek tiiat empties into twD small lakes, the larger of which is known as Eai'ls Lake. The shores of both these lakes are low and grassy, with only one rock exposure at the western end of Pearls Lake. Between Matiawa and Calvin stations the rock is usually well foliated granite-gneiss, althougli in one or two places it is very massive, and the foliaiion is uther absent or (|ui(e indistinct. Some of the bands dilTer in colour from dark-gray to almost black where the biotite is exceptiunally abundant ; others are light-gray, while still otiiers are i>f shades ot llesh-ied or pink wheni the felspar is plentiful and is of that colour. The component bands are fro([UPntly so irregular in their development and in jjlaces so contorted, while the region as a whoh; hcas undergone such uneven truncation, that it is often e.\ccedinL,ly dilticult to i>ronounce with any degree of certainty as to the direction of either the dip or the strike. In general, though, these rocks giadually bend round from S. 45' W. a littleVost of ^lattawa, to 8. 80 W. in the vicinity of Calvin, with a connnon dip at a higli angle to the south. One of the pegmatite dykes, noticed about two miles west of ^lattawa, is composed of a very large quantity of llesh- red felspar in coarse cleavable masses, some fjuartz and a considerable' amount of dark-coloured mica, in large crystals and plates, doubtless a partially bh-ached biotite. All of the rocks are well rounded and glaciated, and although the strife are not very phiiidy marked, some indistinct ones have a south-west direction, and ai'e thus referrablc to the period of general glaciation. In the angle formed Ijy the junction of the ]\lattawa and Ottawa rivers, and to the north and east of these streams, the foliation of the gneiss shows a curious fan-like arrangement, the convergent lines pointing towards the Ottawa, where the gneiss shows a rapid change in strike from nearly east-and-west at the southern end of the rock exposure to N. 2")° W. at the northern end. This structure is, how- ever, only a local feature, and is con lined to a small area. To the west, this fan-like fi^rmation broadens, he bands near the southern end curving round rather sharply to the south-west to meet those exposed on tie shores of Boom Lake and in the vicinity of the Plain Chant Rapids on the Mattawa, where the gneiss strikes from S. 30' W. to It Cue S. 60" W. with a south-easterly dip < 40° to 45°. To the north, as the Ottawa liiver is ascended, on the west shore the strike of the gneiss of llnrtll- f Mat- o y. t-4 4> o s fco >^ a -S H S ^ ^ 3 ? r*. J) y. H a 3 O i 'J3 O -yj ai" IMAGE EVALUATION TEST TARGET (MT-S) h // :/. U.A ^ 1.0 I.I IM u, 1^ 1 2.5 us 2.2 Mi. IL25 ii.4 |£ 1 2.0 m 1.6 ^ *^ '^^ >^J/' % ^" Hiotographic Sciences Corporation 13 WiSTMAiNSTRiET WEBSTIR, N y. MSSO (716) S73-4S03 >^:¥ '^ ;:S;* Ux w chan be t\ ill.. i ^ 'P' natir ordir the s in dii a stri above eastei and I bands in str Leg gneiss isN. sidera an alu the st: Erabh the e.^ posed I presc-ii tain bi essenti these c as to ( these usuall\ was nc Cyaiiit acterizi flattenc present Aboi shore a erous J <-15t At ti structu nearly l;i III THE OTTAWA AND LAKE TEMISCAMINO. 181 I changes first to the west and then to N. 75° W., which latter seems to be the general direction of the foliation in the vicinity of the Cave P ipids. At the bluff on the east shore, the rock is composed of alter- nating bands of light- and dark-grtay micaceous gneiss, e.idently of the ordinary granitite variety, and shows a strike of N. 55° E. and a dip to the south < 10°-15\ Above this again the foliation exhibits a change in direction, and about three-tjuarters of a mile below the Cave Rapids a strike of S. 75 E. was noted, with a dip southward < 20. A little above the rapids, the evenly foliated gray gneiss trends in a north- easterly direction, dipping to the south-east < 30\ Between the Cave and Les Eraljles Rapids, the granitite-gneiss, which in the more basic bands seems to contain some hornblende in addition to the biotite, varies in strike from S. 70^ W. to N. 70' W. witli a soutiierly inclination. Les Erables Rapids are caused by the outcrop of ledges and islets of At L«s p;ra- gneiss, which obstruct an already much contracted channel. The strike "" "''"^■■'" is N. 70' W., while the dip is northwards at an angle usually con- siderably less than 10'. A little above these rapids the foliation has an almost east-and-west direction, while near the mouth of Snak<^ Creek the strike is N. 80 E., and the dip 8. < 70 . From the head of Les (jmissps Erables Rapids to about half a mile beyond the mouth of Snake Creek, cmtuining ' '' . clyaniK'. the exposure'^, which wore \ery closely examined, show a gneiss com- posed of alternating bands of light- and dark-gray colour. The bisilicate present, which, from its preponderance, gives the dark colour to cer- tain biuuls, is biotite, and the rock is thus a granitite-gneiss composed essentially of felspar (chiefly orthoclase), quartz and biotite. Besides these constituents, there are others, which in places are so abundant as to characterize the rock. The principal and most interesting of these is cyanitc, although individuals of an almandine-garnet are usually numerous, especially in the more basic portions ; while giaphitc was noticed finely, though rather thickly distributed through the rock. Cyanite of a prevailing blue colour is frequently so plentiful as to char- acterize large exposures of this gneiss. It occurs in rectangular or llattcnf d prisms, which are very long and blade-like in their lialnt, presenting round, jai.'ged, or irregular terminations. About a mile below The Mountain Rapids, the high hills on the east R,,(•k^l noar shore are formed of alternating bands of light- and dark-gray yarnetif- J'"' ■)I""">''ain '^ ° . O J P Kill>|ll.S. erous granitite-gneiss, striking S. 55 W., and dipping south-easterly <'15 toG0°. At the foot of the Mountain Rapid, the gneiss is more massi\ e in structure, although still preserving a distinct foliation that runs nearly east-and-west, while the dip is to the south < 35 to 40. In ■-■* 1 .'1 r i mM I lit. i:il I i i\ I !j Ill h *iiii 182 I NIPISSINO AND TKMISCAMING KEOION. A1k)V(' the Kill litis. At narrows of south Seven Ltagiit Lake, On noitlicrn part of hike. Rocks liftwefii Ldiitr Siiiilt and LaUe Keepawa. places it is filled with small crystalline or irregular fragments of gar- net, while the rock in general has a distinct reddish colour. The jNIountain Rapid runs for the most part in the strike of the rock, which is a dark-gray, well foliated gneiss. The ridges and islets are composed of this gneiss, presenting a strike varying from S. 50' E. to S. 5')" E., with a dip to the north-east < 20' to 30'. About a mile above the Mountain llapid, on the west side, the dark-gray, niicaccoiis or granititegiu-iss strikes S. 70' W., with a dip to the south. About one and a-half miles above this point, a gray gneiss was noted with a decided foliation, exhibiting a series of beauti- ful curvings and *wistings, while the general strike is N. 60' E., with a liip to the south-east < (15 to 70^. About four miles above the IMounlain Itapid, a massive, tine-grained, red gneiss was noticed, asso- ciated with some more evenly foliated, gray gneiss ; the whole dipping 40-80'. In the vicinity of the narrows of Seven League Lake, and for some distance beyond, the gneiss is in many i)laces much contorted, and usually of a dark-gray colour, owing to the prevalence of the mow basic liands. In many places the rock runs in long cur\es, presenting a gentle undulating dip, which often approaches horizon- tality, while at other points not far removed the bands are almost on edge. lieyond the narrows on Seven League Lake, the gneiss, which has a gray colour and is well foliated, strikes about S. 65 E., with a southerly dip at a low angle, generally from 20' to 30°. Opposite La Tuque, on the east shore and below the mouth of Obashing Creek, tha lighter coloured bands, which are reddi>ig Oltashing Lake, the gneiss is usually well foliated, often OnObasliinj,' ova light-gray colour, although some portions present • eddish-coloured l,>!inds where the fclspai" contains much iron oxide, and the general strike in the vicinity of the narrows varies fi'oni S. GO E. to S. 75' E. with a dip to the south < 15 to 30°. A.t the east end of the little island in the ba}- out of which the road goes south to the small lake at the hcad-watci's of Snake Creek, the gneiss is conijiosed of alternating reddish and dark-grey bands, in filaces somewhat contorterl, and shows a general stiike of S. 85 Vl. with a dip to the south < 7C to 80 . Near the east end of Obashing Lake, the dark-gray well foliated gneiss strikes S. 8-1 E., and is either ijuite vertical or dips at a very high angle to the south. >iear the outlet of Little Obashing Lake, the gneiss, which is distinctly foliated and has a reddish colour, strikes east-and-west, dipping south at an angle of about 35". The suialler lakes to the southwest of Little Obashing Lake, generally present high shores which are well wooded and green to the water's edge, so that there are only limited opportuni- ties afforded for ascertaining the trend of the bordering gneiss. On a small island in Thompson or ^IcConnell Lake, however, gray gneiss was noticed dip})ing S. 20 W. at a low angle. Xear the head of the Long Sault, on the west shore of the Ottawa, n .i. f,.,„„ the ''neiss is composed of alternatin'' li'dit and dark bands. Many of ''""K ■'^;'»lt ' 1 til U],iiiiika the lighter bands have a flesh-red colour where the felspar is abundant, XanuWH. while others are grayish or nearly white. The dip is S. 30' W. < 20 . There are comparatively few exposures of rock between the head of the Lang Sault and the Opimika Narrows, and the strike at some of these is hard to ascertain witii any degree of certainty. The general strike seems, however, to be S 55' E., which is apparently maintained as far as Schooner or Ship Island. On the east shore, opposite this island, the gneiss, which is exceedingly well foliated in alternating bands of light-gray ileshred aiul dark-gray colouis, dips S. 10 "W, < m. ■i i; ■ ■ i r II 184 I NIPISSIVa AND TEMISC/VMINO REGION. '? i! Curving utrikf I if fuliatiun. Region 8imth-\vcst ■ C)|iiiiiik:i \ rowH. Region nortti-wcst ( Opiiuika N rows. To the south of the Opimika Narrows, on tlie west side, and nearly opposite Luniaden's depot (Opimicong P. O.) is u gray, ratlier fine- grained, evenly foliated micaceous rock, showing lenticular areas of quartz and felspar which are comparatively free from coloured consti- tuents. The microscope shows the rock to be a hornblendegranitite- gneiss composed chieHy of quartz, orthoclase, plugioclase, microcline, biotite and hornblende, whith smaller quantities of ilmenite a.ssociated with leucoxene, sphene, apatite, calcite, zircon and epidote. The dip of this gneiss is S.W. < 45 . This exposure marks the southern end of a great curve in the gneissic rocks, the Opimi'-a Narrows conforming closely with the strike of the rocks in their bend. At the southern end, the strike is north-west, about half-way through it has changed to S. 75 W., at the north end of the Narrows the strike is N. 15" W., while still further north on the same side it bends around to N. 30' W., and near the mouth of Ottertail Creek the rock strikes N. 35'^ E. The gneiss, in this interval, is of the usual gray micaceous variety, occurring in alternating light and dark bands, while the dip is to the west or north-west at high angles, usually about 05°. A thin section, cut from a specimen obtained at the exposure innuediately below the mouth of Opimika Creek, showed the rock to be a gianitite-gneiss, composed chiefly of quartz, orthoclase, plagioclase and microcline, with biotite, epidote and sphene as its principal coloured constituents. In the region to the south-west of the Opimika N.arrows, the country is well wooded, and the few rocky outcrops encountered have a general south-westerh' strike. Near the small bridge on the old McLaren lumber road, crossing Opimika Creek less than a mile from the lake-shore, the gneissic rocks are very evenly ami distinctly foliated, showing intcrlaminations of reddish light-gray and dark-gray material, the whole having a strike of nearly north-and-south and dipping west ' 20 . Two miles south-west of the lake, other small out- crops of a light-gray granitite-gneiss occur, dipping S. 50 W. < 35^ Near the end of McLaren road, the rock is concealeil for the most part by sand, but here and there hutnmou'ks of gneiss occur. One of these, situated about tliree-(iuaiters of a mile from the end of the road is composed of gray well foliated gneiss dij)ping S. 80 W. <20'. To the north-west of the Opimika Narrows are situated Long and White lakes, which empty into Lake Temiscaming a short distance north- west of Lumsden's depot. These lakes are noteworthy as affording an opportunity of ti-acing in some detail the genei'al outline of an immense curve in the strike, that, starting at the south end of the Opimika Nar- rows w Beauvi compo.s which the lay« the lak( On W the nor west. gneisse.s iiig sout On tl very pli long slei portions BARLOW 1 THE OrfAWA AND LAKK TEMISCAMINO. 185 I rows with a direotion N. 40' W., circles arouiul to S. 65° E. at the Beauvais Narrows on I'vke Keepawa. On Long Lake, the gneiss is composed of successive bands of reddish-gray, gray and llesli-red colours, whicli vary in strike from N. 20" W. to N. 7 W., wliile the attitude of tlie hiyeis changes from nearly horizontal in the south-western pait of the lake to an inclination to the west of ;)5° in the north-eastern part. On AVhite Lake, the rocks curve around gradually to N. 53 E., and on the north shore the gneiss lias a strike of only a few degrees south of west. These rocks are light-red, reddish-gray, light-gray to dark-gray gneisses, the layers running in low, broad undulations with a prevail- ing southerly dip at angles varying from 5' to 10^ On the north side of White Lake, there is a reddish contorted gneiss On Wliite very plainly foliated, a ferroniagnesian constituent being present in long slender dark-grecjnish bands, while in the wider and more felspathio portions such coloured constituents are almost entirely absent. To the north-east of McMartin Point, on the portage going to White On jwrtatre to Beaver Jjake, the gneiss is exceedingly well tohated, running in long Lake, generally straight and somewhat continuous bands of alternating liglit- and dark-gray colour and varying in strike from N. 40' 8. to N. 50 E.: with a prevailing north-westerly dip at high angles generally about 75". Exposures on the south shore of White Beaver Lake exhibit a light reddish-gray gneiss in successive bands of lighter and darker colours, the whole showing a changeable strike from N. 60" E. to N. G8'' E., while tiie folia arenevrly if not quite vertical. B(!tweon McMjirlin Point and Latour's mills, the east shore of Lake Of cast slmro Tmnisciining is very high and precipitous and for considerable stretches j'jj"' •\',\^^f' presents perpendicular rocky clifls. For two miles above McMartin Point, the gneiss is compaiatively massive and chielly of the red variety, although gray bands may be noticed marking the foliation. This rock has, in general, a dip N. 65' W. < 35° to 80'. The com- liined action of the weather and tlie waves of the lake have served in many places to remove an appreciable portion of the softer and more micaceous bands, leaving the red felspathic parts standing out in rather prominent relief, smoothed and planed as a result of glacial action. The surface now exposed exhibits, in great perfection, even the smallest bendings and foldings which these rocks have undergone. In the last half mile of the distance already mentioned, the gneissic rocks seem to strike approximately with the trend of the shore-line, exhibit- ing beautiful examples of contortion, while in other places the rock lies in a series of low undulating folds. Above this, for a little over four miles, and extending a short distance beyond Latour's mills, are » :' '■; rr :^ 18G I MJ'ISSINli AND TKMISCAiMINU UK(iION. I '! ! ■ ( ii MIM iij'i II I! H 1^ Of west si Idle near MrMar- tiu I'uiiit. Rocks o|ii)o- siti' riiitiiiirs mills. Jiu'hisions ill gneiss. almost contiiiuouH exposurtis of inicafpons or lagioclase, orthoclase, quartz, hornblende, bititite and ejiidote, with sphene, apatitt> and zircon as accessory constituents. Opposite Latour's mills, and for a short distances both north and south, the gneiss is well laminateil, exhibiting precisely similar features to that on the opposite; side of the lak(\ The felspathic bamls, which are usually ileshred, are rathei- line-grained and contain little quartz or mica, while the darker bands show a superabundance of biotite and other ct)loured constituents. In several places, associated with this gneiss and evid(>ntly caught up in it, are irregular masses of a dark -green, almost uralitic diabase, with somewhat largo and glistening scales of dark-lirown mica. The surface of this rock weathers very unevenly, presenting a very rough and pitted character. This roughness is increased by a series of intri- cate, reticulating dykes of a line-grained aplite or granite that stand out in strong relief. Under the microscope, the rock is seen to be an altered diabase, the hornblende showing uuiloubted evidence of Inning been derived from pyroxene, while traces of a rude ophitic structure TIIK OTTAWA AND LAKT. TK>IISCAMIX(i. 1S7 I Cllll s till )0 (lotoctod Tl K* Other iiiiiu'ials jxesent iire hiotilc, j)la>;i clase, garnet, and iron ore.* l>oLweeii Liitour's mills and the western end of the old Indian port • age-route to Lake Keepawa, the gneiss is not so regular as that further miiis. (in kn llOltll sou th, and in some places runs par allel with the shore-line, while at others it forms considerahle angles with this direction, makin the most part interfoliated with the prevailing gnei.ss. These pre.seni many of the characteristics of paifillel or interfoliated dykes, and snnu' jiiirlions of them cut across the foli.iiion, but their true relations won- not studied in detail, so that it cannot Lt stated with certainty whether tluy are of later origin than the gneiss with which they are associ- ated. Tlu^ micrt)scopic examination (tf two thin sections .shows tluit, although it must bo referred to as nuartzinica-dioritegneiss, it dillci's in many particulars from the basic bands of the ordinary gneiss to which this name has also been applied. It has very evidently been I'ludiutd liy (lerived from the shearing of a basic eruptive rock, resulting in lis ^ "''""'*^' more or less complete iv-crystalli/ation, and seviMal places weio noticed throu.;hout the regit)n where a similar rock could be traced dii-ectly and continuously into the ordinary massive phase, which for sonn; reason had escaped such complete deformation. ( ine of the localities where this can })erhaps be seen to the best advantage, is on the shores of one of the smaller bays running to the north-west, and forming part of Leon- aid Inlet, on the west coast of Shabosagi or Wicksteed Lake. This amphibolite, or (piartz-miea-diorite-gneiss, is composed of quartz, j)lagio- clase, hornblende, with an iron ore (probably titaniferous) and epidotc, g.irnet, apatite and zircon. Associated also with the gneiss near this point is some of the uralitic diabase already described as occurring on the west shore of the lake. From the Indian portage northward to within about two miles of Ivist sliuic, iinrtli to Ml ll'4ill JiiviT. the mouth of the Montreal River, the rocks pre.sent the usual alterna- "'"''' '" *^'""" tion of reddish, gray, and ahnost black bands. The strike of the folia- tion is somewhat irregular or divergent, but the general directions are indicated on the accojupanying map. Alartel Point, as well as the shores of the small bay to the south, and some small rocky islets lying close to the eastern shore of the hike in this vicinity, are composed lic>p'. From lUilValo llock nortliwanl.s along the west shore, the strike of tlie gneiss docs not show any wi(h> variation, the lioneral direotion being from S. 4o \S'. toS. 05 W. with a dip to the south-east c^ 40 to 80'. The general colours are shades of light- and dark-giay, with some reddish l)ands where the felsnar has been stained by iron. A specimen obtained tVom ^m exposure noai'ly opposite the mouth of the Keepawa, siiow.> a tint'-grained, gray, evenly foliated, micaceous rock, slightly discoloured throughout by iron oxide. The microscope shows the rock to be a granitite-gneiss, consisting chiefly of orthoclase, cpiartz, biotite and epidote and bearing a close resemblance to the gneiss exposed near the north end of the Opiniika Narrows, although somewhat liner in texturi'. ('Miitinr nf The contact between these gneissic rocks, m.apped as i^aurentian, Luuciiiiuii 1,11 • 1 ■ 1 •1111 and Iliiidiii^iM. and the lluronian locUs, is exposed on tiie west siiore ot tlie laKeal)out two and :i (piartcr miles south of the mouth of the Montreal River. hniiu'diatcly south of the small crock wiiich enters the lake from the west four and a half miles snuth of the Montreal l'i\er, the gneiss has a strike of S. GO W. with a dip 8. 'M E. <^Sb', while in the bed of the creek itself the rock is a])pareiitly of a coarse (hirk micaceous variety, decomposed ahmi.st whiilly In a chlorite-schist associated with some steatite or .soapstone. l"or nearly a mile north of this, the shoi'e is comiMiscd of a tlcsli-red giici-;sic granite, striking from N. GO W. to N. 70 W. and clipping to the south-wesL at high angles The point about a mile to the south of the contact is occui)ied by a m:issive dark mica- diorite or uralitic diabase, inlersected in \arious diicctions by dykesof red gneissic material. Neai' the junclion the Laurentian is repi'csonted by a light i'(>d(li-h or reddish-gray gneissic graniti-, with somewhat iniliNtinct foliation l)ut no lamination. TJie I'ock is ma--sive, rather coarse-gi'.-iincd, containing a comparatixi'ly small pro[ioi'tion of hisilicate mateiial. I luler the microscope it is st^en to be a graul' ite-gm-iss, the felspar having undergone somewhat advanced saussuriti/ation, wliile the biotite originally piesimt has been wholly con\erted into chlorite. I'lViMciacviii- gloiiicrati' at tlic contact. Contiiiiiod fi'atirini'nt.-!. The rock in contact with this gneissii; granite on the wi>st shore representing the lluronian, is the typictil and widespretid lireccia-con- glom(>rate described by Sir William Logan as "shite conglomerate" or "chloritic .slate conglomeiate". This rock contains numerous angular as well as rounded fragments, among which those of a somewhat coarse tlesn-reil granite are the most abundantly re])res(mted. These granite pebbles ;ire composed chiefly of (lesii-icd orthoclase, with a smaller (|uantity of grayish translucent quartz and relatively little biotite, which has evidently undergone very c • u k i i# I ■ *■ II! advanced rock wliic were noti chiefly (|U tal iiiatei i epidoto ai and inatri The coars to tlu' lilK curves arc The gni together a it not for pieces exh of contact direction granite ha siniihir irr ate. It is tliat they rocks witli posing the a deeper n exposed on Besides, tl often conti similar roc The Hui the lake, is generally c a specimen of the rivei occasionall; microcline, division, w smaller int like in chai or conchoid dipping S. I developed s north of tl: TIIK OTTAWA AND I.AKi; TKMlHrAMINfi. 189 I advanced alteration to chlorite. Occasional specimens of a dark-green I'ock which seems to be an extremely fine-grained and altered diabase, were noticed, while irregular and angular fragments of simple minerals, chiefly (|uart/. and felspar, are rather abundant. This coarse fragmen- tal material is held in a dark-green slaty matrix, in which chlorite and epidoto are the most abundant constituents, llolh the larger fragments and matrix have been subjected to intense and long continued pressure. The coarser fragments are .scjueezed out in a direction at right angh'S to the line of junction, while the softer and more yielding matrix curves around these inclusions. The granite iind conglomerate are very closely and firmly cemented Aotnal lino of together along their line of junction, and it would be (juite easy, weii- J'""-'*"'"' it not for the broken and jointed character of both rocks, to .secuii' pieces exhibiting portions of each in the same band specimen. The lini- of contact in the immediate vicinity of the lake runs in a general direction of S. 7*)' W., but this line is not jjcrfectly straight, ns the granite has a somewhat sinuous edge which is followed '.ery f ilthfully by similar irregularities in theschi^'^^c structure of the breccia-conglouv^r- ate. It is (juite e\ ident from an inspection )f the coarser fragments that the}' have not l)ee.. Jerived from the disintegration of the gneissic rocks with which these elastics come in contact, for the n)inerals com- posing them aie much coarser in their method of crystallization and of a deeper red colour, resembling closely in these particulars the granite exposed on both shores of the lake to the north of the Old Fort Narrows. Besides, the rock in immediate contact with these Laurentian gneisses often contains far fewer fragments of such matei'ials than exposures of similar rock farther removed from the line of junction. The Huronian to the south of Montreal River, on the west shore of (^Immctir the lake, is as a rule represented by a fine-grained felspathic sandstone, |I,,.,,.'\'i','!,\'t'J',.^] generally of a pale greenish-gray colour. ]Microscopic examination of If'vtr. a specimen obtained about a mile and three-cpiarters south of the mouth of the river, shows this rock to be made up of angular, sub-angular and occasionally of rounded fragments of orthoclase, ([uartz, plagioclase and mierocline, cemented together by similar material in a finer state of division, with some chlorite, epidote and serecite often filling in the smaller interstices. In many places this rock is very hard and flint- like in chanacter, breaking readily under the hammer with a splintery or conchoidal fracture. It occurs in somewhat thin beds, often shaly dipj)ing S. 83° W. •< 20° while a set of cleavage planes which havti been developed as a result of pressure dip S. 20° E. <^ 70°. At the point just north of the contact, the rock is a greenish-gray compact slaty grey- ; n i! :. I A- i 190 I NIPISSINC. AND TEMISCAMINO REGION. °^ti' !•:, i if East shore, north (if Mar- tel I'oiut. Character of breccia-con- glomerate. wackt', wliich has evidently been subjected to gnat pressure and alter- ation, for a distinct foliation or chistose structure has been developed, the various Ijands of the rock being squeezed out into lens or pod-shaped areas, while pronounced curves in the direction of the schistosity may be observed, due to the unequal resistance (loforniation offered different bands and portions of the rock. At the immediate line of contact the parallel structure of both Laurentian and Huronian coniform with one another, these being produced as a result of mutual reaction, the resist- ance olVered by the neighbouring clastic primarily determining the direc tion of foliation in the granite, while the forces of upheaval in the gneiss have served to compress very materially the neighbouring clastic rocks. The Huronian strata which are here present, form a curiously lengthened wedge-shaped strip between the Laurentian granite and the laccolitic or overflow mass of diabase which constitutes the summit of the " King of the Beaver." On the east shore of the lake, from Martel Point northward, the Laurentian is represented almost altogether by a pale tlesh-red granite, showing little or no bisilicate material, the principal coloured con- stituent being epidote, which is somewhat abundant. The contact between this rock and the breccia-conglomerate of the Huronian, is, on the east side of the lake, about three miles north of the jNlontreal River. The actual contact is concealed, but outcrops of both rocks occur within a space of less than one hundred yards and from these it would seem that the line intersects the shore at a point immediately south of a small creek which empties into the lake in this vicinity. Inland, the line is effectually hidden by overlying drift material, but its general direction seems to be very approximately N. 55' E. The granite near the contact contains a large irregular mass of a coarse dark-green diorite. An area of finer crystalline chlorite-schist runs at right angles to the line of junction, and may represent either a small basic dyke which has been subjected to pressure, or an extremely altered fragment of the Huronian greywacke which has been caught up in tlie granite. In the breccia-conglomerate the matrix is often present in very sub- ordinate (juantity. The most abundant fragments are of the usual biotite-granite type, while others of a pale grayish granitic rock, are seen in thin sections under the microscope to consist of phenocrysts of plagioclase or orthoclase imbedded in a fine-grained quartz-felspar groundmass. Besides these, there are some fragments composed of a tine-grained altered diabase and others of a greenish-gray slaty rock (resembling in a most marked manner the compact variety of the grey- wacke of the Huronian) and some gray quartz. v.] THE OTTAWA AND LAKE TEMISCAMING. 191 I The material filling the interspaces is seen under the microscope to Stratificntion . consist of a confused aggregate of scales and grains of chlorite and epidote, with abundantly disseminated particles of iron ore and fine granules of sphene and epidote. At first sight this conglomerate, occurring as it does in very massive beds, with no pronounced parallel- ism in the arrangement of the larger fragments, seems devoid of any definite structural features, but a closer inspection shows the strike to he about N. 50° E. while the dip is to the south-east <10°. As here exposed it forms a hill about four hundred feet in height, presenting a very sharp and abrupt northern face, while to the south it slopes more gradually down towards the line of demarcation between the two formations. To the north and west, this rock is succeeded by a dark greenish-gray, compact, slaty rock which seems to underlie the breccia- conglomerate, although in other sections the conglomerate occurs at the very base of the Huronian. The exposures at this place, however, are not in immediate contact, so that the relations of the two could not be ascertained with certainty. On the small island in Lavallee Bay, the rock is a fine-grained. Rocks on greenish-gray greywacke, much squeezed and jointed, breaking with a conchoidal and somewhat splintery fracture. The small island near the east shore about a mile south-east of Roche McLean is also formed of a similar greenish-gray compact felspathic sandstone rather massive in structure. ■; ■ 'r " The western shore of Lake Temiscaming, from the Montreal River to Roche McLean, is occupied by the massive, bedded, breccia-con- glomerate which dips in a westerly direction at an angle of 15° This rock has already been described. A specimen obtained from an exposure about two miles north of the Montreal River^ however, showed the matrix to be relatively more abundant than usual. The diabasic pebbles are also more plentiful than those of red granite, while fragments of simple minerals predominate greatly over those of composite rocks. The quartz and felspar fragments are sharply angular, while the composite individuals are as a rule somewhat rounded. In the conglomerate near Roche McLean, the pebbles are more rounded and much more sparsely disseminated through the matrix. Pieces of an extremely altered diabase were noticed and also some of a fine-grained greatly crushed quartz, filled with small scales of aerecite and chlorite. The reddish pebbles are of the prevailing type of biotite -granite or granitite. Roche McLean itself is a large rounded and glaciated hummock of this breccia-conglomerate, separated from the west shore by a narrow interval at high water. West shore Montreal HivHv to Roclie McLean. I ; -■!; •in '; » I , ■ 192 I NIPISSING AND TEMISCAMINO REGION. m West shore, north of ilurUe McLt'ivn. Isliind Point Spotti-d granite. (Jul tin Puint To the nortli of Roclie McLean, the western shore for a distance of a little over a quarter of a mile, is occupied by a series of dark-gray slaty rocks, the only .structural feature discernible being the planes of cleavage, which dip northward at a high angle. This comes in contact with, and is somewhat altered by, a small intrusion of diabase which is doubtless an extension of the large mass which comes out on the eastern shore at Quinn Point, To the north of this diabase, the mas- sive breccia-conglomerate again outcrops, and is penetrated by a mass or dyke of similar diabase, but with this slight interruption con- tinues northward along the shore almost as far as Island Point. This point is so named because of the existence at high-water of a narrow and shallow channel separating it from the western shore. It is composed of a iimch squeezed, contorted and altered slaty grey wacke, continuing a considerable quantity of epidote. It is pierced through- out by small and intricate granitic intrusion which have evidently assis- ted matei-ially in hardening and otherwise changing. To the north this rook is again succeeded by a conglomerate, containing the usual abund- ance of granitic fragments embedded in a dark-green diabasic ordioritic paste, resembling a diabase-tuli'. Aboutaquarter of amilenorth of Island Point, this rock comes in contact with a fine-grained hornblende-granite that forms the shores of the bay to the south of Pointe a la Barbe, extending inland in a north-westerly direction and possibly connected with the mass of granite exposed on the western shore of the lake above the old Fort Narrows, although it is very different in appearance from this. In many places, this granite shows dark patches, generally oval or rounded in outline, varying in diameter from a few inches to a foot or more. These patches are caused by the segregation of the coloured constituents and the more or less complete exclusion of the felspar and quartz. They constitute what are familiarly known as the " dark spots" (ausscheidungen) so commonly seen in granites, and evidently represent the tirst-forraed nuclei in a slow-cuoling magma. Quinn Point, is the name usually applied to a series of rugged hills that form the shoreward extension of a pronounced range that extends with little interruption for some miles to the north-east. The rock composing these hills is a dark greenish-gray uralitic diabase, in which the ophitic structure is generally apparent to the eye. The rock varies in texture, the coarse phases assuming more of the holocrystalline or granitoid structure, characteristic of gabbro. Jointed structure is very perfectly developed, one set of planes dipping westward <; 80° while another series dips eastward <^12°. The rock is composed chiefly of ■] THE OTTAWA AND LAKE TEMISCAMING. 193 I Cull Rock rshincl.-. pliigiocliise, which frequently contains much disseminated iron oxide, <,'iving it a red hue, and hornblende, which has evidently resulted from the alteration of augite. A small ijuantity of some carbonate (probably dolomite) a little interstitial quartz and titanic iron ore were also noticed. The Gull Rock Islands are situated about half a mile nortii of Quinn Point. There are two of them, presenting low rounded and well glaciated surfaces, but little raised above the high-water level of the lake and almost destitute of vegetation. The rock composing them is the breccia-conglomerate, containing very numerous and often well rounded pebbles and boulders, chiefly of red and reddish-gray granite, with some of a compact dark-green altered diabase and a few of a fine- grained greatly crushed quartzite. The matrix consists of the same sort of material in a finer state, with greenish chlorite filling in the smaller interspaces. Moose Rock is the name applied to a huge boulder of rounded out- :mo()s(! Rock, line, perched upon a shoal. It is almost thirty feet in diameter and must have been detached from the cliffs of similar rock on the east shore, over a mile to the northward of its present site, it has been moved during the glacial period. The northern end of Point a la Barbe, on the west shore, about two Hrnxi.i nf iiiiies south of the Old Fort Narrows, is formed by an island which, at ]/,|l.'i',t/^ '^ high-water, is divided into two almost equal parts, connected by a slender rocky peninsula. The rock composing it resembles the finer- grained, harflened and altered matrix of the breccia-conglomerate. On the opposite shoi'e a steep rocky point juts out into the lake, forming a niUTOws. The breccia-conglomerate is here exposed for a considerable distance along the shore either way, reaching to within about a quarter of a mile of the mouth of the Little River. The shore-line at this point rises steeply into a hill nearly four hundred feet in height, forming the shoreward extension of a conspicuous ridge that runs for several miles to the north-east, and marks the southern limit of the Little River valley. The rock has a strike of about N. 00^ E., and a dip at low angle, less that 5\ to the north-west. The breccia-conglomerate here passes upward, by a gradual diminution of the larger fragments, into a compact, fine-grained arkose sandstone or gieywacke, that is exposed along the shore toward the mouth of the Little River. Under the Micioscoiiic microscope, this rock is seen to be made up of partly rounded frag- charac -r. ments of quartz, orthoclase, microcline and oligoclase, embedded in a matrix proportionately less in quantity and composed chiefly of chlorite and sericite. The fragments are nearly equal in size and show 13 ■ ,^ ;■■ .;.■: ■1"! n i m Mill: ii:!k 0\-rlying bciN, Rocks near Old Fort. Granite area nortli of Old ]''urt. Cliaractcr of granito. 194 I NIPISSIN'(i AXD TKMISCAMING REGION. no pronounced rounding. The greenish colour is owing mainly to the large amount of chlorite present in the matrix. To the north, and in ascending order, this rock is succeeded by a somewhat coarse-grained sandstone or grit, which forms the point immediately north of the mouth of the Little River. It also extends across the lake*, occupying a corresponding promontory on the west side, known as Blueberry Point. On both sides of the lake the rock occurs in thick massive beds, the stratification being shown only by the occurrence of conglomeritic bands disposed in a somewhat con- stant direction. The rock is much jointed and broken, the fragments having a rough "hombohedral outline. To the north, it is concealed in great part by the deep and extensive sand and gravel deposits that form the narrows opposite the Old Fort, but occasional outcrops may nevertheless be noticed. The rock extends along the east shore of the lake, nearly three quarters of a mile north-east of the Nar- rows, where it reposes directly on a massive red biotite-granite, although the actual junction is concealed. To the south of the nar- rows, the rock occurs either in horizontal beds or dipping at a low angle to the north-west, but north of the narrows it seems to dip S. 35° E. < 20° A specimen obtained from a point composed of this rock about half a mile east of the Old Fort, is a pale yellowish-green coar.se-grained quartzite or grit. The thin section under the microscope shows it to be composed of quartz and felspar embedded in a groundmass made up of pale yellowish-green sericite, for the most part present in exceed- ingly minute scales. The granite which replaces the quartzite to the north-east of the narrows, is exposed on both sides of the lake. It forms the western shore as far as Paradis Bay, a distance of about four miles, and extends from half a mile to a mile inland. On the east side it com- poses Wine Point and the southern shore of Kelly (Priests) Bay, extending for a short distance west of the steamboat wharf to the point already mentioned, about three-quarters of a mile north-east of the Old Fort Narrows. In all, these granite exposures cover roughly an area of six miles. Microscopically, the granite is rather coarse in texture and of a deep flesh-red colour, owing to the marked predomin- ance of the felspathic constituents, all of which have been abundantly stained by iron. Several small areas were noticed which have assumed a greenish colour owing to the epidotization and sericitization of a portion of the felspar ; but such decomposed portions are proportionally insigniticant, •] TflE OTTAAVA AND LAKE TP^MISCAMmO. 195 I and the whole mass of the rock is extremely uniform, not only in colour but ill the relative abundance and mode of development of its mineral constituents. The (juartz occurs for the most part in somesvhat rounded tliough itrejLfular isolated areas, giving to the rock aconglome- ritic or purpliyritic appearance, a fact noted by Sir William Logan on the manuscript map embracing his survey of this lake made in 1S4">. Indeed, the rock at first glance presents a marked resemblance to some of the brick-red (juartz-porphyrites of Lake Superior. The ferromagne- sian constituent is present in very small quantity and is now almost wholly converted to chlorite, the deep green colour of this mineral being probably the reason that the rock has hitherto been described as a hornblende-granite. On previous geological maps covering this area, this granite received ronncr views the colouration usually applied to an acid eruptive, and as nothing ^\^[^ granite was stated to the contrary, it was very naturally inferred that, as such, it was of later age than the Huronian elastics with which it is associ- ated. Sir William Logan in his early report does not give any details of its relations with the neighbouring stratified rocks, but only speaks of it as "interrupting" the sandstones on Lake Temiscaraing. During the progress of the present survey, a detailed examination was made of the line of junction between this granite and the quartzite-grit. The best locality for investigating the various contact phenomena, is situ- ated in the small bay immediately west of the steam-boat wharf at Bale des Peres. In addition to the observations made on the ground a large suite of specimens was obtained illustrative of the line of junction, for microscopic examination. The facts obtained indicate the derivation of this quartzite-grit or Clantic rocks arkose from the disintegration, i}i situ, of the granite, and is believed to jj be an almost unique example of the recognition of a portion of the ori- ginal granitic floor upon which the Huronian sediments were deposited and from which they were derived. In the vicinity of the line of junction between the two rocks, the Line of jimc- arkose or quartzite may be poen dipping away from the mass of the '""" granite at a very low angle. Tlie massive and jointed character of the beds of the arkose, render it impossible to ascertain exactly all the minute details of the structural relations, but it is clear that the quart- zite originally transgressed upon the surface of the granite almost hori- zontally. The granite has been unequally eroded and truncated, so that the present line of contact between the two rocks is undulating and irregular. 13^ 4 ■ .-4 I ■ -9 til ■■•; t '■■An' |;^il] m ill' !--:i 4 I 1 196 I NIPISSIXG AXD TEMISCAMIXG KKHIOX. I fi- ll s« Cliiiractcr of uiirtlti red granity. Microeliiit; felspar. Passagf 1m(].m. From a distance, the line appears to be sharp and abrupt, the green ish colour of tlie quartzite showing up very clearly and distinctly in contrast to tiie red colour of the granite. A closer inspection, however, showed that there is a gradual passage upward and outward from the main granite mass to the overlying arkose. Maci-oscopically this pas- sage consists in a gradual loss of the red colouration of thn unaltered granite cand the progressive appearance in its arkose of a yellowish-green hue, although along the immediate contact there is no visible change in the position of the constituent minerals. Thin sections of the least altered portions of the granite exhibit a normal holocrystailine hypidiomorphic structure, witii a tendency to idioniorphic development on the part of the plagioclase. The rook is a rather typical biotite-granite. Tiie quartz is somewhat cracked and the felspar and biotite are more or less altered, but the rock, as a whole, is fairly fresh, and neither dynamic nor chemical forces have acted on it to such an extent as to render its true character and origin doubtful. The junctions between the grains of the various minerals are sharp with no interstitial granulated material. The quartz is the ordinary granitic variety and Is tilled with minute inclusions, frequently arranged in irregular interlacing bands. ^lany of these, when liighly magnified, prove to be cavities filled with fluids and often containing movable bubbles. The larger quartz grains, under polarized light, are seen to be made up of an aggregate of smaller grains with differing orientation, and the quartz has a distinct but not excessive undulatory extinction. The predominent felspar is generally microcliiie, which can be seen in all its various stages of development from grains exhibiting only an indistinct moirt^ structure (Plate V., fig. 2) to those in which the cross hatching is perfectly developed (Plate V., fig 2.) The foimer, however, are the more aVjundant. It is turbid and much stained with iron oxide. Plagioclaso. Plagioclase is as a rule quite abundant, and as already remarked, exhibits a tendency to idioinorphic development. It is frequently embedded or intergrown with the orthoclase and microcline. The individual sections are broad and tabular, parallel to M., and show in great perfection the fine striation due to multiple twining. Their outlines are mote or less rounded. Carlsbad twins appear to be rare, but were occasionally observed. Zonal structure was noticed in only a very few instances and then was not at all pronounced. Like the o.'thoclase and microcline, this felspar is turbid, in consequence of incipient alteration, and little scales of sericite are scattered through (ANlO« ] THE OTl'AWA AND LAKE TKMISCAMINO. 197 I it. Inclusions of biotite are not infrequent. Bending of the twin lamella* is rare, and exists only in a very slight degree. The mean of several determinations gave about -f 10° as the extinction-angle measured on M., between adjacent lainellio, showing the felspar to belong probably to the acidic end of the oligoclase series. As usual, where alteration is commencing, it shows itself in the centre of the crystals. Biotite was the on' ' ferro-magnesian constituent noted in the sec- Biotite. tion. It forms irregular plates and Hakes which are considerably altered to chlorite. The original brown colour of the material has been changed to a light-green, but without entirely obliterating the optical characters of the biotite. Inclusions of ilmonite with leucoxene, are common. Tlie mineral is not very abundant in this particular section. Ilmenite is the iron ore present in the rock, always accompaniec by llnunite. its alteration-product leucoxene, and in some instances immediately associated with zircon and apatite crystals. (Jcuasionally it may be observed replacing titanite, skeleton forms of the latter mineral, with sharply defined acute rhombic outlines, being filled with a mixture of carbonates, ilmenite, etc. Chlorite is present in the rock as the final stage of alteration of the Other constit- 1 ■ , ., Ufiit minerals, biotite. A few irregular grains and crystals of zircon with well-defined zonal structure were noted, and exhibited the usual optical characters of the species. Apatite is also present, but is not very abundant, occurring in small crystals and irregular grains. Sericite, or an allied hydrous mica, is present in minute scales and flakes scattered through the felspar, as the result of their alteration- Red oxides of iron are abundant. At the other extreme, the derived arkose or quartzite-grit show distinctly rounded and water-worn fragments, chietly of grayish trans- lucent .]uartz, varying in size from those only microscopically observ- able, to others which are sometimes an inch in diameter and are arranged in layers which have evidently resulted from a sorting of the material by water action. These fragments are embedded in a groundmass or cement varying greatly in proportionate quantity and composed of a contused mass of minute sericite scales, being the argillaceous product of the decomposing felspar. Ilcrived inatcrials of till' arkose. l.r.' m ^m ll H |l |tH iji' 198 I NIPISSIXG AND TKMISCAMING KKvelop- inent of inicrorHiie at the expense of the orthochise, accompanied hy an incijiient sericitization of the felspar-, which is notice ihle, to a con- siileral)le exh^it, even in the least altered specimens. This is accou.- panit d by marked alteration of tlie hioiite to chlorite, the develop- ment of a distinct undulous extinction in the (juarlz, and a cracking SicuimI stM, r of some of the individual grain-s. A further stage is reached when the Huartz is accompanied by the occurrence of mosaic-like areas between the larger grains, while these latti-r show very pi'onounced strain- shadosvs. Tiio [il gioclase liktnvise shows more frci|atnt evidence of presure in its tv/inning, the lamella' ot'ten in these cases ending abruptly against cracks traversing the crystal, lending of the lainellie is more frequent, while the alteration of biotite to chlorite is more ct-Hiijilete, and is frequently accompanied l>y the ih!jiositit;n of iron ore between the Hakes. Third stagt'. This is closely followed, marking what may be Cilled the third step in the transition, by an aj^preciable advance in the alteration of the felspar, especially of the plagiodase, which becomes traversed by a series of cracks HUed with sericite, the alteration exttnding outwani into the main mass of the individual grains ; but there is still no evi- dence of motion or shoving apart of the fragments. Fourth .stai^(. A fourth, and somewhat sudden advance, appears when the alteration of the felspars has proceeded to an extreme degree, while certain fragments have been shoved aj)art. Kach individual grain still oc 'ipies the same relative position with regard to the other mine- ral constituents, but in places portions of quartz and felspar, especi illy the former, can be noticed to have changed their position along certain cracks traversing the grains, the portions, however, being never widely separated. The plagioclase has been almost completely saussuritized, lea\ing the unaltered quartz grains in almost the original position occu- pied by them. The microcline and ortlioclase, though badly decom- posed, hove not undergone such complete alteration as the plagioclase. Fifth stage The fifth stage is reached when both ortlioclase and microcline have undergone somewhat complete decomposition, some of the individuals being now represented by an intricate mass of their alteration-proclucts. This is accompanied by markedly uneven extinction in the quartz grains, as well as by a cracking and separation of quartz and felspar- crystals, which is more evident in the former. Sixtli stage. The sixth and final stage in the process, shows, that the felspars have almost entirely disappeared, although occasionally irregular cores o 1 i;koI.O(JI(AI, Sl'kvky ok Canapa Vol. \.. Paht I., I'iat.: V Fi(i. 1. Fui. 3. Via. 2. Fig. 4. Kui. 1.— Hiotitf-graiiite or granitite, iiciir Cf(]ar Point, cast side Ijakc Tfiniscaniing— orthoclase, t .;£!' li.;;. i'i 11; i» I ■ARLC ('it &k Stl :' m P Wk h ^s U: ^ 1 1 ■ 1 ( : asajy, 1- In i^^BII ¥■' ■ f- tl..' iiii'. C'Ktl eiiiit Til.- iietic T at'iiti nu'iit llfSS, ,1,'l'itS ii clic iiiici( UllL'lli has ol the gi T'lc (.lis an perpeti diatel} a consi /ontal a very the ex] near \ eastern are coi small J This seating oceasio hard, r thieic a weathe of an ii the exj ■J rUK OTTAWA AND f.AKK TRMIHCAMINfi. 199 I tho unaltered ininenil remain. Tlie ji^rmindiiinHs is now seen to consist (if a line-gruincfl .scrioitic material, in wliich are embedded wliaiply angular or sub-angular fragments with very pronounced uadulous extinction. Tlio whole appearance of tho rock, both in the hand spe- cimen and under the microscope, is that of a typical clastic (arkose). TluTO is every evidence, how(>ver, that much of tho material has not undergone any very wide separation, while the quartz fragments still preserve a tolerably sharp outline, showing no pronounced water- action. The suite of .specimens obtained, exhil)its a still further stage, repre- INrcchaiucally senting the whole process leading to a tliiai assortment and rc-arrange- \^.l[n\_ nicnt of the degi-aded material by w.ator into bands of diflering coarse- ness, and resulting uttimaiely in tho formation of .somewhat typical grits and conglomerates. The change has evidently been iirst mainly a chemical one, primarily attacking the biotite, then the plagiocla.se, niicrocline and orthocla.se and leaving the quartz alone comparatively unchanged. The rock thus softened and loosened by decoiujiosition, liasoflered a less elfectual resistance to the process of disintegration, the process ending finally in the complete breaking down of the surface of the granite mass and the formation of the overlying aikose. The latter rock forms the western shore of the lake between Para- i,i,.,ni>li dis and Martineau bays, opposite Bry.son Island, where it constitutes 'I'l'Htzitf. perpendicular cliffs that rise from 150 to 200 feet, while the hills imme- diately behind, continue with a more gradual upward slope representing a considerable additional elevation. The rock occurs in almo.st hori- zontal beds, striking with the lake, the structure .seemingly representing a very shallow and narrow syncline ; the })eds near the southern part of the exposure in the vicinity of Paradis Day dipping west, while those near INIartineau Bay dip east or toward the lake. Almost the entire eastern shore of the lake, as well as Chief, Drunken and Bryson islands are composed of this greenish quartzite or arkose, excepting only some small patches and strips of Silurian limestone, elsewhere described. This greenish quartzite is remarkabl}' homogeneous, generally pre- its character senting the characters of a coarse quartzose sandstone or grit, but occasionally, as on Drunken Island, becoming liner-grained. It is very hard, resisting well the general influences of weather, and occurs in thick and much jointed beds, generally of a pale yellowish-green colour, w(>athering in some cases to a light-brown to a depth of about an eighth of an inch. It sometimes has a brownish-green colour, in which case the exposed surfaces gradually assume a yellowish-green colour, and in I M ■' fi'lil il!^ ': 1: 200 I NIPISSINO AND TEMISCAMINO UKdION. lifllM" Rt-lntioiiH cif prrcn s« I'ort- 1 f«lr" !?»■ H'l is§ 206 I NIPISSING A\D TEMISCAMING REGION, At Miiples jiDrtage. Contact with gneisses. Character of gneiss. i' «■ . i- stringers composed chiefly of flesh-red felspar and gray (juartz, with occasional small fragments of hornblende. The connection of these small apophyses of granitic material with the lai-ger parent mass of hornblciide-granite-gneiss exposed further east, was clearly established, and these lenticular patches of quartzo-felspathic material become moi'e abundant as the vicinity of the granite-gneiss is approached. The lock contains considerable secondary biotite, developed chiefly along the planes of shearing, and this, in conjunction with lighter fclspathic bands produces a very distinctly foliated rock. The foliation dips westwards at a high angle, generally about 50°. The same rock continues, with the interfoliation of lighter and darker bands, across the fourteenth or Maples portage, at the head of which the course of the river turns rather abruptly to an easterly direction while the width is increased to a quarter of a mile. The dividing line between the hornblende-schists-gneisses crosses this lake-like expansion obliquely. Although the actual contact is not exposed, the two rocks are seen within a very short distance of one another, both striking toward the north-west, while the dip of the foliation is to the south- west at an angle of about 50°. Tlio junction between the two is evidently one of intrusion, the granite-gneiss piercing the amphibolite in the form of the small interfoliated pegmatite-like streaks and patches above described, and it appears that the irruption of the horn- blende-granite-gneiss was the cause of the foliation and alteration of inceptive diabase, producing the hornblende-schist. The granite-gneiss just alluded to, is a reddish, very distinctly foli- ated rock, the foliation being determined by the more or less parallel dis- position of the fragments and individuals of hornblende. The thin section shows the rock to be composed essentially of orthoclase, niicro- cline, hornblende and quartz, with sphene, epidote, zircon and apatite as accessory or accidental constituents. Much of the orthoclase occurs as irregularly shaped individuals or phenocrysts embedded in a iiner- grained mosaic composed of broken up fragments of felspar and quartz. These smaller fragments very often assume the niicrocline habit, which is evidently the result of prevSsure. The larger orthoclase individuals show considerable alteration, especially in their central portions, and although in some cases they exhibit tolerably sharp and perfect crystalline outlines, they are usually more or less jagged, owing to the breaking up of their borders to form part of the tiner-grained mosaic. The hornblende is dark-green, trichroic, and occurs in irregular shreds and fragn\ents having a marked {)arallelism. The sphene id deep brown in colour, and occurs in characteristic wedge-shaped crystals. •J RIVKR AND LAC DKS QUINZE. •207 I Uocks near the lake. The epidole is evidently of secondary origin, and is present in irregular grains and masses of a deej:) straw-yellow colour and strong pleo- chroism. Zircon and a[)atite are in small acicular prismatic crystals. The reddish colour is imparted by the presence of iron-oxide, which fills the cleavage-cracks of the felspar as well as the minute fissures present in the rock itself. This rock continues as far as Lac des Quinze, but near the lake it becomes coarser in textun^ and more highly porphj^ritic, the reddish crystals of orthoclase being frequently as much as half an inch in diameter. The foliation is rather obscure, but on the lake itself is more evident. The fall overcome by the last or fifteenth portage before reaching the lake is about ten feet. Lac des Quinze takes its name from the river The general summer L;ic des level of this lake, as determined by the mean of a large number of '''""'"' • aneroid readings, is 848 feet above sea-level. The area of the lake is approximately forty square miles. A considerable portion of the northern part of the lake is, however, not represented on the accom- panying map. There is a Hudson's Bay trading post on the lake, known as Long Point, while lumbermen now at work in the country near Lake Winnowaia or Expanse, a little to the east of the present map- sheet, have several farms or clearances, and depdts for supplies. The main body of the lake extends to the south-east from the outlet Form andout- for a distance of about eight miles, with an average width of a little """" over a mile. A second, generally about a mile wide, runs northward for a like distance from the outlet and then divides into two bays, which continue with the same general direction for about three miles further, the more westerly of the bays being the one followed in going to Lake Abitibi. About two miles to the east of the north arm, a second narrow inlet extends to the north for about three miles. From the south-eastern extremity of the main body of the lake, two arms branch oflf. The larger one runs to the north-east for about fifteen miles, gradually tapering to a point, where it receives the Upper Ottawa. The second arm runs to the southward for about five miles, and at its south-easterly corner reaches the western terminus of the road from Bale des Peres. A new road from Lake Temiscaming to Lac des Quinze, to the north of the River des Quinze, starts from the foot of the first rapids, but is not yet completed. The .several arms of the lake have all been eroded in a direction corres- Surrounding ponding with that of the foliation of the gneissic rocks, and evidently '""'^^'^*'- !' i -■n'l 208 I NIPISSINO AND TEMISCAMING REGION. represent the more schistose and least resistinj^ belts of these rocks. The prevailin;^ rocks are gray granitic and dioritic-gneissea, the latter containing usually a considerable proportion of biotite in addition to the hornblendu, and with an increase in the abundance of the bisili- cates, passing into an almost black, glistening amphibolite, in which the schistosity is always well marked. Quartz is present in considerable quantity, particularly in certain bands, and epidote was also noticed as a somewhat abundant constituent. At several points on the lake massive crystalline diorite was observed. The gneisses liavo a well marked foliated structure, the inclination of this foliation varying from 30° < 45 in a westerly or north-westerly direction. $M ■ ) ■•; ■'1 ^^^H^B f J- r) i^^H m. 1 '.V. 'HI ', ■> 'i|l^ Kctjjawa. Fiirmanrl sizn p]l»'vati<>n. Lake Keepawa. The name Keepawa or Kippewa means, freely translated, " a very narrow passage between steep rocks," and I'efers to the presence of a gorge in the northern part of the lake, now generally known as The " Canal." The lake is very irregular in form and full of islands. In general the lake may be described as filling several valleys approximately parallel tc that occupied by the southern portion of Lake Temiscaming. The general trend of these valleys, like that of Temiscaming, cuts across that of the foliation of the gneissic rocks, except in those portions to the south-east of Roche a Corbeau and the Beauvais Narrows, where the main direction of the lake corresponds rather closely with the foliation of the adjacent gneisses. The greatest length of the lake, from Chemagan Bay on the north, to the portage leading out of Jeanbeau Bay on the south, is almost thirty-two miles, on a line bearing S. 12° E. It may be said to be divided into two main portions occupying an approximately parallel position, each, how- ever, branching off in bays and arms in various directions. These two larger portions are connected about the centre by a few comparatively narrow channels. The portion to the south-west, extending from the outlet at the north-west end of Sandy Portage I>ay to Jeanbeau Bay, measures twenty-seven miles in a direction of S. 38° E. ; while the large body of water to the north-east, reaching from the north-west end of Taggart Bay to the outlet of Hunter Lake, a distance of twenty- eight miles, has a general trend of S. 42° E. The ai'ea of Lake Keep- av. . , 'ling the islands, is nearly 120 square miles. Its height ;'' a i'jvel varies from 87G to 88G feet. The Keepawa River, its 11 !• 1 o',.?k't, is a crooked and rapid stream which enters Lake Temiscaiiiing a iutle over six miles below the Montreal River. The lumbermen ha ve, however, built a dam across the Keepawa at the ■] LAKE KEEPAWA. 209 I north-west end of Sandy Portage Bay, thus raising the water-level. Artificial The rocky obstructions between the south-western part of Lake Keep- awa and the ponds at the head-waters of Gordon Creek having been removed, a large portion of the Keepawa waters now discharge by this artificial channel. In this way the " drive " for logs is much short- ened and the water held back till required. The greater part of the shore-line of the lake is somewhat Surrounding high and rocky, the sui'face being often strewn with large boulders, chiefly of the underlying gueissic rocks. There is little level land, although clearances have been made and farms cultivated in connection with lumbering. Most of the white pine of first quality has been cut, but the shores are still beautifully wooded. Of the very numerous islands, McKenzie and Karl islands are the Islands, laigest, the former being a little over five miles in length and averaging about two miles in breadth, while the latter is scarcely half this size, measuring a little over two miles in length by about a mile and a-half in width. The " Canal," already mentioned as giving its name to the lake, is a picturesque feature, being a narrow gorge about a ([uarter of a mile long with perpendicular walls of gneiss situated, about a inile north- west of Mackenzie Island, and it leads into a couple of small lakelets or expansions. The rocks so abundantly exposed along the shores and islands of ( Jneiss of uni- Lake Keepawa are remarkably uniform in composition and macro- tg,'."' scopical characters. They are typical examples of " gneisses " being, as a rule, very distinctly and evenly foliated, and exhibiting darker and lighter-coloured bands of more or less basic character. The more acid bands are usually of grayish, reddish, gray or flesh-red colour ; while the more basic bands are of varying shades of darker gray, becoming almost black in certain instances. The lighter-coloured pliases are, perhaps, the most abundantly represented, and besides occurring as interfoliated bands associated with more basic material, these in themselves constitute the greater portion of somewhat impor- tant and extensive rock-masses. Under the microscope, they are seen Microscopic to contain orthoclase as the prevailing felspathic constituent, and biotite as the principal and often the only ferromagnesian mineral. They must, therefore, be referred to as biotite-granite or granitite- gneiss. Besides these, microcline is usually abundant, together with some plagioclase (usually oligoclase). A large amount of quartz like- U ill 1 struoture. wj PJi ill The darker rocks. Rocks near Kippawa post-oHice. On sotithern part of lake. 210 I NIPISSINO AND TEMI8CAMIXG REGION. wise accompanies the felspar. The biotite is, as a rule, fresh and of a deep brown colour, occasionally showing alteration to chlorite A little muscovite (most of which is of secondary origin), sometimes occurs, but not in sufficient (juantity to characterize the rock. Besides these, smaller quantities of epidote, sphene, sericite, chlorite, apatite, zircon, magnetite, and sometimes allanite, are usually present. Occasionally, somewhat darker and more basic portions are seen to contain a compact dark-green trichroic hornblende in addition to the biotite, the rock thus becoming a hornblende-granitite-gneiss. These portions are usually of a dark-gray colour, and show a very n;arked abundance of the coloured constituents. The very dark-gray, almost black varieties, in which but little of the lighter-coloured minerals can be macroscopically detected, often show plagioclase as the prevailing felspar, while biotite is replaced by hornblende, the principal ferromagnesian mineral, although biotite is likewise almost invariably present. The constituent minerals are essentially the same as those present in the more acidic phases, differing only in their relative proportions. The structural relations of these rocks show that they form integral and inseparable portions of one complex, produced by differentiation during the slow cooling of a magma of moie or less heterogeneous com- position. At the head of Gordon Creek, and in the vicinity of Kippawa post- office (formerly Norclifl'e), the gneiss is very distinctly foliated, the strike being about S. 55° E., the dip S.W. < 10° to 20°. The thick massive bands in the high bluff to the north of the railway terminus, repre- senting the more acid portions of the rock, are granitic both in appear- ance and composition. Felspais, both reddish and grayish, are present as well as quartz, and a very sparing quantity of mica. The quartz, besides being present in grains and areas distributed throughout the rock, also occurs as veins and masses, evidently representing the most acid form of the prevailing pegmatite. On the north-east shore of the largest island of the group, situated about a mile east of Kippawa post-office, are good exposures of light-gray and pinkish-gray quartzo-felspatliic gneiss, alternating with darker bands which contain hornblende in addition to the more usual biotite. The strike is east-and-west, with dip to the south < 35° to 45°. Along the shore the basic bands have been weathered out more easily than the acid ones. Further to the south-east, toward Jeanbeau Bay, the gneiss varies in strike from S. 50° E. to S. 60° E. with a dip to the north-east BARLOW ] LAKE KEEPAWA. 211 I < 20° to 30'. North of Gordon Creek, the foliation of the gneiss corresponds rather closely with the trend of the shore-line, dipping to the north-east at varying angles. At Ureenorton Bay the schistose gneiss is very basic and contains hornblende in addition to the biotite. This rock also holds garnets and vein like bands of smoky quartz. At the font of Gibson Bay, the gneiss is of the common light-grayish granitite variety. On the south shore of Bryson Island, there ar*> good exposures of a light-gray granititegneiss, the foliation being much contorted. Beavais Narrows cuts the foliation of the gneiss at a considerable North of angle, the strike being S. 65'^ E. with dip to the north-east < 15° js'arrows. to 2.5". On the south shore of Smith Ba}-, exposures of hornblende- granitite-gneiss show the constituent felspar much decomposed and a large part of the biotite altered to chlorite. At Fowler Point, a knoll rising about forty feet above the surface of the lake is com- posed of a fine-grained almost black quartz-mica-diorite. This rock contains irregular patches and stripes of a much more acidic gneiss, light llesh-red in colom", which .seems to contain felspar, quartz, biotite and garnet, with occasionally some muscovite and epidote. Near Edward's depot, on the north shore of Smith Bay, the granitite-gneiss is as a rule very acidic, containing only small quantities of biotite. At Somerville Point, the gneiss is a reddish granitite much weathered and showing what appeared to be a very p^^•^^^ local strike of N. 40 E. The south-west shore of the lake opposite Sunnyside post-office is composed of i-eddish granitite-gneiss, generally striking with the trend of the shore, but sometimes showing many local twistings. At Turtle Portage, the usual granitite-gneiss shows a beautiful curve in the foliation, the strike gradually turning from N. 80" E. to S. CO' E., with a prevailing southerly dip. At Hunter Lodge Narrows and on Hunter Lake the gneiss strikes about S. 60' E., dipping in a southerly direction. Along the south .shore of jNIcLaren Bay, the gneiss is usually of a Gneiss of light-gray colour, rather fine-grained, micaceous and granitic in |j,^y '"®" appearance, being tinged with iron-oxide. It usually shows a distinct though imperfect foliation on account of the comparative scarcity of bisilicate material. The strike is N. 82" E. and the dip to the south. Microscopically, this is a typical holo-crystalline granitic rock or granitite-gneiss, consisting essentially of orthoclase, quartz and biotite, with apatite-zircon, sphene, a very little magnetite, much microcline and some plagioclase, (oligoclase) small quantities of secondary musco- vite and epidote are also present. 14^ At Somerville ill..: '! V ! :: :i li .11 ' R I V m '1 f :! *l V £xi>o«urea near McKen- zie iHliind. Gneiss at Campbell Bay. On Karl Island. m^i Porphyritic diiirite. 212 I NIPI8SIN<; AND TEMI8CAMINO KEGIOX. At the south end of an island immediately east of McKenzie Island, there are exposures of the ordinary llesh-red granitite-gneiss. On the north-west shore of McKenzie Island, the hornblende-granitite-gneiss seems to change in strike from N. 20° E. to N. 50' E., thus conform- ing with the trend of the shore-line, while the dip is to the south-east at varying angles generally about 00\ At one point a vein of (juartz (pegmatite) varyiiig in width from six inches to two feet cuts the gneiss, of which it contains fragments. The gneiss here is well foliated and often locally twisted. The gneiss composing the cliffs on either side of the "Canal," contains a considerable quantity of quartz and is much weathered and stained. It has a strike of N. 65^ E, with southerly dip < 80'. At the south end of Campbell Bay, the strike of the gneiss is north G2° east. A thin section of a specimen obtained from the western shore, about two miles south of the entrance, repre- senting the most basic bands, showed the rock to be a quartz-mica- diorite-gneiss. The rock is nearly Vjlack, very evenly and distinctly foliated and exhibits glistening cleavage-surfaces along the planes of foliation. Exceptional bands are of light pinkish-gray colour, felspar being the predominant constituent. Microscopically, this rock is composed of plagioclase, orthoclase, microcline, quartz, hornblende and biotite, with epidote, sphene, apatite, zircon and some pyrite, more or less altered to limonite. On the west shore of Karl Island, as well as on the island lying to the south-west, the gneiss shows the usual variation from grayish to reddish, with interfoliated darker bands in which the biotite is more abundant. The strikes vary from N. 64' E. to N, 67° E., with dip to the south < 60° to 70°. xVt one place on the north shore of the lake, half a mile north of the north-east point of Karl Island, a very ma.ssive and coarsely crystalline porphyritic diorite, is associated with the ordinary grayish granititegneiss. This rock is of a dark-green colour when fresh, but near the surface is decomposed for a depth of nearly two inches, the decomposed layer being much lighter in colour. Large phenocrysts of deep-green hornblende, some of which are an inch or more across and most of which possess tolerably well defined crystalline outlines, are developed in a coarse-grained groundmass composed almost wholly of allotriomorphic individuals of dark-green trichroic hornblende, the small and irregular interspaces being filled with felspar and quartz. Much of the hornblende includes dark schillerization products. The decomposed layer near the surface shows the somewhat abundant development of epidote at the expense of the hornblende, giving the prevailing yellowish-green colour to this portion of the rock. The MATTAWA RIVER. 213 I whole exposure measures about fifteen yards long by twenty-five yards wide and is surrounded by tlie grayisli granitite-gneiss, wliile several dyk^'s of pegmatite varying from a (juarter of an inch to six inches in width cut the diorite. In the northern portions of Hay Baj', the prevailing rock in the Hay Bay. oidinary granitite-gneiss, the strike of whicli varies from N. GO E. to N. 70- E. Rocks on Sandy Port- age Bay. The rock exposed on tlie shores and islands of the bay running towards the outlet, the north-western portion of which is generally known as Sandy Portage Bay, is the usual reddish and grayish biotite- granite-gneiss or granitite-gneiss. The strike varies in general from N. 50' E. to N. 60° E., while the dip is to the north-west at high angles, generally varying from G5° to 85°. Near the outlet, the strike turns more to the north, the foliation in this vicinity running about N. 40' E., while the bands are nearly if not quite vertical. At one or two points extremely basic portions of the gneiss were seen to be highly hornbleiidic, thus passing into quartz-mica-diorite. Mattawa River. The term I^Iattawa was first applied to the confluence of this Q|,j^rjjgtpf qJ river witli the Ottawa. The river has also been known as the Petite Mattawa Kiver. or Little l^iver, wliile to the Indians it was formerly known as the Tessouacsipi. It is really a succession of large deep lakes united by comparatively narrow and shallow rocky stretches. The total distance from the Ottawa to the western end of Trout Lake, in a straight line, is about thirty-six miles, but following the river this is increased to forty miles. The direction is in general nearly east-and-west, following a continuation of the main valley occupied by the Ottawa below the con- tluence of the two streams. In ascending the jNIattawa, rapid water is encountered almost at once, the stream ilowing over a shallow bouldery bed. This, together with a small rapid, a little over a mile above at the outlet of Boom Lake, gives a fall in the river of about two feet. Boom Lake, the first expansion reached, is only about a mile and a pyoin and Plein lakes. quarter long, and not over a quarter of a mile at its greatest width. I'lein Chant At the upper end of this lake, the river is contracted in two places to a width of less than a hundred feet and a fall of nearly twenty feet is occasioned by the Plein Chant Rapids. Plein Chant Lc*ke at the head of these rapids, is five and a half miles in length. The widest portion is near the eastern end, where it is about thirty chains, but this gradually diminishes westward, till, near the upper end it is not more Ranidx aiMi Liic (U's Aiguillt'M. Series i)f raiiids tn Fimisi Lake. Talon Chflte. 214 I NIPI8SIN0 AND TEMISCAMIVO REOIOX. than three or four chain.s wide. In the widest portion a depth of over two hundred and eighty feet was found. Between this lake and Lac des Aiguilles, the next expansion, the distance is a little over two miles, and four rapids intervene, with alternuting stretches of still watiw' ; the combined fall is eighteen feet. Tlie three largest rapids ate known in ascending orilei' as Les Epine.s, La Rose and Des Roches or Des Aiguilles. The Amable du Fond Jiiver, the largest tributary of the ^fattawa, enters from the south side a short distance above the second rapid. Lac des Aiguilles, which is a little over a mile long and a (juarter of a mile wide, is separated from the next succeeding stretch of river, lying parallel to it on the north side, by a rocky bar known as Ties Aiguilles Islands. The three narrow rocky ciiannels formed by these two islands, even at high water, barely afford a passage to loaded canoes. The eastern one constitutes the main route, and a small rapid at this point shows a descent of a few inches. Above tliis is a long stretch of deep water that gradually diminishes in width. The river throughout this distance of two and a half miles is flanked on either side b}- almost perpendicular walls of gneissic granite. At the end of this stretch, the upward course of the river changes sharply to a southerly direction for about two miles, and presents a .series of rapids with intervals of deep water, the total fall being fifty- five feet. The Chute des Paresseux, where the water falls thirty-four feet, is the first and largest of this series. Pimisi or Eel Lake (some- times also called Penice Bay and Moon Lake) above these rapids, marks another change in the course of the stream, which from this place to the head of Talon Lake trends north-westerly. Between Pimisi Lake and Talon Chute, the river flows for three-tjuarters of a mile through a narrow rocky caiion inclosed between perpendicular walls of granite. Talon Chute is the greatest single fall on the 'VNole river, the water descending forty-three feet over a rocky ledge oouipused of massive Hesh-red gneissoid granite. The main channel is r a the north side, but in addition, there is another though much smaller parallel pass- age. The downward extension of this passage is continued in a deep gorge which connects with the main channel a short distance lielow the falls, tlie whole apparently representing the erosion of a band of crystal- line limestone that here occurs. About half a mile below Talon Chute, a small rapid occurs with a descent of less than a foot, and a short dis- tance above it is Talon Lake. To the left, on entering the lake, a large bay runs westward for about three miles, Kabiskaw Bay at the western extremity of which an important tributary (Kabiskaw Creek) BARLOW ] MATTAWA IMVEU. !15 I onters, foriniHg the outlet of Nasbonsing Luke, a large ami irregular sheet of water situated in the southern part of the township of Ferris. Talon Lake lies north-west and south-east, ia about seven miles long TiUoii Luko. and has in general a breath of almost three(|" irters of a mile. The sliores are generally bold ami rocky, although occasional small sandy llats occur. The general depth may be said to vary from fifty to one hundred feet, but in occasional spots a depth of two hundred feet and over was met with. The connecting stream between Talon and Turtle or Lower Trout 'Pal"ii to T\ir- Liike, the next expansion in the river, is about four miles. The stream leaves Turtle Lake about a mile fron: the eastern extremity. It is shallow, rocky and rapid with some small intervening ponds of deeper water. Turtle Lake lies nearly east-and-west and is about four and a half miles in length and not more than half a mile in width. Thence iui ascent of barely a foot occui's, in a short channel, l^ Trout Lake, at Trout Lake, the summit. This is eight and a half miles in length with a greatest breadth, near the upper end, of about two nules. It is often over 200 feet deep, and the shores are rough and rocky. To the north of the lake, a range of hills from three to four luindrod feet high extends with almost unbroken continuity to the mouth of the Mattawa River and tlu'i.ce northward and north-westward up the valley of the ()ttawa. Tiie extreme west end of Trout Lake is only about three miles distant Route thence from Lake Nipissing, and the neck of land separating the two lakes is j,';',,^,'^ " ^ ''' in general very level. The canoe-route usually followed to Lake Nipissing, leaves Trout Lake in a bay running to the south near its western end. The first portage runs over a ridge of sand. The Riviere do la Vase is then utilized all the way to Lake Nipissing, a distance of a little over six and a lialf miles. This small stream runs through low and often marshy ground most of the way, entering Lake Nipissing about six miles south-east of North Bay. The land in the immediate neighbourhood of the ]\Lattawa River ciiiinicter is generally rocky, barren and unfit for agriculture. A short distance "f ''^"*'' from this river, however, in the townships of Papineau, Calvin, Banfield and Ferris, considerable areas have been cleared, and good progress has already been made in the settlement of these townships. The rocks exposed along the Mattawa are for the most part massive Kocks seen reddish granitite-gneisses, the strike of the folation running in a series "'""I? the Mat- . . ... tawa. of widely undulating curves in a general east-andwest direction with a prevailing southerly dip < 35° to 65^. Crystalline limestone is Liinestones. very sparingly present in association with these gneissic rocks, and ''^il 216 I NIPISSING AND TEMISCAMIXf REGION. i m ' '■:? Gneiss of Trout Lake. Size and fdi'ii, of LakeNii)is sing. Elevation. Coasts and islands. wherever noticed the evidence seemed to show that it has been caught up in the gneiss during the irruption of the latter. On the .south shore of Talon Lake, as well as in tlie southern channel at the fa,ll.s, at the outlet of t( s lake, the crystalline limestone was found in association with a very massive indistinctly foliated granitite-gneiss, the intrusion and later age of the latter being apparently clear. Near the western end of Nasbonsing Lake, the rock is a light-reddish granitite-gneiss com- posed chiefly of felspar, with a small proportion of giayish quartz and a little black mica occurring in isolated areas of aggregated scale.s, together with numerous small garnets. The striks is to the north-west with a dip to the south-west, generally at a high angle. Near the eastern end of the lake, the gneissic rocks present are more highly dif- ferentiated and occur in irregular curving bands which have a general strike curving gradually around from east to north-east. On Trout Lake, the granitite-gneiss occurs in reddish and dark- coloured bands which have a prevailing direction of nearly east and- west, gradually bending round to the north-west in the western part of the lake, while the dip is to the south < 45° to o5'. Lake Nipissing. 1 This important lake has an ai-ea of 345 square miles, and is wholly surrounded by Laurentian rocks. Its main length is east-and-west, and its greatest length, from the shore at East Bay, near Callendar station to the western end of Bear Bay (west arm), is sixty miles ; while the greatest width, from Beaucage Bay on the north to the moutli of the South River, is sixteen miles. The elevation above sea level, at different seasons, varies from 642-2 to 649 '5 feet. The northern and eastern shores are in general low and for the most part present sweeping beaches of sand, separated by rounded points of rock. The water, for a considerable distance from the shore, is shallow. The west end of the lake has an irregular coast line with long arms and bays extending and rocky islands. A great number of these islands strew the more open water outside, running in long lines, more or less parallel in direction with the peninsulas or points which divide the bays from one another. The islands, generally small, are sometimes several miles in extent. The southern shores arc bold and rocky and the water is deep even in their immediate vicinity. The whole of the eastern end of the lake is wide and exposed, con- taining only two small groups of islands known as the Manitou and Goose Islands. •J LAKE NIPISSING. 217 I The weatern end of the lake consists of four principal bays or Bays at wost- arms, separated from one another by rocky promontories, their con- j.^j^^, tinuation towards the deeper water in the central portion of the lake being marked by the occurrence of long lines of islands and reefs. The most northerly inlet, McLeod or Goulais Bay, has an almost direct north-and-south trend. It is about four miles in length by neaily two in breadth and lies immediately west of the marshy delta of Sturgeon River. The water in this bay is very shallow. A rather narrow and crooked channel, however, exists near the eastern shore, but is navigable only for very small steamers or tugs. Immedi- ately south-west of this bay and separated from it by the rocky peninsula ending in Goulais Point, is another arm of the lake, divided to the west into two subsidiary bays, known as the North-West Bay and Middle West Bay respectively. North-West Bay is over four miles in length, with a width rarely exceeding a quarter of a mile, and having the general direction indicated by its name. Gradually taper- ing westwards, it receives a small stream that drains some marshy lakes situated in the north-western part of the township of Macpheraon. Middle West Bay is much less important, being only about two miles in length, and at the west end receives a small tributary known as West River, that drains the southern part of the township of Mac- jiberson. Of the indentation extending to the west, however, the largest is West arm or known as the West Arm or Bear Bay. The general trend of this extension is nearly east-and-west. An inspection of the accompany- ing map will convey a good idea of the close depcmdence of topo- graphical outline on the strike of the foliation of the inclosing gneissic rocks. In many instances abrupt changes in direction are irrep ilar encountered, but these follow correspondingly sharp curves in the f'"'"' lines of foliation and cleavage. The width ot (he bay i ■ very variable, alternately contracting into narrow straits only a few chains in width and opening again into wide expanses generally crowded with islands. T.n the eastern portion for a distance of nearly eight miles, the average width is nearly two miles. The bay gradually nairows towards the west end where it receives the waterc of a small stream, draining several important expansions to the west. Several important streams enter Lake Nipissing. The largest is Streams enter- the Sturgeon River, draining about 3000 stjuare miles of country to '"*'' ''^'^ '*'^''' the north and west, and joining the lake in the midst of a large marsh on the north side. This low tract of land, forming a delta, has be< n produced by the gradual accumulation of detritus brought down 'y the stream. <■*■- 1 '!' I ( ;'i 'ill; .1: V 218 I NIPISSING AND TEMISCAMINO REGION. ; I ■: ) ■ Little Star- The Little Sturgeon or Silver River, enters the Great North Bay *^^°"' with a swift and deep current, being navigable for canoes, without interruption, for a distance of a little over two miles from the lake, where the stream becomes very small and rapids occur. The general course is at first nearly north, and the upper course i.s nearly north- east, to its sources in the southern part of the township of Blyth. Duchesney and Ohippawa creeks enter the lake in the vicinity of North Bay. The Riviere de la Vase or Little jNIattawa, flows into the lake about five miles south-east of North Bay. Other important tributaries enter the lake from tLa south, but these are beyond the V.'uve River, boundaries of the present map. The Veuve River is an important stream which enters the west side of McLeod Bay, draining a large tract of land, the .sources extending westward almost to the Wahna- pitae River. Several important islands and groups of islands occur, lying out towards the middle of the wide eastern portion of the lake. The most important of these is the group named the Manitou Islands. These are five in number, situated five miles south-west of North Bay. The largest is known as the Great Manitou or Newman Island. It is an irregular triangle in form and about a mile across. McDonald Island, the ne.xt in size, is about half a mile in length from north to south but only a few chains in width. The other three islands are much smaller. Goose Islands. The Goose Islands lie toward the centre of the open part of the lake, about six miles west of the ^lanitou Islands, and about twelve miles west-south-west of North Bay. The largest island is known as the Great Goose, and is nearly a mile long with a trend of east- and-west. To tlio west and north-west of these there are aVjouc a dozen smaller ones, some of which are merely rounded hummocks of rock. Manitou Islands. Country and rocks of west end (if lake. The general aspect of the western end of Lake Nipissing is rocky and desolate. In many cases the sparse soil overlying the rarely concealed hummocks of rocks, atlbrd substance to a rather thin and scrubby growth of red pine, while the level spots are for the rao.st part occupied by vast marshes, but some snniU tracts of level land occur along the banks of some of the tributaries, notably the one situated on the south side of Bear Bay near its entrance. The northern shores of the lake, however, border large areas of cultivable land. The rocks are generally well exposed, especially in the western and southern portions of the lake. They include the prevailing varieties of granititegneiss and hornblende-granitite-gneiss, the former ii|>^ •] LAKE NIPISSING. 219 I m being the prevailing type. These are cut by dykes and masses of peg- matite presenting the usual characteristics. The Manitou Islands are composed of a rock which is remarkably Kocks of the uniform in composition and appearance, being a medium-textured jsjands? reddish gneiss, that has evidently been subjected to intense dynamic action. It has a rather indistinct blotchey appearance, due to irregular bands of chloritic and epidotic material running through it, resulting from the alteration of the bisilicates. The micro- scope shows that the rock has everywhere been greatly granulated. Its chief constituents are quartz, orthoclose, plagioclase, hornblende and biotite, with epidote, chlorite, calcite, sericite, iron ore and apatite. It is thus a hornblende-gninitite-gneiss which has suffered great alteration, the felspar being turbid and full of inclusions of sericite, calcite, etc., resulting from its decomposition. Numerous irregular patches of calcite are scattered through the section. Both felspar am^ c^uartz extinguish very unevenly. Hornblende is the^most aba/i'! lilt iorri)magnesian mineral present, but it has suffered such extreme alteration to chlorite and epidote as to mask its true char- acters. Biotite, largely altered to chlorite, occurs intergrown with the hornblende. The section is traversed by numerous cracks tilled in with secondary quartz, epidote, iron oxides, etc. On several of the islands, this rock, which has evidently resulted Crystalline from the crushing of a hornlilentle-granite, contains large patches of ''•"'^'^'^o"^* pinkish crystalline limestone ; the latter, however, doubtless represents portions of the clastic Grenville series. The gneissic rocks are inter- sected by dark-greenish dykes of basic material previously described in that portion (■* the report treatin^^jf post-archiean eruptives. On several islands ujuil onMiers of the iiirds Eye and lilack lliver formations are exj.:.,'sei!, as elsewlnu'e noted. liock cxposi'V- .liT abundant on the Goose Islands, showing a Hocks of medium-grained red .granitic gneiss. The foliation is determined by """"" '''*"'*' the parallel arrai geuient :.i the little bands of biotite. The principal constituents are (iiartz, orthoclase, plagioclase, microcline and biotite, with small quanMties of apatite, zircon, chlorite, epidote, sphene, calcite and secondary iron ore. It is one of the typical biotite- Constituents gneisses or granitite-gneisses of the region, evidently resulting from "f *'"^ k"i''»*'- crushing and ilifferentiation of a granitite. The felspars are exceed- ingly turl)id, 5.iJ^"* grey slates, while the north-eastern shore in tliis dircctitjn is low and l-akc covered with thick green bush. About a iin'le and a quarter north of the outlet, the slates are overlain in conformable sequence by the yellowish- green quart zite-grit, the whole having a north-westerly dip < 5° to 12\ The slate as usual shows a gradual transition througli a more massive slate into a grcywacke or felspatliic sandstone, which merges upward into the comparatively coarse-grained arkose sandstone or quartzite- grit that rises into hills varying from 250 to 300 feet above the lake, in places forming precipitous cliffs of considerable height. A specimen of this rock was examined by the late Prof. G. H. Williams LitlioUwical and was taken to represent the transitional portion near the immediate fjiaract^ r uf ^ ' the sliitr. junction between the coarse greywacke and the quartzite or arkose. The small hand specimens showed a banded coarse and fine conglomer- atic sandstone or greywacke. The coarser portion of the specimen presents the ordinary characters of the prevailing quartzite-grit, liolding good sized fragments of (juartz both angular and rounded in outline, embedded in a moderately abundant sericitic matrix. The finer-grained portion, which has a somewhat darker hue, is a rather typical greywacke, showing " an aggregate of angular and sub-angular quartz grains with some felspar. Betsveen these grains much chloride has been developed, which, together with the magnetite present, gives the dark colour to this layer." 15 !:i 1 i l: ;ll 226 I NIPISniXG AN'D TEMISCAMING HEfJION. Quartzito and eke. Dialmso of Fort ago Bay. Bay Lake to Mountain Lake. This quartzitp, as usual, occurs in very tliick find massive beds and the dip cannot be nia'Io out with any certainty e.xtept in a few places. It is exposed all along the suuth-west shore of the lake as far as the inlet and forms the south-western portion of the puint that separates Portage Bay from the main body of the lake. Fuither up the river this rock is underlain, first, by a massive brownisli greywacke orslatf, exposed a short distance below Pork Rapid, and next, in descen'ling order, by the well banded greenish slate.s, dipping 8. 55° E. < 10' to 15°, which continue as far as and a little beyond the inlet from Laily Evelyn Lake. Tlie .structure is therefore tiiat of a somewhat shallow syncline, the basal bed being represented both by ihe banded slates exposed in the south-eastern part of Uay Lake and thosci occurring in the vicinity' of the outlet from Lady Evelyn Lake, the overlying quartzites resting in the trough thus formed. The point on which Bay Lake post is situated, is composed of coarsely crystalline diabase or gabbro, the felsj)ar frequently possessing a distinct flesh-red colour. The massive and rounded exposures of this rock are cut by irregular ramifying dykes, composed of a fine-grained pale-grayish or pinkish aplite. This basic irruptive forms the shores of Portage Bay, as well as the north-eastern part of the point separating this bay from the main body of the lake. To the northwest of the lake, it continues for a considerable distance inland, forming a series of high, though i-ounded hills in this district, while to the east, as far as can be learned from the occasional outcrops, it is continuous with the mass which forms the southern part of Sharp Lake extending as far as the western shore of Lake Temiscaming. Between the head of Bay Lake and the head of Lady Evelyn Lake (Mattawapika), the river is in general a line, wide stream, with occa- sional short stretches of swift current. Pork Rapid (Kokooshbuwatik), has a total fall of nearly seven feet, the portage being on the south- west bank. The north-eastern banks of the river are low, and the country for many miles is flat and swampy. On the south-east side in that direction there are only occasional low rounded exposures of the greywacke and slate, and these are situated some distance away from the stream, forming a series of rounded hills. Between the Mattawapika and Rounder Mountain Lake the river is, as a rule, wide and navigable, with only two interruptions by rapids One of these is a little over a mile and the other about four miles below Round Lake, the portage in both cases being on the northern or north- eastern bank of the river. The combined fall of these two rapids is about eight feet, the upper one being the larger with a descent of five feet. "^ lARLOW. J THE MONTREAL UIVEK. 227 I S The shores in the vicinity of the Mattawapika, show exposures of a well banded slate which dips S. 55" E. < 10' to 15", and Cdntinueb for ahout a mile above this f)oint, where it is interrupted by a mass of diabase or gabbro, which, on the south-east side, rises into a series of precipitous hills. This rock may extend across the stream to the northward, but any hills on this side are much lower and less pro- nounced, and are therefore more likely to be underlain by the gray- wacke slate. This mass of diabase extends to within a ([uarter of a mile of the outlet from Mocassin Lake, and is an extension northward of the mass of similar rock which forms the western shore of the last stretch of Lady Evelyn Lake. To the north-west, this diabase is replaced by the (juartzite grit or ai-kose which forms smaller and less conspicuous eminences extending northward and inland for some miles ; while to the north-west, the general surface outline would seem to indi- cate its continuous presence as far as the south-eastern extremity of Indian Lake, although no exposures could be seen. The rock is the u> between lakes Temiscaming and Temagami. Its head-waters lie to the north and west of White-bear Lake. The smallest branch takes its rise in Caribou Lake, on the main canoe-route, within a (|uartcr of a mile of the north-east arm of Lake Temagami, and this small lake sends another and larger stream into Lake Temagami. The largest or main branch of the river rises in Mountain Lake, to the south-east of Annima-nipissing and Bay lakes. Two other branches of some size drain lakes that lies close to the hills bordering the lower stretch of the Montreal River, debouching in the north-eastern corner of White-bear Lake within a short distance of one another. From the mouth on Lake Temiscaming to Mountain Lake, the dist- ance, in a straight line bearing N.70' W. is nineteen miles, while follow- ing the general canoe-channel, this distance is inci-easedto tliirty-seven miles. This whole space is divided into two main directions of How, forming an angle of 70' with one another, these constituting two sides of a triangle, while the third has the length and direction already men- tioned. The tirst of these stretches, which extends from the mouth of the river to Rabbit Point on Rabbit Lake, has an upward bearing of S. 44"^ W. for thirteen and a half miles, although the channel usually iUld iHllllcllf liDwer i>art of Matabit- «houan . ¥' ■] THE MATAUlTCilOUAN UI\ EH. 229 I Lnivclled measures about sixteen miles. Tlifl third side of tlie triangle, wliicli reaches from Ilabhit Point to Mountain Lake, shows a •,'('n('ral direction of M. 20 W., with a lfn;,'th of nineteen miles, although the most direct canoe channel measures about twenty-one miles. From the mouth of the Matabitchouan to the tirst portage, the river has cut a fairly deep channel throuijh drift material, the bands on either side l)('i i|)osed of a stratified gray clay. The strength of tiie current ill I .nterval varies with the height of the water, for during times of freshet, the water of the lake backs u|), forming a comparatively deep channel to within a short distance of the tirst portage ; while, during (iidinary stages, the stream has a swift current almost to the mouth. The norihern banks are as a rule much lower than those on the south side of the stream. A short distance south of the river is a high and Hi'iiver prominent hill, known us the King of the Beavers, also sometimes cal- led the Montreal Mountain or Beaver Mountain. Acconling to baro- iiuarical observations, this hill has an elevation of GGO feet above Lake Ti-miscaming, or 1248 feet al)ovo the sea. The sunmiit of Beaver Mountain, for 340 feet, is composed of a | ,,,|.^ fmnid •'reenish-grey medium textured diabase, much sheared anil broken, ''1 1'":'^''.''' ° ^ . . , . Mountain, the pi "es of shearing being abundantly coated with greenish decom- posit >roducls. Below this rock is a gi-eenish slate, which marks the 1 tnd more gradually sloping portion of the mountain. The strike of the slates curves around, conforming beautifully with the line of outcrop of the diabase, dipping into or beneath what seems to be an irruptive mass of lacolitic origin. The first, or Matabitchouan portage, occurs a little over two miles Matahit- frum the mouth of the river, where a series of rapids and falls occur ^g|!. ' with a descent of 200 feet. The stream here describes a sharp bend to the north, while the portage, to overcome these obstruc- tions cuts, across the bend thus formed, running over a hill, the high- est point on the trail being 330 feet above the level of the river at the foot of the portage. The ascent of the portage is steep, passing iirst over stratified gray clay, and clay and b(julders, but near the summit it is rocky. This is the breccia-conglomerate, containing pebbles chietly of a flesh-red granite embedded in a dark-green chloritic matrix. The west end of the IMatabitchouan portage comes out on the first of a series of four Bass lakes, i^urabered in ascending order. These are s'nidl expansions, united by narrow shallow channels, with an appreci- able current. The south-east shore of the Second Bass Lake, consists of high per- Soconci B