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GEOLOGICAL SURVEY I MEMOIR 76 I No. 62, Geological Series Geology of Cranbrook Map -Area, British Columbia BT Stuart J. Schofleld OTTAWA GOVBBNMBNT PUHTING BuRBAU 1915 No. 1505 Mk I MfU>T^ ofCrnobt C VLANATION or PlaTK I. Morning on the Goat river. ^r%f^. •,:'■*; : .1 dlhll':^) ■AOnkCAJHiS'^' .Tjvh t«>0'-'.ij|, aa, jc*; i— l^ 1^ i'i^«w^-«it,*'u.Tnj > CANADA DEPARTMENT OF MINES Hon. Louis Coderrb, Minister; R. G. McConnell, Deputy Minister. GEOLOGICAL SURVEY i MEMOIR 76 I No. 62, Geological Sbues Geology of Granbrook Map-Area, British Golumbia Stuart J. Schofleld OTTAWA GoTBunaiTT PiiimMO Buuau 1915 No. ISOS 1=1 CONTENTS. CHAPTER I. PAOB Intraduction 1 Gencfal itateiiieiit 1 Field work and acknowtedgmenta 2 Location and area 2 Meana of communication 3 Previoua worketa 4 BibliogFaphy 6 CHAPTER II. General character of diatiict 8 Topography g Regional 8 Local 8 Fauna and flora 14 Climate and agriculture 15 Temperature, precipitation, and altitudea 15 Irrigated and irrigable areaa 16 CHAPTER III. General geology 19 General statement 19 The Purcell leriea 23 General statement 23 Aldridge formation 25 Distribution 25 Thickness 26 Lithology 26 MetamorpUam 27 Structure 28 Creston formation 28 Distribution 28 Thickness 29 Lithology 29 Metamorphiam 30 Structure 31 Kitchener f(Hination 31 Distribution 31 Thickness 32 Lithology 32 Structure 33 u PAOK Siyeh formation 33 Dictribution 33 Lithology 34 ThkkneM 35 Structural relation* 35 Gfttcway formation 34S Distribution 36 Lithology 36 ThickncM 37 Structural relations 37 Origin of the Purcell series 38 Sources of the sediments 40 Purcell sea 40 Age and correlation of the Purcell series 41 Gateway formation 42 Phillips formation 42 Roosville formation 42 Burton formation 43 Age of the Burton formation 44 EUco fMmation 47 Age of the Elko formation 47 Jefferson limestone 48 Unconformity at base of Burton 48 Relation of Gallon series to Purcell series 49 Con vlation of Purcell series and Coeur d'Alene series.... 51 Pslcosoic foraiations of Purcell range 53 General statement 53 Jefferson (?) limestone 53 Distribution 53 Thickness 53 Lithology 53 Relation to older formations 53 Age and correlation 54 Wardner formation 55 Distribution 55 Thickness 55 Lithology 55 Relation to older formations 55 Relation to younger formatiocs 55 Age and correlation 56 Pureell sills 56 Distribution 56 Lithology 57 Gabbro 57 Variations in the gabbro 59 iii PAta Qiuuts-dkrite or tnuitioB nwk 62 Granite 63 Internal relation* 65 External relatiotts 66 Summary of contact metamorphitm 68 Age of Purcdl nib 68 Rdationa of Purcell nil* to Purcell wriea 68 Relation* of (ills to Purcell lava 69 Age of Purcell lava 69 Correlation 70 MetamorphiHn 70 Structure oftheall* 70 Moyie ailb 70 St. Maryaill* 74 Summary of geneais 75 Purcell lava 76 Diatribution 76 (ithology 76 Thickne** 77 External relation* 77 Age 78 Gfanite* 78 Distribution 78 Lithology 80 Structural featurea 82 Age and correlation 84 Superficial deposit* 85 Pldstocwfie deponts 85 Focal content of the St. Eugene silt* 87 Age and correlation of the St. Eugene silt* 90 CHAPTER IV. Structural geology 92 Folds 92 Faults 93 Age of faulting 95 Regional structure 95 CHAPTER V. Geological history 98 Introduction 98 Beltian sedimentation 98 Aldiidge epoch 98 Creston epoch 99 iv Kitchener epoch ^ siyeh epoch !!.!!!!!!!!!!!! 99 Purcell lava !.......!........ 99 Gateway epoch !!.!!.!!."!. 99 Phillipe epoch 100 Roocville epoch ...".!!.!!.!!. 100 Cambrian !.!."!!.!!!!. 100 Devonian-CarboniferoiM epoch *" inn J"«^ '.'.'.'.'.'.'.'.'.'.'.'.["'.['.[['.'. 101 101 102 102 103 Late Juraisic or early Cretaceous. Cretaceous erosion Tertiary Quaternary CHAPTER VI. Economic geology Mineral production of East Kootenay !!....!...!. Silver-lead deposits !..!."...!,.! 106 Distribution -qU 104 lOS 108 108 109 Mineralogy .q. Native elements ' ' |Qg Sulphides !!.!!..!!!!!! 107 Sulpho ivlta !!!!!!]!... lOS Oxides !............. Carbonates \'" Silicates !.*.'!!!" Phosphates !!!!!..! 110 Paragenesis ..!......,.,..,. HI Genesis of the dei osits * * " j < 9 Comparison with COeur d'Alenea 113 Correlation of ore deposits ug Age of deposits !.!!.!!.!!. 117 Future of the silver-lead deposits 117 Description of mines and prospects 117 Moyie area ] " j.y Geology ' " " j jy Fissure system j jg St. Eugene mine jjg Aurora group of claims 123 Guindon group of claims 125 Cambrian and Mabelle claims 125 tocJpfyGirl 127 Kimberley area 127 Location ' _ " j27 Geology '.'.'.'.'.'.'.'.'.'.'.'.'..'.'.'. 128 PAOB Chatacter of depotiu 128 Sullivan mine 130 North star mine 133 Stemwinder 135 MaKot and Edipw 135 Gold quartz vein* 13ur in the main valley o( St. Mary river Panorama of vicinity of Cranbrook The U-shaped valley of Baker creek Trough-shaped valley of Matthew creek Detailed view of a cirque Looking west up the St. Mary valley in the nughbour- hood of Marysville Alpine topography looking northeast from head of Hells Roaring creek Index map Natural section of the Moyie sill* Columnar section of the Moyie sills Natural section of the St. Mary sills Granite intrusbn on Helb Roaring creek. Detail showing intrusion methods Cross section along vein of St. Eugene, Cambrian, and Aurora mining claims Plan of 1,800-foot level, St. Eugene mine Longitudinal section along north or main vein of St. Eugene mine Plan of Aurora mine Longitudinal section of Aurora mine Plan of Moyie lakes, showing contour of lake bottoms Diagrammatic cross-section of Sullivan mine Diagrammatic longitudinal section of Sullivan ore-body Diagrammatic cross-section of North Star ore-bodies Planof Running Wolf mine. Perry creek XVIL XVIII. XIX. XX. XXI. XXII. XXIII. XXIV. XXV. XXVI. XXVII. XXVIII. XXIX. XXX. XXXI. XXXII. • XXXIII. Figure 1. • 2. • 3. • 4. ■ 5. • 6. • 7. • 8. • 9. • 10. • 11. • 12. • 13. • 14. • IS. vU raoB 199 199 201 203 205 205 207 209 211 211 213 213 215 217 219 221 221 223 225 227 229 231 3 72 73 74 79 118 121 122 124 126 129 131 132 135 139 Geology of Granbrook Map-area, British Golumbia. CHAPTER I. INTRC^iJCnON. General Statement. Mining was initiated in East Kootenay by the discovery of placer gold on Wild Horse creek near Fort Steele in the eariy nxties, and since then the district has advanced from the stage of uncertain placer mining to one of steady lode mining. Accord- ing to the annual reports of the Minister of Mines of British Columbia, from the time official records were kept up to the close of 1912, the Fort Steele mining division of East Kootenay^ has produced $20,212,709 in valuable metals, chiefly gold, silver, and lead. The principal producing mines of the district are the Sv'*ivan and the St. Eugene, while :he minor properties which ship occa- sionally are the Society Girl, Aurora, Stemwinder, and North Star. The study of the area embraced by the Cranbrook sheet was initiated in order to come to some conclusion as to the origin and possible future development of the ore deposits, so that prospecting might be directed in those areas in which the chance of discovery of similar deposits was the greatest. The examination of the great number of copper deposits associated with the Purcell sills proved to be not only of economic but of scientific importance. ' East and Weat Kootenay are now combined, and form the electoral dlviaion officially known as Kootenay. In this report the name East Kootenay dengnates the former dectoral division of that name. I I The placer depodtt which had been the iource of A« early wealth of Eait Kootenay. are now worked only "P*"^" cally and in a «naU way. M energy is now devoted to tode miidng. which early proved to be of great value in the industnal development of the region. » u • i, .«j CUy depoMts •uiuble for the manufacture of bncka, and other day products, are widespread in the Kootenay vaUey; while limestone for building stone and for the manufacture ol lime occurs in large quantities aroum* Wardner. Field Work and Acknowledcmbnts. The field work upon which this report is based was carried on during the field seasons of 1909. 1910. 1911. 1912. and part ol 1913. This length of time was necessary since the problems to be solved were for tiie most part regional, involving the «a™n»^ tion of a wide extent of territory in almost inaccessible districts. A reconnaissance of the western portion of the Rocky mountains was made where the Pre-Cambrian sedimentary senw (Galton series which are equivalent to the Purcell series) was m contact with the fossUiferous Palaeozoics. A comparative «tudy jwa made of the stratigraphy and ore deposiu of the Coeur d Al«e district of Idaho where the geological conditions are so weu The officers of tiie Consolidated Mining and Smelting Company. Limited, and die owners of mineral properties m the region, at aU times rendered every assUtance in tiieir power for the advancement of the work. . . n u The writer wishes to record his indebtedness to his fidd assUtants. Messrs. W. Galbraitii. L. E. Wright. P. P. Baily. T. L. Tanton, M. F. Bancroft, and G. Hanson. Location and Asba. The Cranbrook map-area (Figure 1) lies in soutiieMtern British Columbia and indudes part of botii the Fort Stede and N.'-on mining divisions. It is bounded on tiie south by tiie International Boundary line whidi separates it from Montana and Idaho. Ita eaatern border ia fonned by tht Kootenay valley or Rocky Mountain trench which alw con- ■titutea the eaatern lit t of the P>jrcell range. The northern limit of the area ia 49* 45' north latitude and iu western limit ia marked by longitude 116* 3(/ west. The total area enclosed is 2,535 square utiles. The chief town and distributing point of the region is Cran- brook (PUte XXVIII). NORTH AMENICAN «.ORDIUX«A Figure 1. Index map. Means of CouutnncAnoN. The Crowsnest division of the Canadian t'adfic railway passes through the area from Wardner to Kootenay Landing. Following the same route as the railway, p motor road forms a link iu the projected transmontane highway from Calgary to Vancouver. From Cranbrook, a branch line of the Canadian Pacific railway runs to Kimberley, the centre of the Kimberley mining area. From Yahk, another line diverges along the Moyie river and crosses the International Boundary at Kingsgate on its way to Spokane and Portland. The Great Northern railway entering Canada from Montana at Gateway on the International Boundary line, runs north along the eastern bank of the Kootenay river and taps the Crowsnest Pass coal- fields through the Elk River valley. The drainage area of the St. Mary river is accessible from Marysville by a wagon ro£id as far as the ranch of W. Meachen. From here, trails have been constructed up the main branches of the St. Mary river, the trails on the south and west forks of which cross the summit of the Purcell range and finally reach Crawford bay and Kootenay lake. From the foot of St. Mary lake, a trail runs up Whitefish creek to Sanca on Kootenay lake. A branch trail diverges from the Whitefish trail, goes up Fiddle creek, crosses the St. Mary rivei^-Goat River summit, and follows the Goat river to Kitchener on the Canadian Pacific railway. The country south of Cranbrook will be made accessible by a projected wagon road from Cranbrook to Gateway through the Gold Creek valley. A trail branches off from the road up the south fork of Gold creek, enters the drainage area of the Yahk river and descends the East fork of the Yahk river where it joins the Boundary trail which leads to the town of Yahk on the Crowsnest branch of the Canadian Pacific railway. All these trails although well defined and greatly used in the nineties, are now almost impassable because of fallen timber, which in the burned areas is especially troublesome. The Boundary trail which follows the International Boundary line as closely as the configuration of the country permits, in 1912 was utteriy useless on account of fallen timber. It seems a pity that a trail so well built and of such historic interest should be useless as a means of travel. Previous Workers. Bauerman,' who was connected with the International ' Bauerman, H., G.S.C. Report of ProgreM, 1882, p. 25 B. Boundary Commission of 1859-1861, gave the first account of the geology of the Purcell range in southeast Kootenay. He describes the very thick, well-bedded, non-fossiliferous rocks occurring along the Boundary line between the two crossings of the Kootenay river. From the ripple marks, sun cracks, and false bedding, he classes them as shallow water deposits and the presence of casts of salt crystals he explains by the evaporation of a shallow sea which had no connexion with the ocean. Associated with these slaty rocks, he notes the occur- rence of interbedded greenstones and amygdaloidal surface flows. Bauerman also describes the Carboniferous limestone occurring at Tobacco plains in the Kootenay valley and gives a list of the fossils found in them. Dawson' describes the limestone which occurs near Wardner as probably Devono-Carboniferous in age from its resemblance to the Devono-Carboniferous on Crowsnest lake. He noticed the abundant crinoid fragments in the limestone. In this report, he puts the slaty unfossiliferous rocks of the Purcell range in the Cambrian. From the fragments of lignite occurring in the Kootenay River valley, he outlines an area of Tertiary rocks; but work by the writer subsequently revealed the lignite in place, and definitely places the lignite as Pleistocene; hence no Tertiary rocks have as yet been found in the Kootenay River valley. In 1900, McEvoy' in a reconnaissance survey made a topographic and geologic map of East Kootenay. A description of the rocks and mineral properties is given. Daly' during the field season of 1904, made a detailed ' tudy of the Purcell range in the vicinity of the International Boundary line. He defined the sediments of the Purcell range as the Purcell series (the greater part of Cambrian age) and subdivided them into theCreston,Kitchener,and Moyie formations in ascending order. In connexion with this work in the Purcell ' Dawson, G. M., G.S.C., Ann. Rept. Vol. I, 188S, p. 148 B. » McEvoy, J., G.S.C., Summary Report, 1899, p. 87 A. • Daly, R. A., G.S.C., Ann. Rept., 1904, p. 91 A. — G.S.C., Memoir 38, 1913, pp. 119-138. range he also studied in soire detail the origin of the granite (micropegmatite) which occurs in the gabbro sills of that section. The various reports issued by the British Columbia Bureau of Mines conUin descriptions of the mines and mineral properties in East Kootenay. ^ , • i The reports of the officers of tiie Umted States Geological Survey, on the Belt formations in Montana and Idaho, were of assistance in correlation. BiBUOGRAFHY. Bauerman, H.-Geol. Surv., Can., Report of Progress, 1882. Pt. B. Burling, L. D.-Geol. Surv., Can., Mus. Bull. No. 2, p. 93. 1914. Calkins, F. C.-U. S. Geol. Surv., Bull. 384, 1909. Corless, C. V.— Jour. Can. Min. Inst., Vol. 5. p. 503, 1902. Daly, R. A.— Am. Jour, ^o., Vol. 20, 1905. Festschrift von H. Rosenbusch, 1906. Geol. Surv., Can., Summary Report. 1904. Geol. Surv., Can., Summary Report, 1903. Geog. Jour., Vol. 27. 1906. Geol. Surv., Can., Memoir 38, 1913. Dawson, G. M.— Geol. Surv. Can., Ann. Rept., Vol. I, 1885, Pt. B. Hershey, O. H.— Min. and Sci. Press, Vol. 107, 1913. MacDonald. D. F.—U. 3. Geol. Surv.. Bull. 384. McConnell, R. G.-Geol. Surv., Can., Ann. Rept., 1886, Pt. D. McEvoy, Jas.-Geol. Surv., Can., Ann. R^pt., 1904, Pt. A. Ries, H., and T" ele, J.— Geo. Surv., Can., Mem. 65. p. 65. 1915. Ransome. F. L., and Calkins. F. C.-U. S. Geol. Surv.. Prof. Paper 62, 1908. Schofield, S. J.— Geol. Surv., Can.. Summ. Rept.. 1909. Geol. Surv.. Can.. Summ. Rept.. 1910. Geol. Surv.. Can., Summ. Rept., 1911. Geol. Surv., Can., Summ. Rept., 1912. Geol. Surv., Can., Summ. Rept., 1913. Geol. Surv., Can., Mus. Bull. No. 2, p. 1, 1914. Geol. Surv., Can., Mus. Bull. No. 2, p. 79. 1914. Econ. Geol.. Vol. 7. p. 351. 1912. Science Conspectus, Vol. IV, p. 122, 1914. Scientific American Suppl. Vol. 79, 1915, p. 88. Umpleby, J. B.— Jour, of Geol., Vol. 20, 1912. Walcott, C. D.— Smith. Misc. Coll., Vol. 57, 1910. Geol. Soc. Amer., Bull. 17, 1905. CHAPTER II. GENERAL CHARACTER OF THE DISTRICT. TOPOGRAPHY. Regional. In the southern part of British Columbia the Interior Plateau region separates the North American cordillera in Canada into two main divisions, each of which, in contrast to the Interior Plateau region, is characterized by alpine mountain topography. Each division is subdivided into mountain systems which are separated from each other by well defined topographic features. The eastern division includes from west to east, the Colum- bia, Selkirk, Purcell, and Rocky Mountain systems. The Purcell range or system, that system which is mainly discussed in this memoir, according to D'ly is an elliptical- shaped group of mountains about 25*^ cs long by 60 miles wide, lying between the Selkirk ,-.em on the west and the Rocky Mountain system on the east. Most of this range lies in British Columbia, the remainder in United States. The Purcell system is separated -om the Selkirk system on the west by the Purcell trench in which occur Duncan river, Kootenay lake, and the north-flowing portion of the Kootenay river. From the Rocky Mountain system on the east the Purcell range is separated by the Rocky Mountain trench in which occur the north-flowing portion of Columbia river and a south-flowing part of Kootenay river. This latter river after flowing southwards into the United States swings through a semi-drcle, and with a northward course crosses the International Boundary line again and empties into Kootenay lake. This semicircular valley forms the southern boundary of the Purcell Mountain system. Local. The area embraced by the Cra"brook map area includes the central part of the Purcell range in southeastern British Columbia. In a view from one of the higher peaks in the western part of the range, the most striking feature is the accordance of mountain summit-levels, giving the impression of a deeply dissected upland surface with numerous projecting peaks of greater elevation and great trough-like valleys. On closer exam- ination of details, this imaginary reconstructed surface appears to slope gently towards the Rocky Mountain trench on the east, and to be modified by recent glacial action. Three types of topog- raphy can be recognized. In the neighbourhood of the watershed of the range, the region is mountainous and rugged (Plate V) many peaks exceeding 9,000 feet in elevation. Towards the east, in the neighbourhood of the Kootenay River valley, the mountains are more subdued in character, having rounded wooded summits (Plate II) and finally ceasing altogether where the prairie land (Plate III) of the Kootenay River valley is reached. This valley in the neighbourhood of the St. Mary river, is 16 miles wide. In the background (Plate IV) the Rocky Mountain system rises wall-like to a height of 9,000 feet out of the valley which here has an elevation of about 3,000 feet. In the central, alpine, mountainous region where the non-resistant rocks of the Kitchener formation outcrop, the waste covered slopes are gentle and more subdued than where the tough argillaceous quartzites of the Aldridge formation with their interbedded gabbro sills, are exposed. This difference in form of outcrop is a valuable aid in the field in distinguishing the formations at a distance. The form of outcrop assumed by tha Aldridge formation is well exhibited in the mountains north of St. Mary lake which occur in the axis of the anticline where the strata are almost horizontal. Here, the intercirque divides or arStes are saw-like in character and almost vertical. The alpine peaks have serrated summits and are subject to rapid erosion by the action of ice and snow. Valley head cirques or basins are very numerous throughout the mountainous district and are somewhat modified by the talus slof^^s which at times encroach upon the small urns, so characteristic of these glacial amphitheatres (Plate XXXI). One small glacier exists 10 within the confines of the Cranbrook sheet and is situated on a cliff above Hall lake (Plate VI). . To the east and southeast of this mountainous region 1mm the subdued mountain belt (Plates VII and VHD diaractemed by rinded hills rising to a height of 7.000 to 7.500 feet above sea-level, holding here and there small cirques which m this region are few in number and not very conspicuous. On the ndge south of Perry creek, there is still some of the old uplaad surface preserved (Plate IX). . «,^ . The entire drainage of the Cranbrook map-area is effected by the Kootenay river which rises in the north partly in the Rocky Mountain system and partly in the Purcell system. It flows southwards across the International Boundary Ime at Gateway into the United States where it pursues a semicircular course finally flowing northwards into Bntish Columbia where it empties into Kootenay lake at Kootenay Landmg. The Rocky Mountain trench (Plate IV). that great and remarkable longitudinal depression whose southern portion lies between the Rocky Mountain system on the east, and the Purcell range on the west, extends from the sUte of Montana to frintemational Boundary line between Alaska and the Yukon In the neighbourhood of the Cranbrook area the floor of this intermontie depression is a beautiful stretch of parW^e country 16 miles wide containing numerous open meadows, lakes, and the meandering Kootenay river. Rising abniptly from the valley floor, the western Rocky Mountain front forms L'aSem flank. In contrast to the w^-Uke character ^lU eastern border, the western flank is marked by rounded wooded foothills, which in turn give way to the rugged mountains of the Purcell range (Plates III and XXXII). The five main tributaries of the Kootenay nver draming the Purcell range in the Cranbrook map-area are the St. Maiy river. Gold creek. \ahk river, Moyie river, and Goat nver. Most of the streams tributary to the Kootenay river head in the numerous rock basins or glacial arques m the mountainous '^ The St. Mary river (Plates X and XI) carrying the drainage of the northern part of the area, rises on the summit of the range 11 in several heads, and flows eastwards into the Kootenay river at Fort Steele. In the upper part of their courses the tributaries of the St. Mary river flow over wide, rocky floors in trough-shaped valleys (Plates XXIX and XXX) ; but within variable distances from the St. Mary river (2 or 3 miles) they enter narrow box-like canyons where they plunge over falls from 50 to 75 feet in height. At these points they leave the hanging valleys of their upper courses and flow with decreased gradients to join the St. Mary river at grade. These lowest reaches are usually marked on either side by gravel cut-banks about 50 feet in height. Hanging valleys (Plates X and XXVII) characterize Whitefish, Hells Roaring, and Perry creeks which flow north into the St. Mary river; and Pyramid, Alki, Matthew, and Mark creeks, which enter the St. Mary river from the north. On Mark creek, a fall occurs in the normal position about 4 miles from its junction with the St. Mary river and in addition another fall is present within 200 yards of this junction. The main St. Mary river (Plate X) pursues a meandering course in a wide valley floor, the walls of which rise abruptly to a height of from 4,000 to 5,000 feet. Above this elevation the slopes become more gentle indicating that the upland surface has been reached. The interlocking spurs so prominent in valley sculpture in non-glaciated regions are here lacking. The spurs have facetted fronts so that in a view up the valley the cross section is trough-like in character. In the western part of this main valley, the river flows eastwards in anastomosing channels through a flat valley bottom which in spring floods is covered with water. Approaching St. Mary lake (Plate XI) the valley floor is marshy and contains many oxbow lakes (Plate X). Where the river enters the lake, a delta has formed and it is very probable that the deposition of sediment by the river has greatly lessened the area of the lake which is at present 2 miles long by 1 mile wide. In the vicinity of St. Mary lake (Plate XI), the valley walls rise very abruptly on either side and are composed of Aldridge quartzites and intercalated gabbro sills dipping to the v/f^'* or up the valley. The valley at this point is relatively narrow. It is probable that the outlet of this lake is located on a diorite sill. No terraces or benches are present around 12 the lake; but as the Kootcnay valley is appro-irhefi to the east the terraces gradually make their appearance m . tne St. Mary river flows in a meandering course in a trough which it has cut in the stratified gravels and sands (Plate XII). The terraces are most prominent from Marysville to the junction of the St. Mary and Kootenay rivers. The bluffs which occur along the St. Mary are not of equal height, owing to the irregularities in the surface of the prairie at its junction with the river valley. These bluffs are occasionally ornamented with hoodoos. Two addirional streams drain the prairie belt within the Cranbrook map-area, Cherry creek, which flows east to join the Kootenay river and Luke creek, flowing south into the St. Mary river. The latter creek is located entirely within the prairie belt, and about half a mile from its mouth it disappears into the gravel and sands to reappear close to its junction with the St. Mary river which it joins by a series of cascades in a narrow gorge cut in the gravels. This non-accordance of grade between the two streams is evidently due to their different erosive powers. This disappearance of streams into the gravels is a common occurrence in the tributaries of the Kootenay river where a wide stretch of gravels has to be crossed before the main river is reached. The stratified floor Hicks, H. B., Report of Minister of Lands for British Columbia, 1912, p. D150. 16 continuing through January and February, the temperature ranging from freezing point to lero, and occasionally, for a few days at a time, going as low as 20 or 25 degrees below zero. The snowfall is sufficient for sixty or seventy days' good sleighing. In a very exceptional year, the temperature may go to 30 degrees below zero during November, with 12 or 15 inches of snow, this low temperature lasting only one or two days. In the month of I 'arch all snow and ice will disappear from the lower flats and valleys. Generally, the rainfall is scattered through the months of April, May, June, September, and October; July and August are the dry and warm months. In exceptionally wet seasons it is necessary to irrigate but very little. "Below is a table compiled from the records taken at Cranbrook and kept by the Meteorological Service at Victoria, giving the total precipitation for all of the year 1911 and eleven months of the year 1912. It may be noted that 10 inches of snow is equal to 1 inch of rain. I believe the total precipitation for the year 1911 would represent an average year. The total precipitation is not necessarily the governing factor in deter- mining whether a year shall be called a wet or dry year. Two consecutive years might have the same precipitation; but if the rainfall were so distributed that during one season it was neces- sary to irrigate, and the next season it was not, they would be called respectively a dry and wet season. "The elevation, together with the dryness of the atmosphere, makes the climate most agreeable and invigorating. The altitude of the lower valleys and benches will vovy .' c i 2,450 to 3,100 feet. The adjacent mountain-ranges vary in height from 7,000 to 9.000 feet." Irrigated and Irrigable Areas.' "The district known as the 'East Kootenay,' a part of which is embraced in this report, is quite distinct from other parts of British Columbia, south of the main line of the Canadian » Hicks, H. B. Report of Minister of Lands for British Columbia, 1912, p. D 150. 18 P .<;•:. c I ilway, in respect to the extensive areas of evenly .,'ioping la Is lying between the rivers and the mountains. The CgwTvs i;; .n in the following table include not only such areas u. ..lay ue readily irrigated from adjacent streams, but take into consideration the fact that, in the near future, systems of conserving the waste waters will be developed, making it possible to irrigate all the valley and bench lands: — Locality. Bull River Fort Steele Wasa Sheep creek Skookum-chuck Cherry creek St. Mary prairie Upper St. Mary prairie Perry creek Cranbrook Upper Moyie Lower Moyie Total Irrigated or culti- vated acres. Irrigable (esti- mated) acres. 750 833 360 260 140 750 1,150 50 80 830 200 50 5,455 25,000 18,000 29,000 18,000 13,000 20,000 33,000 10,000 2,400 30,000 5,000 12,000 215,400 In addition to these localities the areas in the vicinity of Gold and Linklater creeks, contain the following acreages.' Locality. Irrigated or culti- vated acres. Irrigable (esti- matcil) acres. 170 300 6,500 Gold creek 17,408 470 23,908 > Biker, W. J. E., Report of the Minister of Lands for B.C., 1912, p. D154. 19 CHAPTER III. GENERAL GEOLOGY. : GENERA L r>TATEMENT. The rocks c th • Purcell r iige form the western part of the ancient group :/ .eHiments dt posited in the Rocky Mountain geosyncline. These beuiii.u; ts. called the Purcell series, and of Pre-Cambrian Beltian age, consist of a great thickness of fine-grained quartzites, argillaceous quartzites, argillites, and limestones, all remarkable for their homogeneity. At various horizons in this series, shallow water characteristics, including ripple marks and mud-cracks, are very common. The Purcell series extends across the International Boundary line into Idaho and Montana, but geological exploration has, up to this time, been insufficient for the exact determination of the northern limits. To the west, on account of batholithic intrusions, the relations are not very clear, but there is some evidence to show the existence of numerous patches of acidic pre-Beltian schists in the Selkirk mountains. This ancient acidic terrane probably represents at least part of the old land from which the quartzitic Purcell series was derived. The stratified members of the Purcell series pass unconformably under the younger Palaeozoic formations of the Rocky mountains to the east. The small cross-cutting bodies of granite and porphyritic granite, which intrude the Purcell series, are believed to be small, cupola-like stocks bearing a genetic relationship to the great West Kootenay granite batholith. The age, subdivision, and correlation of the great thickness of sedimentary strata, exposed in the Purcell range, have been the subjectof much study during the last few years. The sedimentary series of East Kootenay forms a part of this greatly discussed series. Since no fossils have as yet been discovered in the Purcell series, the subdivision into formations is based solely on physical and lithological grounds; hence the dividing line be- 20 tween the subdivisions is purely arbitrary and the personal equa- tion enters largely into the matter, especially as the formations pass conformably into one another. Along the International Boundary line, the Purcell series has been subdivided, in ascending order, into the Creston, Kitchener, and Moyie forma- tions, by Daly.' The table of formations given below represents equivalent sections in the Purcell range and in the western part of Rocky Mountain system in the neighbourhood of the Crowsnes , 3S3. The Purcell series is here used to include all strata below the unconformity which marks the top of the Pre-Cambrian. The base though not yet discovered will probably be the unconformity at the base of the unmetamorphosed Purcell series where it rests on the pre-Beltian schists and gneisses. The Galton series of the Galton range, a western subdivision of the Rocky Mountain system, is the eastern phase of the Purcell series. For conveni- ence an expanded geological column of the series exposed in the Purcell range is given; this will be followed by a full descrip- tion of each formation. ' R. A. Daly, Summary Report, G.S.C., 1904. Middle or Upper Cambrian Middle Cambrian Pre-Cambrlan (Beltian) 21 TaMe of Formations. Purcell range Rocky mountains Post-Glacial Stratified clays and sands Glacial Wycliffe drift Interglacial ? St. Eugene silts Jurassic ? Dyke intrusion Dyke intrusion Kootenay granite Mississippian Wardner formation Wardner formation Devonian Jefferson formation Jefferson fo. mation Elko formation VncoHformity 'Gateway formation i Purcell lava and Purcell Purcell sills Siyeh formation Kitchener formation Creston formation Aldridge formation I Burton form ation Unconformi'y Galton Series Roosville forma- tion. Phillips formation. Gateway forma- tion tl 22 Tabular Slatement of Geolotical Record. Quaternary Tertiary Cretaceous Jurassic (?) Carboniferous Devonian Silurian Ordovician Cambrian Post-Glacial Glacial InterglarLl ? Mississippian Erosion; deposition of clays and sands in depressions in drift. Erosion; deposition of Wycliffe drift. Erosion; deposition of St. Eugene silts, sands, and gravels (fossil plants). Erosion; uplift in eariy Tertiary; dissection of Cretaceous peneplain. Erosion; formation of Cretaceous peneplain. Orogenic movements; formation of Purcell range follow?d or accom- panied b/ intrusion of Kootenay granite. Wardner formation, mai 'ne deposi- tion of limestones and shaly lime- stones (fossils). Jefferson limestone; n.arine depoM- tion of grey or black magnesian limestones, heavy bedded (fossils). Erosion. Erosion. Erosion; early Cambrian uplift. Gateway formation; (continental de- position), sandstones, sandy argil- lites, some concretionary siliceous dolomite. Purcell lava, Purcell sills: intrusion of gabbro accompanied by out- 23 Pre-Cambrian (Beltian) f Purcell serie* Siyeh formation: (mainly continental some possibly marine deposition), red, purple, and green mud cracked argillites, sandstones, some lime- stones. pouring of basalt over land surface. Kitchener formation: (continental and possibly marine deposition), calcareous argillitr-:,, argillaceoua quartzites ripple marked, mud cracked, some limestones. Creiton formatum: shallow water deposition, quartzites, argillaceoui quartzli.es; mud cracks, and ripple marks. Aldridge formation: argillar«oiu quartzitei, some conglonieratea. THE PURCELL SERIES. General Statement. The Purcell series of East Kootenay was first described by Daly in the Annual Report of 1904,' and this was again published in unchanged form in a memoir in 1913.* The following is Daly's stratigraphic section: — Erosion surface. feet. Middle Cambrian Moyie 3,400+ Purcelllava 465 Kitchener, upper part 6,000± Lower Cambrian Kitchener, lower part 1,400+ „,. Creston, upper part 3,000 + "W'"*" Creston, lower part 6,500+ Base unexposed. 1 R*!^' B ^■' S*°!- S"^- Can-. Ann. Kept., 1904, p. 91A. • Daly, R. A., Geol. Surv., Can., Memoir 38, 1913, p. 119. 7,400 9,500 24 In 1911, Daly identified for the writer, the Kitchener and Creston formations, in the neighbourhood of Kingsgate, B.C., (8ee map) where the south-flowing Moyie river crossra the Inter- national Boundary line. Subsequent work by the writer in 191 2, definitely proved that the so-called Kitchener rocks near Kings- gate are older and not younger than the Creston, and the name Aldridge formation was proposed for this group of rocks. Fur- ther work on the section in the neighbourhood of the Moyie lakes (see map) showed that a group of rocks lithologically similar to those described by Daly as Kitchener, overlies the Creston and underlies the Siyeh. The name Kitchener has hence been retained for those rocks which overlie the Creston and under- lie the Siyeh. The Moyie formation was examined over a wide area. The area of Moyie rocks outlined by Daly west of Kingsgate was found to rest conformably upon the same rocks which Daly identified as Kitchener, near Kingsgate, and which were subsequently proved to belong to the Aldridge formation. Hence, they cannot be Moyie as originally defined by Daly as lying conformably on the Kitchener. Lithologically, these so-called Moyie rocks are identical with the Aldridge and hence are classed as Aldridge. The Moyie in the vicinity of the Yahk river rests conformably on the Kitchener formation as defined by the writer, and in this region is lithologically similar to the lower part of the Siyeh formation and occupies the same strati- graphic position as the Siyeh south of Cranbrook, where it overlies the Kitchener and underlies the Purcell lava. The Purcell lava is absent in the Boundary section but is present in the section south of Cranbrook (see map). Daly states that the Purceil lava is absent between the Kitchener and Moyie on the International Boundary line, since the flow did not extend as far west as the Yahk river. The writer con- cludes that the lava occupied a position above the Moyie and has been removed by erosion and that the Moyie is equivalent to the lower part of the Siyeh. Hence, the name Moyie has been dropped from the stratigraphic series of East Kootenay. The following is the author's stratigraphic section:— 25 EroHon surfau. Pre-Cmmbrian. . Gateway Purcell lava Sijreh Kitchener Creston Atdridge Base unezpoted. Ald^udce Formation. 2,000+ 300 4,000 4,500 5,000 8,000± f 1 Distribution. — The Aldridge formation is the oldest known member ol the Purcell series. It embraces that succession of dark grey, argillaceous quartzites characterized by their rusty weathering colour, which underlies the greyish coloured, argil- laceous, Creston quartzites. This homogeneous formation occupies a large area within the Cranbrook map-area. A north- ern belt embraces the greater part of the area drained by the St. Mary river, and there the strata form, in general, an anti- cline plunging to the north. The western border of this belt where it crosses the South fork (Baker creek) and the West fork of the St. Mary river, is a conformable contact with the overlying Creston formation. South of Baker creek, the meta- morphosed Kitchener calcareous argillites are faulted into contact with the Aldridge formation. The northern border of the belt ha.s not been explored but it is believed that there the Aldridge formation passes conformably under the Creston formation. The southern border is formed by a fault which brings the Aldridge and the overlying Creston formation rnd, farther east, the Aldridge and Kitchener, in contact. From Marysville this fault strikes on the one hand, southwest and on the other hand, east, and continues beyond the area of reconnais- sance. The eastern portion of this Lelt passes under the Pleis- tocene deposits of the Kootenay valley. The next area of the Aldridge formation to the south is separated from the northern area by a block of Creston argil- laceous quartzites. Starting at Cranbrook where the northern edge is a conformable contact with the overlying Creston forma- tion, this area of Aldridge strata strikes southwesterly and enlarges gradually to the west, forming a roughly wedge-shaped 26 mass which reaches to Kootenay Lake valley (Purcell trench). Hence this band of Aldridge quartzites forms a belt which stretches nearly across the whole width of the Purcell range and it proved a fine field for studying the variation in sedimentation. In the most westerly portion of the belt, where the Goat river crosses the Aldridge formation, it contains many beds of con- glomerates, consisting of well rounded pebbles of andesite and quartzite. In the eastern part of the belt the Aldridge formation contains no conglomerate and the rocks are all fine-grained ai^llaceous quartzites with very small amounts of grey argil- laceous limestones. The most southerly area of the Aldridge is an elliptical shaped mass of anticlinal structure whose greater portion lies southeast of the Canadian Pacific railway and west of the main Yahk river. The railway runs within this area along its western side and in the numerous rock cuts the strata are well exposed. The southern portion of this area lies in Idaho and was not visited. A small anticlinal area of the Aldridge lies east of the Yahk river in the neighbourhood of the International Boundary line. Thickness.— The base of the formation was not seen and the upper part was so badly folded that only a rough estimate of its thickness can be given ; this estimate is 8,000 feet. LUhology.— The Aldridge formation is made up of a series of argillaceous quartzites, purer quartzites, and argillites (Plate XIV). The argillaceous quartzites form about three- quarters of the whole series and occur in beds with an average thickness of one foot. Megascopically, they are fine-grained rocks, dark grey on fresh fracture, and weather to a rusty brown colour due to their rath»r high content of iron oxide. Under the microscope, the argillaceous quarUite is seen to c nsist of small, angular, interiocking grains of quartz 05-0-t mm. in diameter, thoroughly cemented together, in mosc cases, by argillaceous material which is altered to a network of seriate needles. Small amounts of striated feldspars occur as grains in most of the specimens examined. Muscovite, in lath-shaped individuals, and biotite in irregular plates are quite abundant in nearly all ths argillaceous quartzites. Small garnets, 0-01 mm. in diameter, and often showing optical anomalies, complete 27 the mineralogy of this rock type. In a few cases true sandstones were noticed in this formr.tion. They are coarser-grained than the quartzites but consisted of the same constituents. The purer quartzites strongly resemble the argillaceous quartzites under the microscope except that biotite and argillaceous material were far less abundant in the purer variety. At the lower falls on Mark creek, several strata of greyish talcose limestone amounting to a thickness of 6 inches, are exposed at low water. The Aldridge formation exposed on the hill north of Cameron creek, a branch of the Goat river, contains numerous beds of conglomerate whose pebbles, varying in size from a fraction of an inch to 2 inches in diameter, consist of grey quartzites. black slate, and an altered igneous rock, probably volcanic, related to an andesite. Most of the pebbles are water- worn but many are angular and subangular. Metamorphistn. — ^The metamorphism of 'he rock types of the Aldridge formation, as might be deduced from its com- position, has been for the most part very slight. On Matthew creek, at its junction with the St. Mary rive.*, a belt of gametif- erous mica schist is exposed and represents the metamorphosed argillaceous quartzite of the Aldridge formation since this schist passes gradually, on all sides, into the normal argillaceous quartzite. In the hand specimen, it is a glistening rock con- taining a great quantit*/ of Muscovite and quartz. "iVhen studied microscopically, it is seen to be composed chiefly of the micas, biotite and muscovite, with subordinate amounts of garnet, quartz, and sillimanite. The sillimanite indicates the presence of an intrusive mass in the vicinity of the sillimanite schist, since this mineral is the stable form of aluminum silicate at high temperatures. According to Vernadsky,' the inversion tempera- ture of cyanite into sillimanite is between 1320 degrees and 1380 degrees C. Gee' gical evidence of the inversion point has been given by Barrow,^ who described the conversion of cyanite into sillimanite by contact metamorphism. Close to the granite intrusives, the Aldridge argillaceous > Vemadsky, Zeit. fOr kryrt, Vol. 29, 1904. > Barrow, J. Q.J.G.S., Vol. 49, 1893, p. 340. 28 quartzites are changed to a knotted quartxite.the knota consisting of the accumulation of carbonaceous material. The Aldridge formation is characterized by the occurrence of economic deposits of silver-lead ores. The productive portion of these deposits occurs in heavy bedded, purer quartzites; while in the thin-bedded argillaceous members, the veins consist of quartz with minor amounts ol the sulphides. Structure. — ^The present attitude of the strata of the Aldridge formation shows that it has suffered some orogenic movements. In general, it is warped into a series of anticlines and synclines striking in a northerly direction. The Moyie valley in the neigh- bourhood of the Moyie lakes, has been eroded along the axis of an anticline which plunges to the north. The folds are usually gentie but occasionally, as in the mountains in the vicinity of the St. Mary river, minor overturned anticlines, mashing and faulting, modify the major folds. The com- pression to which these rocks has been subjected has not developed any signs of schistosity except in the argillites which separate the heavy bedded, purer quartzites. Creston Forhatiok. Di'trihution. — The Aldridge formation passes by gradual transit! ri >nto the overlying Creston quartzites. The tran- sitiona . ..unit averages 500 feet in thickness and is well exposed along ihe Crowsnest branch of the Canadian Pacific railway, 4 miles north of Moyie city. From this point, continuing north, the Creston formation outcrops in the many rock-cuts along the railway as far north as the northern end of Upper Moyie lake. In the region examined, two main belts of Creston rocks, separated by a monoclinal fault block of the Aldridge formation, strike in a northeast-southwest direction across the Purcell range. The northern b^lt appears at Steele in the Rocky Mountain trench in contact with the Pleistocene. This belt of Creston rocks strikes almost due west for a distance of 16 miles, then swings to a southwesterly direction until it passes beyond the western boundary of the sheet. From a study of the West Kootenay 29 map sheet, it is concluded that this belt of Ct eston rocks probably is cut off on the west by an intrusion of granite. The southern belt pursues a semi-elliptical shaped course with its apex on Upper Moyie lake, and forms the outer portion of the anticline whose centre is composed of Aldridge strata form- ing the Yahk mountains. The western and northwestern outer border is bounded by the Moyie fault which brings up the Al- dridge formation into contact with the Creston rocks. The northeastern and eastern outer boundary is formed by the conformable contact with the overlying Kitchener formation. About 5 miles north of the International Boundary the eastern portion of this elliptical shaped belt splits into two bands which form, respectively, the eastern and western limbs of a syncline whose centre is occupied by Kitchener and younger strata. The more easterly band again divides into two about 2 miles north of the boundary line where these two subdivisions form the limbs of an anticline whose centre is formed of Aldridge beds. Good exposures of the Cresfon formation occur on the Upper Moyie lake, in the Yahk River canyon, and on the mountain side east of the Moyie river at Kingsgate. The study of this southern area of Creston rocks was of very great service in the attempt to unravel the structure of the region and as well, had an important bearing on questions of correlation. Thickness. — The section of the Creston formation along Upper Moyie lake is comparatively free from folding and faulting. One traverse was made across the formation at this locality and the thickness was found to be about 4,500 feet. All of the section was not exposed but it is believed that the thickness given closely represents the total thickness of the formation. Daly, from his measurements across the same formation along the International Boundary, estimates its thickness to be about 8,000 feet, and in his sections the base and the top of the formation were noi exposed. Lithology. — ^The Creston formation embraces that succession of greyish argillaceous quartzites which is included between the dark rusty weathering, argillaceous quan-^ites of the Aldridge formation and the thin-bedded calcareous rocks of the Kitchener. In general, the Creston formation consists of argillaceous quartz- 30 ites, purer quartzites, and argillites, whose beds average about 1 foot in thickness. The formation as a whole, contains purer quartzites more abundantly than the underlying Aldridge formation and the quartzites are light grey on fresh fracture and weather in greyish tones so that, at a distance, the rock outcrops resemble limestone. In fact a common local name for these light grey quartzites is "bastard lime." Between these quartzites occur thin beds of argillite about 1 to 3 inches thick, which are darker in colour than the quartzites themselves, so that, in steep cliffs, a decided banding is a prominent feature. No limestone was found in the Creston formation. A progressive change from west to east is tc be seen in the texture of the quartz- ites. The Creston rocks, where they cross the Goat river about 12 miles north of Kitchener, are made up of material resembling coarse sandstone; while in the neighbourhood of Moyie lake and on Perry creek, they consist of fine-grained, argillaceous quartzites. This change in texture is in accordance with that described above as characteristic of the Aldridge formation. The most striking feature revealed by the microscope was the very small size of the grains which go to make up the rocks of this formation. The main constituent is quartz which occurs in small angular interlocking grains O-OS-l mm. in diameter. However, in the true sandstones, which are present in small amount in the Creston formation, the grains are larger and spherical in outline. The ar(;illaceous quartzites have an argillaceous cement which is usually altered to a dense network of sericite needles. The argillaceous cement is, in a few cases, replaced and also accom^mied by calcium and mag- nesium carbonate, thus giving rise . > calcareous and dolomitic quartzites. When the cementing material is lacking altogether, the rocks pass into the purer quartzite which is composed almost entirely of small interlocking grains of quartz, with a little striated feldspar. Muscovite is often present in dusty aggregates and sericite, in needle-like forms, is rather common. Small garnets sometimes appear sporadically in the argillaceoua quartzites. Metamorphism. — ^The members of the Creston formation 31 are quartzites of different varieties which are themselvca meta- morphosed sandstones of various coniposif <• tns. In a few cases, the quartz grains, by their optical properties, show that silica has formed around the grains since deposition. This indicates the process which cemented the quartz grains into a firm dense rock. In the argillaceous quartzite the sericitic material is the result of chemical rearrangement and recr>'stal- lization of the formerly existing argillaceous material. The argillaceous quartzites, and purer quartzites of the Crcston formation are very resistant to the action of contact and regional metamorphism. Around the granitic intrusions, the only effect is the formation of knots of carbonaceous material, within 500 feet of the contact. The rocks farther away are normal in every respect. Regional metamorphism has induced a shearing at right angles to the bedding planes of the argillites which separate the thick-bedded purer quartzites. Structure. — ^Since the Creston quartzites lie conformably upon the Aldridge formation, these two series must have a similar structure, that is, the Creston has been folded into anti- clines and synclines. The Crcston quartzites are characterized at various horizons by shallow water features. Ripple marks are well shown in the rock cuts along the Upper Moyie lakes and along the road on Perry creek above Old Town. Kitchener Formation. Distribution. — A small area of Kitchener calcareous argil- lites and quartzites occurs between Perry creek and the St. Mary river in the neighbourhood of Marysville. The strata rest conformably upon the Creston formation on the west and pass under the Quaternary deposits of the Kootenay valley on the east. The northern and southern boundaries are formed h"' faults which have a general east and west strike. On the north, the Kitchener is in contact with the Aldridge formation, while to the south, it is in contact with the Creston argilla- ceous quartzites. In the vicinity of the headwaters of Whitefish or Meachen creek and the Goat river, an area of westerly dipping Kitchener 32 rocks occurs. Its northeastern border is bounded by a fault which brings the Aldridge into contact with the Kitchener. This area extends to the west beyond the map-area where it was found that these rocks pass gradually into the Selkirk series. The southern boundary is formed by a fault which strikes in a northwesterly direction. This fault brings the Kitchener and Creston formations in contact. Starting on Upper Moyie lake a linear-shaped area of Kitchener beds extends southeastwards to the International Boundary line and forms part of the easterly dipping limb of the Yahk anticline. On the north, it is cut off by the Moyie fault which places it in contact with the Aldridge formation. Its easterly and westerly limits are formed respectively by the conformable contacts of the overlying Siyeh and the under- lying Creston formations. Another area of the Kitchener rocks occurs between the two crossings of the Yahk river at the International Boundary line where it forms a synclinal basin capped by about 1,000 feet of the overlying Siyeh green and purple, mud-cracked shales. Thickness. — ^The best section of the Kitchener formation for measurement, was found along the Canadian Pacific railway on Upper Moyie lake in the vicinity of Jerome. Exposures are fairly good and show evidences of only very little folding; hence the measured thickness, 4,500 feet, can be taken as correct. Lilhology. — In comparison with the underlying Creston and Aldridge formations, the most notable feature of the Kitchener formation is its content of lime. The formation consists of cal- careous and argillaceous quartzites, quartzites, and limestones. The argillaceous limestones are well exposed in the railway tunnel at Jerome and occur in beds 6 inches to 1 foot in thickness. The general weathering colours are yellowish brown and grey. On the weathered surface, parallel to the bedding planes, are numerous linear depressions about one-eighth to one-quarter inch wide and one-half inch deep (Plate XVA), while on the planes perpendicular to the bedding, these depressions are irregular and some are vermicular (Plate XVB). Evidently these depresuons are the result of the leaching out of the 33 purer calcareous phases. This peculiar weathering effect is characteristic of these argillaceous limestones. Purer lime- stones also occur and were noted on the divide between the main river and the west fork of the Yahk. Argillaceous quartz- ites, darker on fresh fracture than the Creston quartzites, are quite abundant and weather to a yellowish brown or a light grey colour. Structure. — The Kitchener formation rests conformably on the Creston formation. The contact exposed south of Jerome in the railway cut, shows that no sharp line can be drawn between the formations and that they grade into one another, the transition zone being about 500 feet thick. The Kitchener is overlain conformably by the Siyeh formation and this contact, which is gradational also, can be seen about one-half mile north of the Upper Moyie lake on the road which follows Peavine creek to Cranbrook. Siyeh Formation. Distribution. — ^The most westerly exposure of the Siyeh formation occurs between the points where the West fork and the main Yahk river cross the Internationcd Boundary. Here it forms the axial portion of a small syndine. No limestone occurs in this section since the thickness exposed is only 1,500 feet. This exposure is surrounded in Canada by the Kitchener formation. The southern portion, since it lies in Idaho, was not explored. A long linear area of the Siyeh formation begins on Moyie mountain where its northern continuation is cut by the Moyie fault which brings up an area of Aldridge argillaceous quartzites. The Siyeh formation from Moyie mountain, strikes in a southerly direction and crosses the International Boundary line. The strata form part of the western limb of a syncline which strikes in a north-south direction. The western boundary of the Siyeh area is formed by a conformable contact with the underlying Kitchener formation, while the eastern boundary is marked by the Purcell lava. Another large area of the Siyeh formation forms, for the 34 most part, the most easterly hills of the Ptsrcell range. This area begins south of Cranbrook and with one interruption, continues to the International Boundary line. The central portion between the first gap in the hills south of Cranbrook, and Plumbob creek, is occupied partly by the Gateway formation and partly by Devonian-Carboniferous limestone. Fine exposures of the Siyeh formation showing its relation to the Purcell lava can be seen on Baker and Moyie mountsiins. Litkology. — ^The lower part of the Siyeh formation is composed of thin-bedded, green and purple, mud-cracked metargillites and sandstones (Plate XVI, A and B). Some black metargillites are also present which weather to a rusty brown colour. About one mile north of Upper Moyie lake on Peavine creek is exposed a massive conglomerate about 200 feet thick which was seen in no other section of the Siyeh for- mation. It occurs about 200 feet above the determined base of the Siyeh. The lithology of the conglomerate is quite varied and consists of pebbles of greenish grey argillaceous quartzites, brownish red sandstones, white quartzites, and highly altered amygdaloidal and non-amygdaloidal basalt. Most of the pebbles are rounded; but some are angular and subangular. The origin of the pebbles cannot be definitely determined, although most of them strongly resemble the underlying forma- tions. The terrane from which the pebbles of basalt were derived is unknown, as no lava flows were found in the under- lying formations. Underneath the conglomerate with no unconformity, occur chocolate brown and purple, mud-cracked metargillites. The significance of this conglomerate could not be determined from the one isolated exposure. This con- glomerate was succeeded by chocolate brown sandstone composed of small particles of the same materials as the conglomerate. The microscope shows that the sandstone is composed of angular and subangular grains of quartz, plagioclase, argillaceous quartz- it*', and altered basalt in a calcareous cement. About 2,000 feet above the base of the Siyeh formation occur thin-bedded and mascive, siliceous, concretionary lime- stones, grey on fresh fracture and wea lering grey and buff. They reach a thickness of about 1,000 feet. These limestones 35 I are succeeded by purple and green, mud-cracked metargillites in thin beds and since the purple and green beds occur grouped alternately for a thickness of 10 to IS feet they give a striped appearance to the mountain sides. This is especially well shown on the west side of Baker mountain. Towards the top of the Siyeh on Baker mountain, the following section, in descend- ing order, was measured: Purple and green metargillites and sandy quartzites. . . 20 feet Porphyritic-amygdaloidal basalt 50 " Purple and green metargillites and sandy quartzites. . . SO " Non-amygdaloidal, non-porphyritic basalt ICO ' Purple and green metargillites 400 " Amygdaloidal basalt 300 " Purple and green metargillites and sandy quartzites . . . SOO-f-" Remainder poorly exposed. I . sediments which form the top of Baker mountain are succeeded on the east side of Baker mountain by another flow of amygdaloidal and porphyritic basalt. Frequently the lava flows are succeeded at the immediate contact by a sandstone composed of particles, generally angular, of the underlying basalt. Thickness. — No complete section, with the definite top and bottom of the Siyeh formation was found, but a rough estimate of several sections gave a maximum thickness of 4,000 feet. This agrees well with Daly's thickness of 4,000 feet for the same formation at the International Boundary line. Structural Relations. — ^The Siyeh formation rests conform- ably upon the Kitchener argillaceous quartzites and limestones with a transitional zone of 300 feet thickness. The top of the Siyeh formation, as defined by Daly, is the base of the Purcell lava. As seen from the above description of the Siyeh formation, several lava flows occur separated by important thicknesses of sediments. The top of the Siyeh is placed at the bottom of the last flow of lava since the sediments between the under- lying flows of lava are identical with the remainder of the Siyeh metargillites. The Gateway formation which rests on the last Purcell lava bed, is in strong contrast both lithologically and in its colour scheme, to the Siyeh formation. r! 36 Gateway Formation. Distribution. — ^The Gateway formation is found only in the most easterly part of the Purcell range, the McGillivray range. The axis of this latter range is marked by a syndine of the Gateway formation striking a little west of north. The western boundary is limited by the Purcell lava, which also outcrops in places along its eastern boundary. The eastern contact for the most part, however, is formed by a fault striking north- northwest-south-southeast and roughly parcdielling Gold creek. This fault brings the Siyeh into contact with the Gateway formation. Near the International Boundary the eastern limb of the syndine is exposed, the fault cutting across the succeeding anticline of Siyeh rocks to the east. A smaller area of the Gateway formation, which dips to the east, occurs between the stream south of Baker creek and Plumbob creek. On the west, the Purcell lava forms the boun- dary, while on the east the Gateway is overlain unconformably by the Devonian-Carboniferous limestone. Another area occurs in the Kootenay valley opposite the mouth of Elk river and this is also bounded on the west by the Purcell lava. It passes at its remaining boundaries under the Quaternary deposits of the Kootenay valley. Lithology. — ^The base of the Gateway rests on the Purcell lava conformably and is formed of a fine-grained grit containing pebbles of the Purcell lava as well as a few pebbles of quartzite. This is succeeded by alternating beds of conglomerates and sili- ceous limestone. The conglomerates observed never exceeded 15 feet in thickness. The limestone weathers buff and is con- cretionary in habit, the siliceous parts projecting from the weathered surface. Some dolomites are also present. Inter- banded with the dolomites are purple shales and grey sand- stones. These are succeeded by greyish brown weathering, sandy argillites in beds 1 to 2 inches thick, containing abundant casts or salt crystals (Plate XVII), which were not found in any other formation in the district. Interbanded in these sandy argillites are numerous heavy bedded buff weathered sandstones and quartzites. 37 Thickness. — ^A complete section of the Gateway was not found in the region examined. The thickness of 2,025 feet determined by Daly' is, therefore, taken. Structural Relations. — ^The Gateway formation rests upon the Purcell lava conformably. In the Purcell range the Devonian limestone rests unconformably on the Gateway formation. Where this contact was examined no discordance of dip between the formations was noted; still the absence of the Phillips, Roosville, Burton, and Elko formations, present in the Rocky mountains, points to a great time interval between the Gateway and Jefferson limestone. The actual contact shows the sandy limestone brecciated and recemented. Many small patches a few feet to yards in diameter were noted on the hillside on Gold creek. On the north side of Plumbob creek, the southern part of the hill is occupied by the green and siliceous mud-cracked metargillites of the Siyeh formation, while the eastern part is covered by the Devonian-Carboniferous limestone. Although i.ue contact between these two formations is not well exposed, yet exposures are sufficient to show that the limestone rests upon the Siyeh formation and the Purcell lava. Thus the placing of an unconformity between the Carboniferous limestone and the Pre-Cambrian io warranted. Willis' describe lilc break between the Carboniferous series and Pre-Camb. \.i the Yakunkak valley, as follows: "On crossing the Flath i valley, however, to the Gal ton range a small area of limestone is encountered in Yakunkak valley. The rock is a light grey and dark blue limestone about 100 feet thick, distinctly bedded, commonly crystalline, occasionally oolitic it is without upper stratigraphic limit, but rests conformably on a quartzite, which is unconformable on Algonkian strata. The quartzite is 25 feet thick, and it and the limestone lies in a nearly horizontal position The Yakunkak limestone contains numerous fossils of the Saint Louis horizon of the Mississippian series The absence of earlier Mississippian ' Daly. R. A., Ged. Suiv., Can., Mem. 38, 1913, p. 107. • G.S.A.. Vol. 13, 1902. p. 325. 38 strata is significant of an unusual overlap it is possible that it (Yakunkak limestone) rests on the Siyeh limestone, in which case the break between the two would not be readily recognized, as the rocks are very similar and the angular difference of dip is slight." Origin of the Purcell Series. In the detailed description of the Purcell series, it was stated that the series consists of a great thickness of argillaceous quartz- ites, quartzites, argillites, and limestones. In general, the rocks are well bedded ; the individual beds vary from 1 inch to 8 feet in thickness. The rocks consist of interlocking grains of quartz, striated feldspar, and argillaceous material. At various horizons in the series, occur ripple marks and mud-crcicks which are especially abundant in the Siyeh formation. Casts of salt crystals are especially abundant only in the Gateway formation. Evidence of contemporaneous erosion occurs in the Aldridge formation. The extreme fineness of grain and the almost perfect separa- tion of the siliceous and aluminous materid, lead to the con- clusion that these sediments were derived from an older terrane probably composed of acid gneisses and schists, in a region in the stage of topographic late maturity. The Aldridge argillaceous quartzites are dark grey on fresh fracture and weather to a rusty brown colour. Hence, the iron contained in these quartzites is in a ferrous condition. It is also probable that some carbonaceous material is present. This shows that the climate at the time of the deposition of the Aldridge sediments was humid.' The presence of the striated feldspar in the quartzites, supports the idea that mechanical disintegration of the source of supply was more rapid than decomposition or weathering. The evidence of contemporaneous erosion, as well as the conglomerates, found in the Aldridge formation on the Goat river suggests that the water in which these sediments were deposited was shallow and that subsidence and deposition proceeded approximately at the same rate. 'See page 39. "• ' iTMBMi tSm 39 The quartzidc Creston formation is characterized by a green- ish colour which, when wet, has a translucent olive green hue. Ripple marks are present at various horizons throughout the whole formation. Evidently the conditions of deposition of the Creston sediments were similar to those under which the Aldridge sediments were deposited. The more calcareous portion of the Ilitchener formation evidently accumulated in comparatively deep water, since no shallow water features were noted in it, although they were very prevalent in the more quartzitic phases. The next succeeding formation, the Siyeh metargillite, is characterized by the presence of alternating greyish-green and purple to chocolate-brown argillites, the latter being especially dis- tinguished by the presence of abundant sun cracks. Hence, the water in which these sediments weredepoaited was shallow, and even shallower than the Aldridge or Creston sea, since occasionally the water of the basin became shallow enough to allow the forma- tion of mud-cracks. The climate at the beginning of Siyeh time must have been alternating humid and arid, since it is believed that such climatic conditions are necessary for the formation of alternating greenish-grey and purplish-red strata. Barrell* speaks of the significance of red coloured deposits as follows: "Turning to the climatic significance of red, it would therefore appear both from theoretical considerations and geological observations that the chief condition for the formation of red shales and sandstone is merely the alternation of seasons of warmth and dryness with seasons of flood, by means of which hydration, but especially oxidation, of the ferruginous material in the flood-plain deposits is accomplished. This supplements the decomposition at the source and that which takes place in the long transportation and great wear to which the larger rivers subject the detritus rolled along their beds. The annual wetting, drying, and oxidation not only decompose the original iron minerals but completely remove all traces of carbon. If this conclusion be correct, red shales a d sandstones, as distinct from red mud and sand, may originate tmder intermittently rainy. \l » Barrdl, J., Jour, of Geol., 1908, p. 292. 1 i 40 subarid, or arid climates without any close relation to temperature and typically as fluvial and pluvial deposits upon the land, though to a limited extent as fluviatile sediments coming to rest upon the bottom of the shallow sea. The origin of such sediments is most favored by climates which are hot and alternately wet and dry as opposed to climates dry." Continental deposition under arid conditions prevailed throughout the Gateway times, as shown by the presence of the casts of salt crystals and the abundance of ripple marks. Sources of the Sediments. The Aldridge formation in the eastern part of the Purcell range contains no conglomerates; but ir the western part, as in the vicinity of the Goat river, conglomerates are quite abundant. The Creston formation also is coarser in the western part of the range. Hence, it is concluded that the land from which these sediments were derived was situated to the west of the Purcell range, and probably as close as West Kootenay, for the Pre- Cambrian complex of gneisses and schists ouLv..ops at various points in that region. Daly' in a study across the whole Rocky Mountain geosyncline, remarks on the decrease in the coarseness of the sediments from west to east. Purcell Sea. The water in the Purcell continental basin, in which the Purcell sediments were deposited, was certainly shallow for the most part. Walcott* believes from the abrupt appearance of the Cambrian fauna in sediments of Rocky Mountain geo- syncline, that the Purcell sea was not connected with the ocean and that the water in the sea was either fresh or brackish. Bauerman* in his report on the Purcell range classes the rocks now known as the Purcell series as shallow water deposits and the presence of salt crystals he explains by the « Daly, R. A., G.S.C., Summ. Kept., 1904, p. 97A. • SmithBonian Col!., Vol. 57, 1910, p. 1. • Bauerman, H., Geol. Surv., Can., Rep. of ProgicM, 1882, p. 25 B. 41 evaporation of a shallow sea which had no connexion with the ocean. Age and Corselation op the Puscell Series. Dawson' first described the rocks of the Purcell range as Cambrian and McEvoy* followed him in this determination. Daly* working across the range along the International Boundary line considers the lower part of the series as Pre-Cambrian and the upper part Cambrian. The writer considers the Purcell series to be entirely of Pre-Cambrian age, the evidence for which is submitted in the following discussion. Since the evidence collected in the Purcell range was in> sufficient to determine the age of the Purcell series with any degree of certainty, it was found necessary to examine in detail a section in the Rocky mountains where the contact of the Pre-Cambrian Galton series, which is correlated with the Purcell series and the older Palaeozoic formations, is exposed. A fine section was found in the hill north of Elko, B.C. A full discussion of the correlation of the Pre-Cambrain and Cambrian rocks of the Purcell and Rocky mountains has been given in the Museum Bulletin No. 2.* The mountains to the north of the Elk River valley at Elko, form the most western part of the Rocky Mount£un system. The structure of these mountains is of the nature of a syncline striking northwest-southeast. The eastern limb of the syncline is cut off by a northwest -southeast fault which brings the Devonian-Carboniferous limestone in contact with the Rooaville formation. The strata forming the western limb '^f the syncline and incidentally the western face of Rocky mountains, dip on an average of 45 degrees to the northeast. Elko, a station on the Crowsnest branch of the Canadian Pacific railway, is situated on the western slope of the Rocky Mountain system, at the Elk River portal to the Kootenay Valley ' G. M. Dawson, Geo!. Surv., Can., Ann. Rep., 1885, p. 148 B. II S. J. Schofieia, Mui. Bull. No. 2, GecA. Surv.', Can",' 1914,' pp." 79-91. U 42 or Rocky Mountain trench. The section exposed at Elko can be mc t easily expressed in a stratigraphical column. 300+ feet 90± • 80± • Devonian Jeffenon limettone. Cambrian Elko formation Middle Cambrian Burton formation. . Uncot^ormity. Beltian Roosville formation 1 ,000 ■ Phillips formation 500 * Gateway formation 1,000+ * The Gateway, Phillips, and Roosville belong to the Galton series of Daly.* Gateway Formation. The lower part of the formation consists ot alternating bands of massive, concretionar /, siliceous dolomite and limestone weathering buil, and massive, light grey quartzites. These are succeeded by thin-bedded, sandy argiUites and greenish grey, siliceous aigillites. The sandy argiliites weather a light buff and are characterized by the presence of abundant cast* of salt crystals. Phillips Formation. The Gateway formation passes gradually into the over- Ijdng Phillips formation which consists mainly of dark purplish and red metargillites, sandy argiliites, and sandstones. At several horizons are intercalated thin laminae of green «liceous argillite. These rocks are exposed in a rock cut on the Great Northern railway, 1^ miles east of Elko, from which point they rise to the east on the hill to the north of the track. RoosmUe Formation. The Phillips is overlain conformably by the Roosville which is composed mostly of massive laminated, green, siliceous metai^illites weathering greenish grey and rusty brown. Mud » Daly, R. A., G.S.C., Memoir ?S, p. 97. 43 cracks are abundant at all horizons. The Elk River canyon is carved in the horizontal strata of the Roosvillc formation. These rocks have been called the Elk River Bridge beds by Dawson'. i i Burton Formation, The Burton formation, called after Burton creek near Elko, rests mth no discordance of dip on the Roosville siliceous metargi'.htes and consists in great part of greenish black, calcar- eous shales with interbedded siliceous limestone bands. A de- tailed section of the Burton formation at Elko is as follows: Elko formation. Greenish black shales with limestone interbands 60+ feet Burton formation J Sandy limestone 10 * Greenish black shale 4 * Calcareous grit 3 * Hematitic conglomerate 8-10 inches Roosville siliceous metargillites. No structural unconformity could be detected between the Roosville and the Burton in this section. The hematite conglomerate, the base of the Burton, is composed of rounded to subangular pebbles of siliceous hematite, embedded in a ce- ment consisting of quartz and hematite. The origin of this conglomerate might be attributed to the erosion of hematite deposits which occur quite abundantly in the underlying Pre- Cambrian formations. This conglomerate passes gradually into the overlying grit which is made up of angular and sub- angtilar grains of the Roosville siliceous metargillite and a great number of milky white and glassy quartz grains in a calcareous cement. This grit contains the oldest fossils found in the Burton series. Succeeding this ^rit are about 4 feet of calcareous, greenish black shales which readily weather to soft earth. They are brittle and break up in small rectangular shaped pieces. Above this shale comes 10 feet of sandy limestone, in beds from 1 to 2 feet in thickness, broken by vertical joints. The weather- ing colour of this limestone is brown. Above the limestone > G. M. Dawson, Geol., Surv., Can. Vol. 1, 1885, p. 78 B. 4 i 44 comes aixi 't 60 feet of g:reenish black, alcareous shale containing numerou» oands of siliceous limestone. These interbands are especially rich in trilobite remains. Age of the Burton Formation. The a^e n! tht Burton formation is discussed by L. D. Burling as folk..vs:' "the Burton formation has been named and describe' I v J. Schofield*. who, together with the writer, mcnsur -J tho ir owing section in the slope directly back of the Bur - .liiit ab ut 2 miles northwest of the town of Elko, Britifc 1 C ^Isimbia. Sec oi, 0,' 3u ton Formation near Elko, British Columl'ia. Feet. Fauna. Elko li;pi «>(.rit: '< ap'';(i.' e .9 B i 5. Gi-'.ish '._. ■ j.ea with .•< irljedd ' 1 tones, the Kr ertone I ' n. the form oi 1 naes ar i . -rg 1 to 3 ii ie» in l^,(.l^I;lN. 111(1 more o less continuous t ut mak- ing up a very small propor- tion of the strata. 60 In interbedded limestones within 5 feet of the base: Mtcromitra (Paterina), Micromxtra (Iphi- dHla) pannula, Obolus sp., AcrotkeU sp., Acrotreta sp., Agraulos sp., Ptychoparia sp., AlberUUa sp., Olenoidts sp., Bathyuriscus sp., and Crtput- phalus 2 species. 4. Massive, dirty grey, sandy limestone. 10 Near top: Mu romitra sp.. Micro- mitra (IpkideUa) pannula, At- raulos sp., Trilobite fragmenu 2 species. 1 Near base: Mtcromitra (Iphidd- la) pannula, Trilobite frag- ments 2 species, one suggesting OUnfllus § 1 3. Green micaceous shale, badly sheared. 4 ,One trilobitic fragment. 1 GQ 2. Rubbly weathering, calcare- ous grit, with annelid like borings in top layer. 3 1 Annelid borings, Uicromitra (Pa- Ifrina) sp., Acrotreta sp., Trilo- bite fragments 1 species. 1. Hematite conglomerate. 1 Roosville siliceous metargillite (Pre-Cambrian). > L. D. Burling, Geol. Surv., Can., Mus. Bulletin No. 2, 1914, p. 125. « Geol. Surv., Can., Museum Bull. No. 2, 1914, p. 82. 1 4S So far as the writer ia aware there are only three reported occurrences o( the genus Crepicephalus in the beds below or immediately above the line leparating the Lower from the Middle Cambrian. First, in the Pioche formation of Nevada, second, in a limestone with Alberktia on Mount Stephen, British Columbia', and third in interbedded limestones in a Middle Cambrian shale immediately overlying a quartzite on an island east of Niang-Niang-Kung, Liau-tung, Manchuria.* The limits of this paper will hardly permit the inclusion of any further reference to the latter occurrence or to the relations between this shale series and the horizons under discussion. The Middle Cambrian aspect of the fauna of No. 5 of the Burton formation was evident at the time its study was undertaken, but the associ- ation in the same 1-inch layer of two species of Crepicephalus and a representative of the genus Albertella suggested the com- parison of the Burton formation with the Albertella fauna and the Pioche formation, horizons which had both been referred to the Lower Cambrian. Analysis of the Albertella fauna in the other regions from which it has been identified revealed the lack of any necessity for the assumption that its Lower Cambrian age was infallible and the writer turned his attention to the Pioche. This was shown to be diviuble into Lower and Middle Cambrian zones respective- ly, and even to comprise faunas which, at the type localiiy of the Albertella fauna, are separated by 1,600 feet of limestone. At the type locality of the Pioche formation the range of faunas included in that unit does not appear to be so large and the Middle Cambrian horizon, to which the name Crepicephalus zone has been applied, is to be correlated, at least tentatively, with the Burton formation. The correlation of the Burton formation with the Albertel'j, fauna is based largely upon the pres- ence in the former of an Albeitella, a genus which, according to our present information, is confined in the Cordilleran region to this one horizon. The weight of evidence so largely opposes the Lower Cambrian age of these formations and corrob-^rates their reference to the overlying division of the Cambrian that the ' Walcott: Smithsonian Miac. Coil., vol 53, No. 5, 1908, p. 213. • Wakott: Reaearch in China, vol. 3, 1913, p. 26. legality iSr. f :U i I B 3 3 I x ca I a a 3 O a .9 3 3 I •c n a D s I B 3 1 § n gj2 j -noijTOijoj «j " OS }ano)i^ I a o GO 'oopeuijoj I Sx uopttujoi ^lii£k« 'TS 47 Burton formation is referred with some degree of certainty to the Middle Cambrian. It is hard to resist the impression, however, that the clastic portion of the Burton formation may represent the Lower Cam- brian, and while the few species occurring in these lower layers are either unrecognizable or referable to types hitherto unknown, the suggested definition of the Burton formation will not invali- date its future division into shale and sandstone members. The Burton formation is, therefore, interpreted as a more or less heterogeneous formational unit unconformably overlying the Pre-Cambrian, referable to the early Middle Cambrian, and easily separable into upper and lower members if such a division should be warranted by future work upon the faunas of its basal portion." Elko Formation. The Elko formation, called after the town of Elko, on the Crowsnest branch of the Canadian Pacific railway, rests upon the Burton formation. The exact contact between these two forma- tions was not exposed in the sections studied, but no structural evidence of an unconformity was present, exposures on each side of the contact being very good. The lower 30 feet of the Elko formation is composed of massive, grey, siliceous ''mestone, weathering grey, containing indistinct coral-like forms (Plate XVIII). The limestone by gradual transition, passes into a cream coloured siliceous dolo- mite in massive beds averaging about 6 feet in thickness. Age of the Elko Formation. At Elko no determinable fossils were found in the Elko formation. The fossiliferous Jefferson limestone rests confor- mably upon the Elko formation, hence from the evidence at Elko, the Elko formation may include Cambrian, Ordovician, and Silu- rian strata. During the season of 1914 the writer, in company with C. W. Drysdale, found a Cambrian section at Canal flats situated on the east side of the Rocky Mountain trench about 48 65 miles northwest of Elko. Fossils were cdlected in the straU resting t»nforniably on rocks, which strongly resemble the Elko formation in lithology and physical character. Mr. L. D. Burling, who examined the fossils, states, "I was unable to find the Albertella fauna, indeed most of the horizons appear to be much higher than the Albertella horizon, and represent the Middle or Upper Cambrian. If this interpretation is correct, you have obtained an upper limit for the Elko formation, placing it in the Cambrian instead of the interval between the Cambrian and the Devonian." Jefferson Limestone. In the Rocky Mountain system, the Devonian limestone apparently rests conformably upon the underlying Cambrian series (at Elko, the Elko formation) while in the Purcell range to the west, an apparent unconformity exists between the Devonian limestone and the Gateway formation. The staple rock of the Devonian is a massive, dark grey limestone weathering a whitish- grey colour. The following fossils were found in the limestone and were identified by Dr. E. M. Kindle: Atrypa reticularis, Spirifer ptonensis, Orthothetes chemungensis var. arctostriatus. Unconformity at the Base of the Burton. Although no structural features emphasize the presence of an unconformity at the base of the Burton yet from other evidence such an unconformity is believed to exist. (1) In harmony with the other sections throughout the Rocky Mountain geosynclinal, a marine Cambrian transgression is represented in the deposition of the Burton formations. (2) The conglomerate at the base of the Burton is composed chiefly of hematite pebbles with minor quantities of pebbles of quartzite and quartz in a hematitic quartz cement. The hema- tite pebbles, although some have a concentric structure, repre- sent the erosion and subsequent concentration of hematite layers which occur abundantly in the underiying Pre-Cambrian series. The quartzite (metamorphosed sandstone pebbles) are identical dKBr ifl 49 with the quartzite of the underlying Phillips formation. The occurrence of these pebbles already metamorphosed before the deposition of the Burton, indicates that a time interval existed between the deposition of the Roosviile and Burton formations. (3) The grit which overlies the conglomerate is characterized by the abundance of milky white quartz particles evidently derived from the erosion of quartz veins which are known to be present in the underlying Roosviile formation and other members of the Pre-Cambrian series. Green particles of the Roosviile siliceous metargillites are also present and since they are identical with the underlying Roosviile, it supports the idea that the Roosviile formation was metamorphosed before the Burton was laid down, hence the idea of a time interval between the deposition of the Roosviile and Burton formations is strengthen- ed. (4) The difference in degree of metamorphism of the Roos- viile and the Burton is very striking in the field. The Isimina; of the Roosviile siliceous metat^llites are so throughly cemented together that they always form steep cliiTs, in fact the perpendi- cular walls of the Elk River canyon are carved in the Roosviile formation. In contrast to this the Burton formation weathers to a soft earth and is characterized by gentle slopes. i I ! Relation of Gallon Series to the Purcdi Series. The Purcell series of the Purcell range is regarded as the western or near shore equivalent of the Galton series. Daly's correlation of the two series is as follows. I'l 50 CorrekUioH of the Purcell Series and Galton Series by Daiy} Galton Seriei, Gallon Range, 49* N. Lat. Purcell Serie*, Purcell Range, 49* N. Lat. Eroaion surface. Erocion surface. Moyie. Thickneia. 3,400+ feet Roosville. ThickneM. . 600+ feet Phillips. Thickneas. . . . 550 feet Gateway. Thickneas ... 1 , 850 feet Kitchener. Thickneas... 6, 000+ feet Gateway. Thickness.. 125 feet Syeh. Thickneas 4,000 feet Kitchener. Thickness... 1,400+ feet Creston. Thickness... .3,000 i: feet Wigwam. Thickneas... 1,200 feet MacDonald. Thickness 2,350 feet Hefty. Thickness 775 feet Creston. Thickness. ... 6 , 500 ± feet Baae concealed. Total 20,300+ feet Altyn. Thickneas 650 feet Base concealed. Total 12,100 feet Daly, in hia correlation, emphasizes the importance of the Purcell lava in the correlation of not only these two series but of all the equivalent series of the Rocky Mountain geosyncline.* This, however, must be used with care as the writer has found several lava flows separated by important bands of sediments. Correlation of the Purcell Series and Galton Series by Schofidd. Galton series of the Galton range Mountain system. of the Rocky Purcell series of the Purcell range. Roosville. PhiUips. abttnt. Gateway. Gateway. Purcell Lava. Purcell Lava. Siyeh. Siyeh. Wigwam. MacDonald. Hefty. Altyn. Kitchener. Creston. Aldridge. > Daly, R. A., Geol. Surv., Can., Mem. No. 38, 1913, Uble VIII, p. 178. * Daly, R. A., Geol. Surv., Can., Mem. 38, 1913, p. 62. SI A comparison of the above correlation tables shows marked differences. These differences primarily depend upon the position assigned to the Purcell Lava in the stratigraphy of the Purcell series. In a previous paragraph of this chapter (page 24) evidence is presented to show that the Purcell Lava occurs above the Moyie formation and not below it as Daly has postulated. The position of the Purcell Lava above the Moyie formation equates the Moyie and the Siyeh formations which are lithologically similar. The name Siyeh thus replaces Moyie in the strati- graphy of the Purcell series. The Kitchener is correlated with the formations between and including the Altyn and Wigwam because the Kitchener is correlated with the Wallace which is equivalent to the Newiand. The Newland and the Altyn both contain Beltena danai. CorrelaUon of Purcell Series with Coeur d'Alene Series. The correlation, as made by Walcott and Calkins, of the members of the Coeur d'Alene series with the Purcell series, was based upon Daly's subdivision of the Purcell series, which was subsequently found to be erroneous. The writer in 1911, care- fully examined the formations in the Coeur d'Alene district and was able to identify in that region with some degree of certainty, the formations exposed in East Kootenay. The following table shows the writer's conception of this correlation. Coeur d'Alene Series. Purcell Series. Striped Peak. 1000 Siyeh (lower part). 2000 WalUce. 4000 Kitchener. 4500 St. Retis. Rexett. Burke. 1000 1200 2000 Creston. ,sono Prichard. 8000 Aldridge. 8000 The following correlation table is based on Walcott's original table,' with additions by the writer, on the results of » Walcott, C. D., BuU., G.S.A., VoL 17, 1906, p. 17. h ^li^H •t-4 S2 field work in the Pre-Cambrian of Idaho and BritJah Columbia. The controveray centres around the age of the Siyeh limestone which is one of the most important horizon markers in the Beltian. The evidence for the determination of the Siyeh limestone as Middle Cambrian, by Daly, on stratigraphical and lithologic bases, is given in part by these words: "Walcott recognizes the Cambrian-Ordovidan equivalent of McConnell's Castle Mountain group as occurring near Belton, Montana, and Nyack creek, Montana. At these localities, massive bluish and greenish limestones, bearing a species of RaphisUma and Stromatoporoid form, were found in great devel- opment. As shown by Plate 6 of Walcott's paper, the field habit of these limestones is extremely similar to that of the Siyeh limestone at Mt. Siyeh, which is less than 15 miles distant from the Nyack Creek locality. It is difficult to avoid the suspicion that these Castle Mountain limestones are, in truth, identical with the Siyeh limestone in which, therefore. Middle Cambrian fossils may at some future time be discovered."' The discovery of very early Middle Cambrian fossils in the Burton formation 3,535 feet above the Siyeh formation, points out that the Siyeh limestone cannot be Middle Cambrian and since the Siyeh formation occurs below the unconformity which exists between the Pre-Cambrian and the Cambrian in the Rocky Mountain geosyndinal, it is concluded that the Siyeh is Pre- Cambrian in age. This conclusion is supported by Walcott in the following words: "The series of limestones at the head of Nyack creek illus- trated by Plate 6, are of Cambrian or Ordovidan age, as in- dicated by fragments of fossils that I found in them. I do not think the Siyeh limestone is to be correlated with them nor with the Castle Mountain limestones of McConnell."* >Dal I^v, R. A., G.S.C., Memoir 38, 1913, p. 183. Walcott, C. D., G.S.C., Bull.. Vol. 17, 1906, p. 19. tnbia. stone 1 the neaa >logic alent ilton, lities, es of evel- field uyeh from icion itical Mrian ithe }ints and hich jcky Pre- m tnng Uus- I in- not Hrith i^ Ctntral CorrtlaHcn TabU bv Clark and Lewia range Rocky mounuim , B.C. Purcell ranee. B.C 49th Parallel. * Coeurd „ » r> , ^^r. ^. ,ThecorreUtionoftheKtwo»ene»bytheauthori8 R. A. Daly, G.S.C. Mem.' ba*ed on Mctiona dcacribcd by Daly (G.S.C., F. C. 38, 1913, p. 97. , Memoir 38, 1913) and sulwequently modi6ed by Prof. F the author. I Lowest Middle Cambriaa I Unconformity. Erosion surface. Kintia, 800 feet. Sbeppard, 600 feet. {Roosville, 1,000 feet. PhilUps, JOO feet. Erosion surface. Gateway, 2,025 feet. Gateway, 1,000 feet. Purcell Lava. jPurcell Lava. Purcell Lava. Erosion t Siyeh, 4,100 feet. Siyeh, 4,000 feet. Siyeh, 4,000 feet. Striptd p Grinnell, 1,600 feet. Wigwam, 1,200 feet. Appekunny, 2,600 feet. MacDonald, 2,350 feet. |Hefty, 775 feet. Kitchener, 4,500 feet. WaUace, Altyn, 3,500 feet. Altyn, 650 feet. 1 i Creston, 5,000 feet. ! I St. Regis Revet t, 1 Burke, 2, iAIdridge, 8,000±feet. Prich.nd, * TabU by StkofirU. Coeur d'Alene dUtrict, Idaho. | Cabinet raofe, Moatana. . F. C. Calkin.. U.S.G.S., F. C. CalloM, VS.GS., I Prof. Paper 62. 1908. p. 25. Ball. 384, 1909. p. 40 Erosion surface. Striped peak, 1.000 feet. WaUace, 4,0(10 feet. St. Regis, 1,000 feet Revett, 1,21K> feet. Burke, 2,000 feet. |Prich.ii(l, 8,000 feet. Cambrian. Erorion tufface. Shalea and MndMonta 10,000 fMt. Striped peak, 2,000 feet. Blackfoot, 5,000 feet. Ravalli, 8,000 feet. Pridiard, 10,000 feet. Pre-Cambriaa. (Bchian). S3 PALSOZOIC FORMATIONS OF THE PVRCELL RANGE. Genbkal Statement. The Palaocoic formations occurring in the Purcell range belong to the Devonian and Carboniferous horizons. On the geological map they are grouped together, as it was impossible to separate them in the field. In the text these two subdivisions are described separately; the £>evonian b tentatively called the JeffersT limestone, and the Carboniferous the Wardner for- matioi Jefferson (?) Limestone. Distribution.— The Jefferson ( ?) limestone probably includes all of the two areas of Palaeozoic formations shown on the geolog- ical map as occurring on Gold creek. Only two areas of suffi- cient size to be mapped were found in this locality, although num- erous smaller patches occur. It is also probable that the most westeriy portion of the Palaeozoic formations shown in the vicin- ity of Wardner belongs to the Jefferson (?) limestone. This determination is based purely on lithological and stratigraphical grounds. Thickness. — ^The base and the top of the formation were not exposed in the area of reconnaissance, where the thickness was 150 feet. Lithology.— The Jefferson ( ?) limestone consists mainly of massive to thin-bedded siliceous limestones weathering grey. The weathered surf is also rough to the touch. The more sandy members are usually thin-bedded and weather a light chocolate brown. Near the contact with the underlying Gate- way formation the Jefferson ( ?) limestone is composed of brec- dated and recemented sandy limestone. Relation to Older Formations. — ^The Jefferson ( ?) limestone in the Purcell range rests with concordance of dip and strike upon the Gateway, Purcell Lava, and Siyeh formations of Pre- Cambrian age. The contact with these formations was carefully examined in numerous localities and from the following observa- I 'f :i ill 54 tions a digconformity is believed to exist between the Jefferson ( ?) limestone and the Purcell series: (1) The Jefferson (?) lin\estone rests in patches of from ... H/)-»-.. HiO— . PA... 11-50 2-M 0-7S 0-OS 0-71 0-07 9»-M > Wamn, C. H., Am. Jour. ScL, Vol. 26, 1908, p. M9. Filling he py. Migite. Ization talsof »dary char- green This blende theory rrence The char- very n one ibroua lende. xnaist uriew, luartz nerals eridte femk doritt dmcn IIM 2 M 0-7S OOS 0-71 007 I t 59 The norm calculated from this analysis is as follows: Orthodaw 4.44 Albite.. ;: 20-96 Anorthite 23 M Dmmie 26-97 HyMnthene 9.86 S»vine.. 8-16 Magnetite 3.24 Ilmenite 1.57 „, 98-93 Water o-76 99-69 Hence in the quantitative classification the rock is salfemic, perfelic, docalcic, presodic; and is, therefore, auvergnoae. The following table shows the chemical relationship of the hypersthene gabbro to other gabbtos: — ■m 1 SiOi.. TiO».. AliO,. FeiO,. FeO... MnO.. MtO.. CaO. NaiO KiOT. H,0+ H«0- PiOb . ». o... 50-36 0-90 13-63 2-22 8-38 0-20 8-67 11-50 2-54 075 0-0» 0-71 0-OT n-m 49-50 0-84 18-00 2 5' 6 2 49-38 119 18-55 2-06 8-37 0-09 5-77 9-72 259 ••2B •-» 51-68 13-88 6-59 4-44 7-87 10-99 2-93 0-81 0-74 99-93 1 Hyp«ri(lbeae gabbro of PitreeB mOa. 2. Averaf* analvm of att ■■bbraa csdudi^^rinMe 3. Average apalyaa of aO noritea.' 4. An analyst oi Karoo .. KiO... Hrf)+.. HiO-.. Pfi,.... COi.... S.G.. 2-660 The calculation of the norm of the granite gives the follow- ing results: — 8«*ft*; 39-90 9!7!"*'« 13-90 An»«*-- 20-96 Acoithite g.34 Corundum "!!."!!'! 4.59 Hypenthene 9 ■ 14 Kfagnetite '.'.'.'.'.'..'..'.'.". 1-16 Titanite !..!!!!!!!!!!!!!!!!! 1-22 99-12 Hence, in the quantitative dassification, the rock is of class persalane, order columbare. rai^ albachase, and subrang albacho%. 11 Internal Relations. 1T.e folding and faulting, to which the sills have been mbject, are evidenced by the attitude and ihe distribution of the sills now exposed in the Purcell range. As they were intruded when the strata were flat, they have suffered all the movements which have taken place in that range, so that now tiiey form anticlines and synclines with all angles of dip from to 90 degrees. The 66 ailb often end abruptly against strata which are older or younger than thoee hoiding the siUa, and in tome caset, the vertical displacement may be several thousand feet. Colum- nar jointing, perpendicular to the upper and lower contact, is especially prominent in the thick sills and is well shown in the escarpment to the north of St. Mary lake. The cross-section of .e columns is a paralletogram with 2 acute and 2 obtuse angles. The most striking phenomenon in the internal structure of the sills is a stratification of the material according to density. The stratification is of two kinds. In the example, «tudied with Daly on the International Boundary line, the distribution of material was: ua upper r ibro zone 26 feet thick passing gradually downwards into .4 granitic phase 80 feet thick, which in turn gradually passed into a luwer gabbro layer 30 feet thick. This type of differentiatiun is similar to that at Shon- kinsag described by Pirsson.* The other type was studied on St. Mary lake and consists of an upper granitic layer 70 feet thick passing gradually down- wards into a gabbro zone also 70 feet thick. All gradations exist between the granite and the gabbro, and an arbitrarily chosen type, representing the intermediate rock between the two extremes, is called the quartz-diorite. The thick basic sills also show a rough stratification in the centre of their masses, where long schlieren of acid material are elongated parallel to the contacts of the sills. The gabbro at the contacts of these basic sills is usually fine-grained, while in the centre it is coarse- grained and pegmatitic. External RELxnoNs. The exomorphic contact effects of the sills are very small, especially where the contact rock is a fine-grained argillaceous quartzite. In one case, the quartzite for an inch from the upper contact is thoroughly vitrified and charged with small needles of hornblende. Outside this narrow contact zone, the sediments are normal in character. A study of the contact under the ' PiTMoo, L.V., U.S.G.S., Bull. 237, p. 43. 67 microacope revealed three distinct but gradational bands. The normal quartzite consists of interlocking grains of quartz 0-5 mm. in diameter. This zone passes gradually into the vitreous vari- ety which shows no great signs of metamorphism, except a thorough cementing of the quartz grains whose ccmtact with each other is very indistinct and whose individuality was only detected by their optical orientation. Hornblende with greenish- blue pleochroism parallel to c and identical with the horn- blende in the gabbro, is present in this vitrified band. This zone, with a gradual increase in orthoclase and plagioclare, passes into micropegmatite in which the quartz holds the feldspar, the latter being filled with dust-like inclusions of sericite. Horn- blende, similar to that described above, and biotite, are sparingly present in this micropegmatite zone. As the hornblende and plagioclase become greater in amount, with a concomitant decrease in the quartz and orthoclase, the micropegmatite variety passes into the homblende-gabbro proper. All three zone* were se.a in one slide taken from a specimen at the contact. The cxomorphic contact action, exhibited at the lower con- tact, was studied in two localities. In the Pyramid basin, a sill 150 feet thick is intruded into grey weathering quartzite and argillaceous quartzite. The latter, at the lower contact of the sill, is impregnated at a distance of one foot with horn- blende, similar to that found in the sill itself. This hornblende is shredded in appearance and sometines occurs in radiating groups embedded in a fine groundmass of quartz grains. Mus- covite in small needle-shaped crystals is present in moderate amounts. A fine-grained variety of the quartzite occurred at a distance of 6 inches from the lower contact, and its metamor- phism resulted only in the development of a few crystals of biotite. Under the microscope, the grains of quartz, whose average size is 0-08 mm., show a pitted structure as if acted upon by a solvent. Biotite is present in a large amount. These dif- ferences in degree and kind of metamorphism of these two lamina; suggest that the texture, as well as the composition, had some influence on the contact metamorphism induced by the sill on the enclosing sediments. In the Bootleg basin, where a sill 140 feet in thickness was intruded into fine-grained, argil- MiaiOCOPV IBOWTION TtST CHART {ANSI and ISO TEST CHART No. 2) ^ /APPLIED IN/MGE I65J Eosi Mom Street «OChMt»r. m» York T4609 USA (716) 482 - 0300 - Phone ;/l6) 28e-5gW-ro» 68 laceous quartzites, the contact effects are very slight and extend ior a distance of 3 feet from the upper contact. The only result, visible in a hand specimen, is a slight baking of the sedi- ments. Under the microscope, this baking is seen to consist of a slight coalescence of the quartz grains whose average dia- meter is 0-09 mm. Muscovite, which, in general, is restricted to the contact metamorphosed sediments, is present in rod-like individuals. Biotite, common to all the sediments of the Aldridge formation, occurs in irregular masses 0-49 mm. in diameter. Summary of the Contact Metamorphism. — ^The sharp line of demarcation between the sill and the sediments is worthy of notice. The very small amount of contact metamorphism induced by the intrusion is perhaps what might be expected, when the intruded rock is a fine-grained quartzite. It consists of a baking of the sediments for a maximum distance of 3 feet from the contact, with the formation of muscovite and the transference of femic constituents from the gabbro into the quartzites for a distance of one foot. Age of the Purcell Sills. Relations of Purcell SUls to Purcell Series. The age of the Purcell sills can be definitely fixed in relation to the Purcell series. A preliminary examination reveals the fact that the sills were injected when the strata were approxi- mately horizontal, for they have been folded and faulted in the same manner and to the same degree as the quartzites which enclose them. An additional proof of this conclusion is supplied by t?.e phenomenon of stratification described above, where sills have a granitic upper portion throughout the whole upper contact. For such a phenomenon to occur, the sill at the time of intrusion must have been horizontal. The earliest folding of the region is believed to have taken place at the close of the Jurassic. Hence, the sills are pre-Jurassic in age. The youngest formation with which the Purcell sills was seen in contact, is the Kitchener calcareous quartzites. Daly' « Daly, R. A., Geol. Surv., Can., Memoir 38, 1913, p. 218. 69 described dykes and sills cutting the Siyeh fonnation; and since no observation is recorded of the Purcell intrusives, either dykes or sills, cutting fo? -jations younger than the Siyeh and the Purcell lava, the conclusion, that the Purcell sills have the same age as the Purcell lava, is worthy of consideration. Relation of SiUs to Purcell Laea. No field facts, except similarity of composition, were noted in the study of the P'rcell range, which would definitely correlate the Purcell sills and the Purcell lava. Daly summarizes his evidence for the association of these two igneous bodies' thus: "The Kintla Canyon sill and dykes crop out 12 miles or more west of the Oil Creek sill, while the Swift Current Pass locality is about 20 miles from either of the other two. Thus, at each of three widely distributed localities, we have a constant asso- ciation of an extrusive basaltic lava resting on the top bed of the Siyeh formation and an intrusive gabbroid sill rock thrust into the Siyeh itself. Though the vertical dykes, either feeding the visible sills or apparently independent of them, are relatively numerous in the Siyeh, no dyke or sill has yet been observed in the admirably exposed Sheppard formation. These facts, of themselves, afford good presumptive evidence that the Purcell lava proper is genetically connected with the sills and dykes. This conclusion is amply corroborated by microscopic study, which, even in the face of the great alteration of all the rocks, goes to show an essential identity of the principal minerals respectively occurring in intrusion and extrusion." Age of Purcell Lava. Since the Purcell Lava and Purcell sills are contempor- aneous, and since arguments have been advanced Tor the Pre- Cambrian age of the Purcell series, the Purcell sills are considered to be of Pre-Cambrian age. ' Daly, R. A., Geol. Surv., Can., Memoir 38, 1913, p. 218. 70 CorrdatioH. In a previouE chapter the Prichard^ formation of Idaho has been correlated with the Aldridge formation of East Koote- nay; hence, the sills which occur in the Prichard formation are the same series of intrusives as occur in the Aldridge quartzites of Eas*^ Kootenay. This idea is also supported by the lithology and the differentiation phenomena which are identical in the sills of the two regions. Mbtaiiorfhisii. The changes which have taken place since the consolidation of the sills have been great. The basic fades, as might be ex- pected, have been most susceptible to alteration. The augite and hypersthene of the original gabbro have been altered to both the fibrous and the compact hornblende, described above, and to such an extent that most of the gabbro is now of the hornblende variety. Zoisite is especially abundant in the hornblende gabbro. The granophyre is always relatively un- altered and whatever alteration has taken place is deep seated. Zoisite is present in small amounts and represents the decompo- sition of the plagiodase. The orthodase in some cases shows a partial transformation to seriate. Dynamo-metamorphic changes were absent in the sills in the region examined. Structure of the Sills. The Moyie SOls. One of the finest, as well as one of the most easily accessible examples of differentiated and undifferentiated sills, is exposed on the western slope of the mountain west of Kingsgate, B.C., on the International Boundary line. This section was described in some detail by Daly.* > Calkins. F. C, U.S.G.S., BuU. 384. » R. A. Daly, Summary Report, Geol. Surv., Can., 1904, p. 98A. R. A. Daly, Amer. Jour. Sci., 4th Series, vol. 20, 190S, p. 185. R. A. Daly, Festschrift zum Siebzigsten Geburtstage von Harry Rownbuich, 1906, p. 203. 71 At the time of his work in this area, through the paucity of rock outcrops, he failed to note two bands of sediment in his Moyie sills. So, instead of one sill as Daly described, there are three sills. This new Held fact, which was found by the writer in 1910, materially affects the problem of petrogenesis. In 1911, the writer guided Daly to the several important exposures and the section was again carefully studied with the results given below. The exposures are not very satisfactory and other bands of sediment may be present in sill D. The mountain to the west of King^ate consists of argil- laceous quartzites, belonging to the oldest known member of the Purcell series, dipping 60 degrees to the east and intruded by sills oi' igneous material. Sections of these sills are given in Figures 2 and 3. Tabular election of the Moyie Sills. (Measured at a locality ij miles distant from section illustrated in Figures 2 and 3.) Sills, thickneM in feet. A,315± B,52S C, 30 D, 438+ Roclc zones, thickness in feet. 100+ 50+ 100 ± 16S + 100 310 215 45 30 250 138 300+ Character of .-ock. Sediments. Gabbro. Granite. Gabbro. Sediments. Granite. Gabbro. Sediments. Gabbro. Sediments. Granite. Gabbro. Sill "A," (Figures 2 and 3) the highest in the series, consists of an upper gab! .ase of specific gravity, 2-96, having a thick- ness of 26 feet aii^ passing gradually downwards into a granite Til km! 72 (micropegmatite) interior whose specific gravity is 2 • 76. This fin- ally gives way to a lower gabbro zone of specific gravity 2 •97, about 29 feet thick. Underlying this sill occur 80 feet of argillaceous quartzites. Sill "B," of specific gravity 2 • 93, 30 feet in thickness, now occurs and in turn is underlain by 670 feet of quartzitic sediments. At this point sill "C" makes its appearance and has a total thickness of 910 feet, containing an upper granitic (micro- pegmatic) zone, 310 feet thick, of specific gravity, 2-74, passing gradually downwards into hornblende gabbro approximately 590 feet in thickness. Intervening between sill "C" and sill "D" occurs 75 feet of argillaceous quartzites. Sill "D" is 1,500 Scalaof Mll« Figure 2. Natural section of Moyie sills. See also Figure 3. feet thick, and was poorly exposed. It consists of hornblende gabbro of specific gravity, 2-99, no large mass of biotite granite (micropegmatJte) being present in thib sill. In the section at the Boundary line no further outcrops of gabbro were seen, but Daly, from his study of the region to the t»uth, postulates another sill, "E", as the lowest sill in the Moyie group of sills. A sum- mary description of the rock types mentioned above has been given under "lithological characters" and will not be repeated here. It will be noted in comparing Daly's columnar section of the Moyie sills with the one accompanying this paper, that there is a difference in the respective thicknesses of sills "C" and "D." Daly estimated his thickness in the field, while the writer obtained his results by calculation, taking into consideration the slope of the hill as well as the dip and strike of the sills. 73 Sill A laSft-thicfc Sill B aOft.thick ijumjuuJUUUumuiiAgBr ^^^^^^^ Sill C 9IOft.thick «XT)rTXV«vX».KVXV (XXKXXXXXXXXXKX (XX XX XXX XX XX XXX (XXXXXXXXXXXXXX (XXXXXXXXXXXXXX XXXX*:xx ysxxX>fXK\'j xxxxxxKX;.-) (X xxxxxxK XXX; XXXX (XXXXXXKXX XXX XKXXXXYX) XXXXXXXXXX'XXXX CXXXXXXXXXXXXXX XXXXXXXXXXXXXX XXXXXXXMXXXXXK KXXXXXVXXXXk ,tX XXXV'XXX xx> mm Sill D ISOOn^hkk mnrrTTT XXXXKli XXXXXi :xxy>xx txxxxxx " xxxxx XxXxxXXKXXXXX 'XxxXXXXXXXXXXX XXX (X^X^ XXKXXXXXXK XXX XXX xxxxx XXX XHX XXXX X (XXX i; XXXX XXXXXX'XXXXXXXX (XXXXX XXXXXXX IXXXXXXXXXXXXXX XXXXXXX XXXX XXX XXXXXXXXXXKXXX (XX X XXKX XV CXXxX XXX XXXXXXX XXXXXXX XXXVXXXX :xxxx v'xxxx kXX XXX XXXXXXX .'XXXKXXKXXXXX XX XXXXX M XXXXXXX XXV*. XXXx XX XX ■ XXXXXX X I XX XXX (XXXXXXXXXXXXXX XXXXXXXXXXXXXX XSXX VXXXXXX XXX KXX XXXXXXX XXXX XXXVXXXXXXXXXX XXX>XXXXXXXXXX xxxxx XXX XXXX XX xxxxnxxxxxxxxx XXXXXXXXXXXXXV CXXMXXXXXXXXXXX XXXX XXXX XXXX k XX XXXXXXX mCKTVPU v^B THICKNB ^•lutxita f7» ....taatt. <>bbr. te;:::: ....in ::::iJ5:::;:. »«t. soft. . ...»ft. 4u...tilta.... ... -278 lOOft. labbre... ....*■»»..... »♦», ^■vttlu.. -*70 -WO ft. (rcnita.. lBt«ri«00 -KSft. .-»» n*t. gabbro.. .&» ISOOft. qvartzH*.. -^7• jooft. Figure 3. Columnar section of the Moyie silli. 74 TJu Si. Mary SiUs. Intruded into the weiteriy dipfung Aldridge quartates, which form the mountains riring on both ndes of St. Mary lake, is a series of gabbio nils which were studied in some detail, an "A" (See Figure 4), which appoxently represents the highwt one in the series, is 140 feet thick and contains an upper granite (micropq;matite) rone of specific gravity, 2- 76, 70 feet in thickness, passing gradually downwards into a gabbro of ^Mnfic gravity, 301, also 70 feet thidc Separating all "A" from sill "B" occur 400 feet of argillaceous Fleui«4. Natnnl wctioB of the St. Mary rillf quartntes. ail "B", which is 985 feet thick, is composed almost entirely of hornblende gabbro. It is in this sill the hypersthene gabbro occurs whidi shows the transformation of augite acd hypersthene into homUende. No granitic (micropegmatitic) zone is present in tiiis sill although here and there in the centre of the sill schlieren of add material were observed. Sill "B" is separated from the underiying sill "C" by 200 feet of argUlace- ous quartzite. SiU "C" is 123 feet thick and consists entirdy 75 of hornblende gabbro. The two remaining sills observed in this section were respectively 565 and 2,165 feet in thickness, but as they were not well exposed, several bands of sediment may be contained in each of the two nils. No granite (micropegmatite) was found in these sills. Stnof AST OF Genesis. The Puroell rills represent intrurimis from a angle inter- cnistal reservoir of a series of magmafr— add magma»— which gave rise to comporite sills whose rock types vary in the same rill, from a granite (micropegmatite) to a gabbro; and of baric m fgtwM which gave rise to rimple sills of gabbro. The reservdr may be assiwied to have been stratified acond- ing to denrity, having a relatively add p(^on collected in the irregularities ajod projections of the roof and grading downwards into mofc baric materials. Cnistal movements would furnish fissures which would tap this reservoir at various levels. In this way a separation of the add and basic materials of the reservoir would occur, so that the add and baric materials would rise through separate fissures and spread out between the strata as sills. Some exotic material was gathered up from the walls of the fissures through which they passed, and in part assimilated by the riring magmas. The magmas would also probably asrimilate some of the enclos- ing Puroell sediments but not enough to materially affect their oomporitioa. 7 " simfde sills solidified in the usual manner of such intru- -r' jle the add material di£Ferentiated under the influence (. - 'ty giving rise to comporite sills. or a full discusrim of the origin of the granite (micropeg- matite) in the Purcell sills consult a paper entitled "The Origin of Granite (micropegmatite) in the Purcell rills, by S. J. SchofieM."* •'.1 L \ ■I I >& J. SdMfidd. G.S.C.. MiM. Bull No. 2. p. L ! !!■ Is; ■ i ml ii ; ;' ii !■:' 1 1 .' ■:( 1 ' n , I ■j «■ ■ i 8- !j: iiii il 76 THE PURCELL LA VA. DlSTKIBUnON. The Purcell lava, although present in the Puroell and the Rocky Mountain systems, ia restricted in its areal extent in the Purcell range to its eastern subdivision, the McGillivray range. It outcrops on Moyie mountain and the course of its outcrop is in a general southeasterly direction until it crosses the Interna- tional Boundary line, forming the eastern boundary of a syndine of the Gateway formation. The Purcell lava forms also the eastern boimdary of the syndine at the Intematicmal Boundary line. One of the finest sections occurs on the western slope of Baker mountain where three flows are exposed. The upper flow out- cropping 50 feet from the summit, is a porphyritic-amygdaloidal basalt. Below this comes 50 feet of Siyeh, purple and green metargillites u. derlain by 100 feet of non-amys^oidal, non- porphyritic basalt. The lowest flow noted consists of amygda- loidal basalt, 400 feet thick. The Purcell lava of Baker mountun extends along the eastern side of the valley of Gold creek imtil the transverse valley of Plumbob creek is ruiched where it evidently swings into the eastern part of the Kootenay valley, where it outcrops sporadically through the Glacial drift. LlTB(XX)GY. The dominant rock of the Purcell lava is usually a highly altered amygdaloidal or porphyritic basalt. The flows generally heterogeneous in character. The one exposed on Gold creek, about 10 miles south of Cranbrook, gave the following cross section: — Amygdaloidal baaalt |?f!!!' Amygdaloidal-porphyritic bawlt M f eet approx. Porimyritic bualt 50 ^ Breccia (baaalt) ** The amygdaloidaljbasalt is dark~green to black in colour, diot through with numerous amygdules filled with quartz M* 77 and, more rarely, hematite. The weathering colour it dark rusty brown. The porphyritic basalt has a greyish green colour and is remarkable for the size of the plagiodase phenocrysts Oabradorite) embedded in a groundmaas of labradorite and decomposed hornblende. The labradorite crystals vary in size from a fraction of an inch to 1) inches in leng^ and make up the greater part of the rock. All "-vdatioBB exist between the amyg- daloidal and porphyritic ty|.js. The lower part of the flow strongly resembles a vokanic breccia and is composed of angular and subangular masses of amygdaloidal and porphyritic basalt. Possibly, however, it is a flow breccia formed by the incorpora- tion in the flow of soUdified surface material. Very little is revealed by a microscopic examination of the lavas because they are so highly altered. The feldspar is piobably labradorite and is embedded in needles of secondary homUende, zoisite, and epidote. The amygdules are generally filled with quartz of fibrous nature with the fibres or crystals normal to the surface of the amygdules. Caldte and hematite also were noted filling the amyt^xdet. The following chemical analysis of the porphyritic type ot the Purcell lava of the Purcell range, is given by Daly.* SiOt. 41-50 T'Ot- 3-33 AliOi IT-W Fe/>, 3-31 f«0 10-08 MnO. trace MgO. 12-74 Sp.Gr. c«o. 0-97 Na,0 2-84 K,a. :...... 0-22 HiOat 116*C 0-21 H|0 above llO'C 6-99 CO.. PrfJt 1.08 100-36 2-792 t '.H i r Thickness. The thicknesb he flows varies from 50 to 300 feet in the Purcell range. External Relations. The Purcell lava generally rests conformably on the under- lying Siyeh formation, but in some cases, as in the Baker Moun- > Ddy, R. A., fieol. Surv., Can., Memoir 38, 1913, p. 209. -•It 78 tain section, several flows occur interbedded in the Siyeh for- mation. The Gateway formation rests conformably upon the Purcel' lava. A detailed study on the eastern extension of the Yahk Mountain ridge exposed, gave the following section: Fine argillaceoui qusruite 10 feet Fine conglomerate 1 foot Coane conglomerate 6 inches Amygdaloidal baaalt The upper surface of the lava is irregular, showing flow structure. Resting on this surface is a conglomerate composed of rounded fragments of fine-grained basalt in a sandy cement. The fine conglomerate also consists of volcanic material in an argillaceous cement. Ace. The Purcell lava was extruded on the surface of the Siyeh metargillites and since arguments have been advanced for the Pre-Cambrian age of the Siyeh formation, the Purc^'i lava is considered to be of Pre-Cambrian age. GRANITES. Distribution. The rocks grouped under this nari'wi are very constant in mineralogical character. As shewn by the accompanying map, they occupy only a very small portion of the map-area. The apparent distribution of nearly all the stocks along lines of fault- ing, cannot be accidental ; rather it is believed that this faulting opened up the fissures through which the magma was given op- portunity to rise and form the stock-like masses now exposed by erosion. The bodies are circular to elliptical in outline with flowing contacts. These stocks vary in size from 200 feet to 2 miles in diame.'-er An exposure of a hornblende variety of the granite is foum* i.e road from Cherry creek to the St. Eugene Mission, aLout 4 miles north of the Mission. Here, it is some- 79 what porphyritic in character, the large phenocrysts of orthodase being embedded in a groundmass of quartz nnd feldspar. At Bradfords quarry, 1 mile north of Wycliffe, a true porphyritic granite is exposed in .-. small cross-cutting mass, 200 feet in diameter. A micaceous variety of the granite is well exposed on the valley walls of Hall lake, where it has a surface exposure of 4 ScsJe of Miles X -i |r<''<>| Porphyritic granite Figure 5. Gtanite intrusion on Hells Roar-ij, rreek intrusion methodk E-E^ Crestc- formation L>e>: ii gl:owiag square miles. In the ridge on the east side of the lake, the downward enlargement of the stock can be clearly seen. The methods of intrusion of these stocks were studied at the head- waters of Hells Roaring creek (Figure 5). if 80 The apophyses related to the granite intrusion are not very numerous. They consist of the complementary rocks, aplite and lamprophyre, with a minor number of coarse pegmatites. Very frequently these dyke rocks are intruded along the bed- ding planes of the sediments and also cut the granite stocks themselves. The complementary dykes, which can be seen to advantage around the stock at Hall lake, are generally very narrow, having a maximum determined width of 15 feet, while some of the pegmatites are 200 feet wide and occitf intruded along the bedding-planes of the quartzites. In the neighbourhood of Elko in the Elk River canyon a dyke of granite porphyry cuts the Roosville formation. The pegmatites are well exposed on the west slope of Hells Roaring creek at an elevation of 5,000 feet. The stocks increase in number and size towards the west, where the Nelson batholith occurs, with which these stocks in East Kootenay doubtless have satellitic relations. LiTHOLOGY. M Megascopically, the granites are all light grey in colour. They are characterized by the presence of large phenocrysts of pink orthoclase feldspar. These phenocrysts are sometimes an inch in length, elongated parallel to the C axis, and in many cases show plainly the Carlsbad twinning. Quartz is very abundant and with the white coloured feldspar plagiodase, occurs in the groundmass. The femic constituents consist of either biotite or hornblende, or both in varying proportions. A more basic variety of the granite, a contact phase, in which hornblende is represented by augite, occurs in the granite at Bradfords quarry. Under the microscope the hornblende and biotite granites are seen to have a hypidiomorphic granular to a porphyritic texture. Orthoclase feldspar occurs in large amount and generally in idiomorphic crystals elongated parallel to 010. Twinning, according to the Carlsbad law, is very common in the orthoclase. The striated feldspar, which gives a maximum extinction angle of 15 degrees, by the statistical method of Michel Levy, and has a lower index of refraction than quartz, is oligoclase-albite. Zonal structure, with the more basic variety as the core, is char- 81 acteristic of the plagiodases. The core is usually formed of basic oligodase, gradually becoming more acidic towards the peri- phery, which is generally composed of albite. The basic core is very often decomposed. Quartz, filling the interstices of the other minerals, is abundant, especially in the biotite granite, which, by the Rosiwal method, contains 28-7 per cent quartz. Biotite, the coloured constituent of the biotite granite, occurs in plates which show strong absorption. In the hornblende gran- ites, the hornblende occurs in hypidiomorphic crystals. Microcline and perthite occur as accessory constituents in all the granites. Titanite is rather rare and shows its usual diamond-shaped cross-section. The following analysts of the Nelson granite, which is related to the granites of East Kootenay, is given by R. W. Brock.' SiOi TiOiAliO,FeiOiFeO CaO MgO NaiO KiO H,0 P,0| 66-46 0-27 15-34 1-68 1-83 3-43 Ml 4-86 4-58 0-29 008 ^99-93 Brock says, "The Nelson granite, which has been carefully studied, is a sort of gramte representative of the monzonite group of rocks, intermediate between the ailkali and the lime-soda series of rocks, and about on the boundary line between granite and diorite." At Bradfords quarry, north of Wycliffe, the contact phase of the granite was found to be a quartz augite diorite which passes by gradual transition into the normal porphyritic granite. The orthodase and the plagioclase, the latter with zonal growth, are in equal amounts. The femic constituent was originally augite, which has been changed to secondary hornblende. Some rem- nants of augite occur as cores in the hornblende crystals. The augite is non-pleochroic and has an extinction angle of 45 degrees. Titanite and apatite are quite abundant in idiomorphic crystals. Calcite, which is considered to be an original constituent, occurs filling the interstices of the other minerals. This basic phase of the granite was only noticed in contact with limestone. In contact with the quartzites, the contact phase was even more siliceous than the normal granite. ' Brock, R.W., G.S.C., Vol. 15, 101 A. 82 Stkcctural Features. Internal. Brecdation and jointing are very prominent in many cases and in the granite stock at Hall lake, blocks 6 to 10 feet square cover the slope of the valley. The granite bodies, in general, are remarkable for their homogeneity. In the larger masses, which have been exposed by erosion to some depth in the magmatic chamber, no basic conUct phase is present, although the contacts with the surrounding sediments are well exposed, especially at Hall lake and on Hells Roaring creek. In the case of the small intrusive mass, 200 feet in diameter, at Bradfords quarry, a well marked contact phase exists. As previously stated, the main mass consists of typical porphyritic granite, which, as the con- tact is approached, gives way to a quartz-augite diorite when in contact with limestone. \\^en the granite cuts the quartzite, a fine-grained acid phase is present, which contains phenocrysts of feldspar, ranging from albite to basic oligodase. These phenocrysts are common in the normal granite, embedded in a fine-grained groundmass of quartz and feldspar. Whether this phase is a fine-grained granite or quartzite impregnated with materials from the granite, could not be determined. The basic contact phase, described above, was coarse grained and contained caldte in such an amount and in such relations that it is believed to be either primary or to have been assimilated and recrystal- lized limestone from the surrounding sediment. This basic phase may be the normal condition at a horizon at this depth and may represent the original composition of, or is perhaps a little more basic than the intruding magma which cooled rather quickly along the contact. On the other hand the interior of the mass was differentiated by fractional crystallization, with the result that the alkalis and silica were concentrated in the upper part of the magmatic chamber, giving rise to the porphyritic granite, while the heavier femic constituents sank to a deeper part of the chamber. 83 External. Granite intrusions cut the members of the Puttxll series but its relation to the Mississippian limestone of the Kootenay valley is unlotown. The contacts of the granite with the sur- rounding sediments are well exposed, and show that cross-cut- ting relations exist beyond doubt. Many apophyses of the granite penetrate the sediments near the contact. The contact metamorphism induced by the intrusive on the surrounding sediments is not of high order. There seems to be a gradation in metamorphism, decreasing in amount as we pass from the roof of the stock into the deeper parts of the body. Around the larger masses of granite, which in the region examined never exceed 2 miles in diameter, contact metamorphism is slight, the only visible effects on the quartzose sediments being the forma- tion of knotted schist in an aureole around the intrusive for a distance of 500 feet. Under the microscope, it is seen that the sediments are very little affected and that the knots are composed of indeterminable collections of fine-grained dark material having no crystal ouUines. In the small stocks, about 750 feet in diam- eter, the contact is peculiar. As mentioned above, in contact with the quartzites an aplitic phase is present, while against the limestone a basic phase, quartz-augite diorite, occurs. The lime- stone, in this vicinity, has been changed to a white crystalline marble, free from impurities except dose to the contact, where it is charged with the contact metamorphic silicates, garnet and epidote, which at times form small veins or stringers in the marble. Associated with the garnet and epidote, are the sulphides, chalcopyrite and pyrite. The quartzites within 200 feet of the contact have been changed to a dense compact chert by infiltration of silica from the granite or by the rearrangement of the sihca of the quartzites. Masses of granite smaller than 200 feet m diameter were not found, but the area of garnetiferous mica schist, described above, is believed to be the result of contact metamorphism of argillaceous quartzites by a granite mtrufflve, which has not been exposed by erosion or, in other words, the schist is the roof of a granite stock. From the above, it is seen that contact metamorphism has been greatest 84 at the roof and gradually diminishes as we descend into the deeper contacts. Evidently the agents producing contact metamorphism must be in greater abundance near the roof, These agents are believed to be the volatile constituents of the magma which collect in the upper part of the magmatic chamber. Age and Correlation. As the youngest sedimentary formation, with which the granites were found in contact, is Beltian (Pre-Cambrian), the age of this intrusive can only definitely be placed as Beltian oi younger. In studying the relations which the granite bears to the folding and faulting, it is seen that it is younger than the chief orogenic movements which affected the region. Argu- ments have been advanced in a later ch pter for a post-Jurassic age of these movements, hence the intrusion is probably post- Jurassic. Investigations by other workers, in adjacent districts, have thrown additional light on this complex problem. In West Kootenay, McConnell' found a granite similar to that ol Efist Kootenay, cutting all the series in that region from the Shuswap crystalline complex to the Slocan slates; the latter are considered to be Pennsylvanian in age. In the Bitter-root and Clearwater mountains of Idaho, Lindgren* describes a porphy- ritic granite of a light grey colour, containing crystals of ortho- clase 3 cm. in diameter, which he holds as certainly post-Car- boniferous; and, as it cuts the sedimentary series on the south fork of the Clearwater river near Harpsler, which is very prob- ably Triassic, the granite may be considered as of post-Triassic age. Again in the Silver City folio of Idaho*, Lindgren and Drake correlate the granite intrusion in Idaho with the granites in the Blue mountains of Oregon and thus date it as post- Carboniferous and probably post-Triassic. From andogy with similar granite areas in Montana and California, this intrusion may very likely be assigned to the Cretaceous period. In his paper "The Gold Belt of the Blue Mountains of Oregon," » McConneU, R.G., G.S.C., Vol. 9, 1896, p. 19a. • Lindpen, W., U.S.G.S., Prof. Paper, 27, p. 20. » U.S.G.S., Geol. Atlaa of U.S.. FoBo, No. 104, 1904. 85 Lindgren' places the date of the granite more specifically where he states "that the granite intrusion is certainly post-Triassic and pre-Neocene and is likely post-Jurassic and pre-Chico when it is compared with the intrusions in California." SUPERFICIAL DEPOSITS. The greater part of the Cranbrook map-area is covered with drift, especially the Rocky Mountain trench and the valley of Gold creek. From their character and distribution, the records are interpreted as belonging to two glacial periods separated by a period of glacial retreat. The interglacial deposits are remark- able for their content of a flora whose modem representatives are indigenous to a climate warmer than that of the southern United States. The deposits, Pleistocene and Recent, can be subdivided as follows. Recent Pleistocene. .Post Glacial epoch. Valley alluvium. Delu deposits. . WycUffe Glacial etoch. Stage of glacial retreat. Marysville sands. Stage of glacial occupation. Wycliffe drift. St. Eugene inlertladal (?) epoch. St. Eugene silts. PLEISTOCENE DEPOSITS. The Pleistocene deposits in the neighbourhood of the Rocky Mountain trench (Kootenay River valley) can be classi- fied under two main heads, viz.: the Wycliffe drift named after the town of Wycliffe on the branch line of the Canadian Paafic railway from Cranbrook to Kimberley, and the St. Eugene silts named after the St. Eugene mission. A detailed section measured on the east bank of th- St. Mary river about 3 mUed east of Wycliffe gave the following results: 'Undgren, W., 22nd Ann. Rept. U.S.G.S., Pt. 2. 1901, pp. 551-776. ? 1 i 1 i f i 86 EroMon lurface. Recent A. Stratified aand 15 feet. Marytville sand*. Unconformity. PleiMocene B. Till 30 C. Stratified Hit 25 D. • gravel 15 E. • silt 5 F. Unstratified coane gravel (till?) 25 G. Stratified sandy clay fC fossi' plants H. Stratified gravels, lignite 60 Base unexposed Wydiffe urift. St. Eugene silts Member A of the series consists of stratified sands deposited in quiet water which filled the depressions in the underlying glacial drift. The maximum thickness of this member is 15 feet. Member B is true till and is unstratified. The most striking characteristic when a section is viewed at a distance, is its dark grey colour which is in marked contrast to the under- lying creamy white silts and overlying slightly grey stratified sands. The boulders in the till, composed of gabbro and quartz- ite, are as large as 2J feet in diameter. Member B rested with an irre<{ular surface contact on the stratified silts. Member C consists of creamy white silts very finely stratified and in general entirely free from pebbles. Member D is composed of boulders of quartzite and diorite and is plainly stratified although very Uttle sandy material is in evidence. Member E very closely resembles member C as it consists of finely stratified creamy white silts. Member F, 25 feet thick, consists of imstratified, very coarse gravel which strongly resembles till. The boulders which are as large as 2i feet in diameter, consist of gabbro and quartzite. Tit : structure, character of the pt jbles, and composition of the material characterize it as true till; but, on the examination of sections of the same Pleistocene material 1} miles east of this locality, this member was absent from the series. Whether or not this member represents a r^onal deposit of till, can only 87 be d«nded by further work in the Kootenay River valley where the Pleistocene u well exposed in the river banks. Member G consiste mainly of finely stratified silts and clay with some gravel The more clayey members near the ba« contain, between the lamina, numerous well preserved plant remauis of the Pleistocene. ^ M.^''"!^ ^'' composed mainly of stratified gravel consisting chiefiy of quartzite and quartz pebbles with a minor quanti? jrfdiontepebbe-. The pebbles are on an average two-thirdsT« inch m diameter and are well waterwom. The exposed surface of the graveb has a rusty appearance and they lookoTder thS it^ir'l' -"^ "^"J"^ P^ °^ ^* section.%mall sean»^ hpute and piecesof hgmtued wood occur in the gravels associated X^'^'^^- ?«'°'*^P^°fthesegravelsisunexpoS m this section, but 3i miles west on the St. Mary riverS^ oT^^^dt^^^''^^ "-^ ^^^^'^ ^- "^ the^Jsllifl^^ Fossil Content of the St. Eugene Silts. for iT"uf'T ~"t^ ^ *•'* ^'- ^"8«"« «'*» ^^ submitted * I.vJ''* ""r*^/" '''*^'''' *•"* P'^' remains are contained is JaiSi^rTi"^"''-^"*"^ '""y- "^"'"-^ considerable care 4 handling. The speamens are. for the most part, comparatively weU preserved, although a majority are fragm^n^ S nSrT'""*'^ "' ''" ^ """'"^ ^ com'pared^th the TnTiL ^P*?™^'"' «^e° " the unidentifiable fragments are mduded as distinct species; and two genera, Fagus SZn^, anout a third of the entire collection. foUo^Js^'**™**''' arrangement of the material identified is as ' I il 88 ll ■«: Antiosperma$. MonoeotyUaonae. Fragment of a large leaf, with obscure parallel nervatio («L). Fragment of a stem, with well-defined longitudinal striatic (43K). Both of these fragments are evidently monocotyledonou but they are too indefinite for either generic or family identifio tion. The leaf is somewhat suggestive of a palm or a yucc and the other fragment has some resemblance to the petio erf a palm, but the characters are too superficial to be of ai diagnostic value. Juglandaceoe. Hicoria. n. sp. ? (43A, 43P in part). This is a leaf which is hardly to be distinguished from tho of and Drysdale* who found them near Ashe. oft underlain by an older boulder clay. If this correlation be OMTect, the St. Eugene sIIls are intergladal. « Dawson, G. M., G.S.C. Ann. Rep. 1894, p. 251B. • Dry«dale, C. W., G.S.C, Summ. Rep. 1912, p. ISO. M 93 CHAPTER IV. STRlICnmAL GEOLOGY. The iouthern part of the Purcell range is a region district, are the result of the first recognized defo?.iiation in th« region. This conforms to the general rule that compression ii the first step in the production of a mountain range, in gem..al they are simple in character and can be recognized in the fielc by the direction and distribution of the strikes and dips. Thes* folds are the result of compressive forces acting in an east am west direction. Following this movement there was a period o tension whose results are expressed in the normal faulting whicl followed the folding. The Moyie range, the most westerly subdivision of the Pur cell Mountain system, in general is a simple, easterly dippini monocline composed of rocks of the Aldridge formation cut o( to the east by the Moyie fault. To the east of this fault, occur the Yahk anticline, the controlling structure of the Yahk range Its marginal portion is composed of Creston argillaceous quartz ites, while its axial portion is made up of the Aldridge argilla ceous quartzites. The eastern limb of the Yahk anticline is modi fied by the formation of the Yahk syndine whose basement, a exposed in the field, consists of Creston argillaceous quartzite while its axial portion contains lower members of the Siye formation. The McGi"vr''/ range, the most easterly subdivisio 93 of the Purcell tystetn, is dominantly a •hallow syncline along whose axis are exposed the lowc members of the Gateway for- mation, while its marginal portion shows successively older members oc*.— Although sediments of this epoch are i present in the Purcell range, there is reason for supposing tl they were deposited and subsequently removed by erosii They were examined in the Rocky Mountain system at Ell B.C., located on the western edge of the Rocky mountai Since the sediments consist of chocolate brown and green sar argillites earing mud cracks and ripple marks they were pr( ably deposited under continental conditions. Roosvilk Epoch.— Ho sediments representing this epoch present in the Purcell range. In the Rocky mountains, they mainly greenish grey, laminated, siliceous argillites, contain abundant ripple marks and mud cracks, suggesting continer conditions of deposition. ^1 J| m' Cambrian. In the Rocky mountains to the east, an unconformit: recorded between the Roosville of Pre-Cambrian age and Burton of Cambrian age. In the Purcell range, an unc formity exists between the Devonian limestone and the Gatei formation of Pre-Cambrian age. As stated above, the Phil and the Roosville formations are lacking in the Purcell rai These rocks have been eroded during the interval between Roosville and the Burton and their detritus is represented the Burton and Elko formations of the Rocky mountains, in the Purcell range there is an interval of erosion between Gateway and the Devonian which has removed the Phi and the Roosville formations, with the result that the Devo rests upon the Gateway. Devonian-Carboniferous Epoch. After this period of erosion, during which time about i feet of strato were removed from the horizontal Pre-Caml n .. 101 beds, the Devtmian sea spread over the eastern part of the Purcell range. The western limits of this sea cannot be de- fined. Similar marine conditions evidently prevailed up to and including the Pennsylvanian period. The deposits of the Devonian-Carboniferous epoch are mainly limestones with minor amounts of argillaceous and quartzose limestones. Jurassic. No record of sedimentation is present in the Purcell range during this period; but to the east the Femie shales form a con- formable part of the Palaeozoic-Mesozoic series. Regarding its deposition or non-deposition in the Purcell range, no evidence has come to hand. ', i « Late Jurassic or Early Cretaceous. The next event recorded in East Kootenay is the folding and faulting which affected the above-mentioned horizontal sediments. The first movement was one of compression which caused the region of the Purcell range to be raised above the sea and to form an area of erosion. At this time the dominant structure of northeriy striking anticlines and synclines of the range was treated. This period of compression was followed by one of tension and is evidenced by the occurrence of normal faults which truncate the anriclines and synclines. The strike of these fault lines is northeast-southwest. This folding and faulting were accompanied by an intrusion of granitic magma which apparently slowly replaced the overiying sediments by over- head stoping.» These granitic masses occur in the neighbour- hood of the main faults of the region and probably have some genetic . ;rions to them. The uprise of the magma may have been aided by the down sinking of fault blocks, similar to that d^bed by Clough, Maufe, and BaUey in Scotland*; only, ' Daly, R. A., Am. Jour. Sci., Vol. IS, 1903, p. 269. • ri u "T".,^'"./""''- Sci., Vol. 16, 1903, p. 107. I p.611 *^' ^- ^- "*"f*' "• ^- S^'-^y- E- B-. QJG.S.. Vol. 65, 1909. 8 102 the blocks in East Kootenay would be very much larger. The age of this deformation and intrusion is placed in the post- Jurassic, for reasons given under "Structure." Following the intrusion of granite, with no great interval of time, came the intrusion of numerous dykes of aplite and pegmatite. During the cooling stages of the granitic magma ocairred the deposition of the lead-silver ores of the St. Eugene and Sullivan mines. .« #; i Cretaceous Erosion. After the Jurassic uplift which formed the Purcell range no record of younger sedimentation other than the Pleistocene has been found. During the Cretaceous period, erosion was yen active in wearing down the Purcell range and in depositini most of the eroded material in the CreUceous geosyncline, whicl covered the area now occupied by the Rocky Mountain systen and the Great Plains. Erosion had proceeded so far at the closi of the Cretaceous and early Tertiary that the Purcell rangi was reduced to a land of low relief or to a peneplain, which migh be called the Purcell peneplain. Tertiary. In early Tertiary times, the Cretaceous geosyncline to th east of the Purcells was mountain-built with the formatio of the Rocky Mountain system. At the same time the Puree range, characterized by a rolling monotonous landscape, wa uplifted without any deformation, thus rejuvenating the streair which proceeded to entrench themselves into the Cretaceoi peneplain. The valleys, now seen in the Purcell range, ai due to Tertiary river erosion. The course of Gold creek i eariy Tertiary times, differed widely from that of to-day. Coi nell creek and the West Fork and South Fork of Gold creel .flowed eastwards through the outer range of hills to join t\ Kootenay, independenUy. Later, the present Gold ere* eroded along the present Gold Creek valley and captured tl various branches of Gold creek, leaving "Wind gaps" throug the eastern range of hills. M 103 QUATEKNAKY. The Quaternary history may be divided into four main divisions as follows: 1. First Glacial period. 2. Intergladal period. 3. Second Glacial period. 4. Poat-Gladal and present period. The records of the first Glacial period, if ever present in the Purcell range, have been removed during the erosion periods which followed this advance of the ice. The depoe' on of the St. Eugene silts of the intergladal period, took place in a lake which once occupied a great part of the present Kootenay valley. The climate after the first retreat of the ice, as indicated by the pUnt fossils found in the St. Mary silts, was, according to Mr. Arthur Hollick, milder than that of middle United Statra. This penod of comparative warmth was followed by another refrigeration of the whole Cordillera, and during this tune the Wycliffe drift was deposited. The southern part of the Cranbrook area was covered with ice, flowing, in general, southwards. A few monadnocks like Yahk mountain projected above the general ice-level. In the country north of Perry creek the glaciation was distinctly alpine. The main movement of the ice was governed by the direction of the main valleys, the two main valleys being the Rocky Mountain and the PurceU trenches, which received tributary ice streams from the moun- tains on each side of these valleys. During the time of the disappearance of this ice-sheet, the ^ clays which he in the depressions in the Wycliffe drift, were j deposited Later, the streams cut down their channels into the deposits of clays sands, and gravels, giving us the present topog- raphy of the valley floors. i- I r?l 104 CHAPTER VI. ECONOMIC GEOLOGY. The Cranbrook area contains varied deposito of econor value and nearly all of theae are in the first stages of deveh ment. For the last derade this territory has been the larg lead producer in Canada, having within its confines the No Star and St. Eugeae mines, which are now almost exhaust and the Sullivan mine aow rapidly coming to the front as a la producer. For facility of description, the ore deposits classified according to the nature of their final product, whi however, has in most cases a direct connexion with the ori of the ores. The following economic deposits are found wit the Cranbrook area. I. Metallic. Silver lead. Gold-quartx. Gold-copper. Iron. Placer sold. II. Non-metallic, (a) Clay. h . 105 MINERAL PRODUCTION OP EAST KOOTENA Y. {Port SuOt Minini Dwiaion.) ToUl Placer I.od« SUver. 1 Lwd. productioii. gold. gold. 1874 « t 50,000 1 t • 1875 41,890 1876 25,000 1877 37,000 1878 25,400 1879 19,000 1880 19,500 1881 25,000 1882 29,500 1883 28,100 1884 57,862 1885 55,250 1886 50,000 1887 29,350 1888 36,350 1889 36,300 1890 37,400 1891 28,550 1892 29,700 1893 19,700 1894 24,900 1895 17,575 878 1896 1897 1898 1899 1900 1901 1902 1903 1904 1905 1906 1907 1908 1909 1910 1911 1912 154,427 163,796 133,308 64,393 2,210,151 1,541,969 200,188 61,848 1,152,487 2,712,252 2,940,744 2,321,121 1,467,481 1,340,585 1,217,792 853,122 953,728 1,054 12.000 ,000 10,000 10,000 12,600 33,000 20,000 20,000 14,160 10,400 10,000 3,400 3,000 3,000 3,000 2,000 124 49,443 69,760 38,623 18,970 560,305 402,333 56,738 14,491 314,923 652,342 665,931 509,740 322,340 283,911 254, ""9 167,231 217,821 8J,908 82,0'6 77,745 35,423 1,639,848 1,127,036 110,450 27,357 817,564 2,045,750 2,264,413 1,801,257 1,141,741 1,039,674 954,983 682,891 733,907 m 106 SILVER-LEAD DEPOSITS. ■ J ip' DISTRIBUTION. The «lver-lead deposits at present are by far the most If portant economic deposits in the region. They occur, with f( exceptions, associated with the Aldridge formation and with tl more quartzitic phases of this group of rocks. The ores ge erally consist of an intimate mixture of the sulphides pyrit pyrrhotite, and galena, either as fissure veins or replaceme deposits in argillaceous quartzites. The gangue, usually sm; in amount, includes garnet, diopude, caldte, and quartz. Wit in the Cranbrook area, two districts include most cf the importa mines, the Moyie and the Kimberly districts, the former co taining the St. Eugene, Society Girl, and Aurora, the latt« the Sullivan, North Star, and Stemwinder mines. Several otli deposiU of minor importance occur throughout the region. MINERALOGY. Under this heading will be given the minerals occurri in the silver-lead deposits, arranged according to Dana's systi of classification. Native Elements. SUver. — Native silver occurred in the oxidized zone in 1 North Star mine as arborescent and reticulated aggregates cavities in limonite. It is silver white when first exposed, 1 tarnishes to a greyish black on exposure. The presence native silver is probably due to the general rule formulated Cooke' that the "enrichment of a primary silver deposit brought about by reactions of silver or its sulphides with i sulphides of iron and their products of oxidation . . . Sulphu acid and ferric sulphate" (derived from the oxidation of pyri "exert a powerful solvent action both on silver sulphide and its companion sulphides, such as galena, chalcocite, orpime »Cooke. H. C, Journal of Geol., Vol. 21, 1913, pp. 1-28. 107 and Btibnite. Of these, •ilver :;ulphide is the least affected. " And further he says: "A mixture? of sulphuric acid and ferric sulphate has a powerful solven'. ^tion on metallic silver .... Equilibrium in silver-bearing solutions between ferric, ferrous, and silver sulphates ia such that the reduction of ferric soluticTis to the ferrous condition by any means will rapidly precipitate the silver in metallic form." Sulphides. The sulphides of iron, lead, and zinc comprise almost the entire ore content of the silver-lead deposits. Galena, PbS. — ^Sulphide of lead is the most important mineral, as it contains not only the lead values but the silver values as well. In general, it is the fine grained, steely variety so well known in the Sullivan ore-deposit; but, it often occurs as the coarse cubic variety which constituted the ore-bodies of the North Star and St. Eugene. In general, the galena is silver-bearing, carrying from 3 to 4 ounces of silver to one per cent of lead. Zinc-blende, Sphalerite, ZnS. Sulphide of Zinc— Sphalerite is always present in greater or less quantities in all the silver- lead deposits. In the Sullivan it is intimately associated with the fine-grained galena and iron s> RaMome, F. L., U.S.G.S., Prof. Paper 62, p. 184. 114 shows some iretamorphism due to the intrusion of the monzonite . . . In consequence of it, the rock usually has a gree colour, due to the development of minute grains of pyroxem or in a few places a pink tint where garnet in microscopic crystal is the principal contact metamorphic mineral. The microscop shows that the quartzite is completely recrystallized to an aggre gate of interlocking quartz grains which enclose variable proper tions of the pale green monoclinic pyroxene, green brown biotitc white mica (probably muscovite), and garnet. The associatioi of the ore minerals with the metamorphic silicates is so clos that the conclusion of their contemporaneous genesis is unques tionable. . . . The microscope reveals the presence her and there of a little carbonate, apparently calcite. The fore going characteristics indicate that the ore of the Granite min was deposited shortly after the intrusion of monzonite and is ; phase of contact metamorphism." A comparison of the description of the Granite or Succes mine of Idaho with that of the Sullivan of British Columbii given above shows a striking similarity. Both deposits an replacements of argillaceous quartzites by an intimate mixtun of zinc-blende, galena, and iron sulphides, the latter increasing towards the periphery of the ore-bodies. The gangue minerali are almost identical in the two cases; but, in the Sullivan, thi contact metamorphic silicates are restricted entirely to the on masses, while in the Granite or Success mine, the enclosing quartz ites are heavily charged with these minerals. Therefore, it is concluded that the Sullivan ore masses were deposited undei conditions of temperature and pressure less extreme than thos« under which the Granite or Success ore-bodies were formed. Alsc the fact which is especially worthy of emphasis is the presence ol an intrusive monzonite genetically related to the ore deposit in the Granite or Success mine, while in the Sullivan no sucli intrusion is known; but, from the similarity of the deposit in mineralogy and relationships, such a mass is doubtless present, although probably too deep to be exposed in the future workings of the mine. With a further decrejise in temperature and pressure the conditions, under which the St. Eugene of East Kootenay, the 115 Eight, and B.B. ore-bodies of Idaho* were deposited, are reached In these deposits pyrite, pyrrhotite. and the contact metamorphic silicates are less abundant and calcite more plentiful than the Sullivan and Granite ore-bodies. With the entire disappearance of the above silicates and a notable increase of carbonates, which point to conditions of deposition less extreme than those of the St. Eugene, we have the Tiger-Poorman Lode* described by Ransome as follows: "In the Tiger-Poorman *uid Standard-Mammouth mines Eidente is only moderately abundant and the ores contain notable quantities of sphalerite and pyrrhotite. Pyrite and chalcopy- rite are comparatively abundant in both mines." The Wardner mines represent ore-bodies deposited under the least extreme of any either in East Kootenay or the Coeur d'Alenes. Concerning these deposits* Ransome summarizes as follows: "In the Wardner mines siderite is more abundant than else- where in the district. Sphalerite is rare, pyrite subordinate and pyrrhotite unknown. Garnet, biotite, pyroxene, and magnetite are entirely absent from these deposits." Thus the evidence regarding genesis brought to light in the study of the silver-lead deposits of East Kootenay supports the view advanced by Ransome in 1908 concerning the origin of the silver-lead deposits of the Coeur d' Alenes. The following table is a summary of the relations existing between the deposits of East Kootenay and the Coeur d' Alenes and showing their probable relations to decreasing temperature and pressure. J MacDonald, p F., U.S.G.S. Bull. 334, p. 99. ! ,ToS'5- P™'- Paper 62, p. 136. •U.S.G.S.Prof.Pa^er62 p. 136. • -• i< #^; II 8 z Q d i 116 lEst Hl"Sji. n I -^5 pi hi i •b|*I . 1 ■ 1 m 17 r^ ^. I SB 11 has P 11 i ill! 1^ Jr. nil 1^ 1i Hi 111 I I CQ I 11 ii! a il If -• - AGE OF THE DEPOSITS, Since the silver-lead deposits are thought to be genetically assoaated w,th the granite intrusionsof Eas^Kootenay and See hese intrusions are correlated with the Jurassic ( ?) Ne Si Jan FUTURE OF THE SILVER-LEAD DEPOSIl^. wuh the Aldndge argillaceous quartzites. as if these quartzites were favourable for the deposition of silver-lead ores If tS ^dn™dl; f T'''°°« "^^' ^'"« ""^^''^i" fo^ -ost irt by the Aldndge formation, offers a wide field for prospecting work contentT-"'"?''"! °' '''' ^"«^^"' -paracio/ofThe high ^ Ss^nT '" '^'f-'':^'^<^ °'^ is solved. rene^-Kl actiSJ wiU be seenin several deposits now in a state of quiescence. Descripdoa of Mines and Prospects. THE MOYIE AREA. and ^d^y^telLTt^lS ttT^"""'.^"^'^°^'^ '^'^ Mabelle daL. !i. A ^ Girl. St. Eugene, the Cambrian and Mabelle claims, the Aurora, and the Guindon group of claims. Geology. The Moyie area is underlain by the Aldridee and Cr^.tn. riT;; T!-""'"^'' ""^^- '^^ formatLrare^S ^ Sncides wfh'th" ';PP'"«.^"^^''-. the axis of which ro^y : "r ThTSdriLlT"""" °''"P'"' '^ *^^ M°y'^ '-J^- -d I antir in« ^ ^^ formation occupies the axial portion of the Stp'to^'fcSTnlil '"' ^Z ai^Haceous^uartzites t «.lour o^ ^iTSSrS I r r '" *^?'"^- '^'^^ weathering ur oi these rocks is a dark rusty brown, which is the most iHi 118 valuable field characteristir in its determination. On the east side of the lake, in the vicinity of Moyie, the rocks strike east ; west with a dip of 30 degrees to the north and are close to axis of the anticline, while in proceeding eastward u^ the towards the Society Girl the formation gradually changes strikes to a northwest-southeast strike with a dip of 25 degi to the northeast, as would be expected in going from the i of the anticline to its eastern limb. On the hill to the wes the lake, where the Aurora and Guindon group of claims arc cated, the strike is northeast-southwest with a dip of 20 degi to the northwest. The axial portion of the anticline is occuj by the Creston argillaceous quartzites, purer quartzites, dolomites which are well exposed on each side of the U( Moyie lake. t 'V Fissure System. All the ore deposits in the Moyie area are connected with main parallel fissures striking a little north of west and dip[ on an average 70 C f the anticline composed of the Aldridge formation. Tl two fissures occur on both the east and west &ide of the 1 and it is probable that they occur in the rock formation ur the lake (Figure 6). The walls bounding the fissures si very little evidence of relative displacement, the greatest mc ment observed being 18 inches; however, in such a homogene series of quartzites the detection of such a movement might impossible. St. Eugene Mine. Location. The St. Eugene mine (Plate XX) is owned by the C solidated Mining and Smelting Company of Canada, and property consists of 1,050 acres situated on the east side Moyie lake near Moyie, B.C. :i!l:: i the eastern rike east and close to the ui. the hill changes its 25 degrees om the axis the west of laims are io- if 20 degrees ! is occupied irtzites, and f the Upper ted with two and dipping OSS the axis lion. These of the lake lation under ssures show atest move- omogeneous nt might be \ le le ir le It It ie o « h »> a e e d e a L y the Con- da, and the east side of Aurora or lak^ Cambrian 'Bedrock S' Eugene Figure 6. Cross-section along the vein of St. Eu(eiie, CamI [ene, Cambrian, and Aurora mining daima. val sidi wet axil to\i stri to of 1 the cati tol by doi< Mo f ' ■■*'' ■' ^ '^M Ni^ mai on of two and the ver met seri imp 1 '. I solii pro| Mo 119 History. Father Coccola, Roman Catholic priest at the St. Eugene Mission, by showing the Kootenay Indians specimens of the different ores of the valuable metals, impressed upon their primitive minds, the importance of discovering deposits of these minerals. Peter, one of the Kootenay Indians now resident at the Mission, on a hunting trip around the Moyie lakes, brought back a specimen of dean galena ore from the hill on the east side of Lower Moyie lake. James Cronin, a mining engineer, while on his way to Fort Steele, visited the St. Eugene Mission, and was told the story of the discovery of rich silver-lead ore. In company with Father Coccola and the Indian, he journeyed to Moyie and lo- cated the Peter and the St. Eugene claims in 1893. On the advent of the Canadian Pacific railway, John Finch of Spokane, Washington, purchased the holdings of the Father for $12,000 and this money was used in building the beautiful church now to be seen at the St. Eugene mission. The development of the St. Eugene mine now progressed rapidly under the management of Mr. Cronin. Later, the Moyie and the Lake Shore group of claims, which lie between the St. Eugene and Moyie lake, were purchased and the St. Eugene Consolidated Mining Company formed. In 1905, the properties of this company were taken over by the Con- solidated Mining and Smelting Company. The total amount of development work under ground to September 30, 1913. is 19-79 miles. Production. From July 1, 1912, to September 30, 1913, the St. Eugene produced 1,826 tons of ore containing 46,082 ounces of silver and 16,098,885 pounds of lead with a total value of $98,623. The total production of the St. Eugene mine since its discovery to September 30, 1913, has been 1,017,106 tons of ore containing 5,365,232 ounces of silver and 229,305,721 pounds of lead, havmg a given value of $10,626,608. ^ m ' M 120 Methods of Mining. In the ground above the level of Moyie lake, the veins are mined by a series of adits driven along the main veins. The ore from the higher levels is transported by an aerial tramway to the ore bins. Below the level of the lake a 3-compartment shaft has been sunk to a depth of 800 feet. Fissure System. The deposit of the St. Eugene mine occurs on a zone of fissuring which has a general east and west strike. In this zone two fissures are the most important, both of which strike east and west with an aver:^ dip of 70 decrees to the south. On the 1000-foot level, which is 1,000 feet above the level of Moyie lake, these two fissures are 600 feet apart and converge down- wards and to the west. Joining these two main fissures is an important system of connecting fissure at various distances apart, which usually meet the main fissure at a small angle (Figure 7). At the junction or close to it, occurred most of the important ore-bodies. Very little displacement was noted along the veins as a whole. Character of Ore-bodies. The ore-bodies (Figure 8) are replacement deposits in the heavy bedded purer quartzites and are restricted to the fractured area between the two main fissures. Where the fissures cross the more argillaceous quartzites, the veins are narrow and usually filled with quartz containing small quantities of sulphides. The ore consists mainly of coarse-grained galena with subordinate amounts of zinc-blende, pyrite, pyrrhotite, magne- tite, and a little chalcopyrite. It is also reported by the officials of the mine, that the sulphides — pyrite, pyrrhotite, md zinc- blende — were slightly more abundant near the periphery of the ore-bodies and that the zinc-blende showed no increase with depth. The gangue, which is small in amount, consists of pink garnet, actinolite, quartz, and some caldte. The garnet, actino- J b) I 122 1 \ -v^U Ni' i»;i-! 1 1! 3 Id 123 lite, and quartz are more abundant in the transition zone of the ore and country rock and at times the fissured quartzii-. near the vein are heavily charged with these minerals. In some cases the quartzites show evidence of silicification, although no true chert, as found in the Sullivan deposit, was identified in the St. Eugene. A study of the paragenesis of the ores of the St. Eugene shows that magnetite was the first mineral deposited and was followed by the gangue minerals. The garnet approximating idiomor- phic outlines, is penetrated by numerous needles of actinolite. The sulphides were deposited last and fill the cracks and inter- stices of the other minerals. The above relations are shown in Plate XIXB. Aurora Group of Claims. The Aurora group operated by the Aurora Mining and Milling Company of Moyie, B.C., consists of five crown-granted claims, the Aurora, Horse Shoe, Durang, Etna, and Portland, situated on the west side of Lower Moyie lake opposite Moyie, B.C. (Plate XXI). The vein occurs on the east and west system of fissuring described in the general -' -^ription of the district, and possibly on the southern of t.. main fissures which here has a general strike east and west, varies as much as IS degrees from this direction. The dip oi cue vein is 60 degrees to the south (Figure 9). The vein cuts across the Aldridge for- mation, the oldest subdivision of the Purcell series, which here strikes northeast with a dip of 50 degrees to the northwest. The formation is made up of thin-bedded argillaceous quartz- ites (locally called slates) and massive purer quartzites which here form the western limb of the northeriy plunging anricline described above. The vein has a maximum observed width of 6 feet and consists of zinc-blende and galena with very little gangue. Occasionally fragments of the wall rocks are enclosed by the ore. In the report on the Zinc Resources of British Columbia, the following assay of the ore is quoted: gold 0-02 ounces, silver 7-3 ounces, lead 31-5 per cent, zinc 33 per cent. The ore represented in the Aurora is also considered by the same . )■ M' m 8 i e I 125 commission to be the simplest to treat of any of the ores examined in their series of experiments. Development on the property consists of about 1,500 feet of workings, mostly in the form of tunnels (Figure 10). Operations on this property are suspended, for at present there is no demand for zinc ore in British Columbia. GuiNooN Group of Claims. This group, consisting of the Guindon, Fereole, the Alice and the St. Joseph fractions, is located in the territory adjoining the Aurora group to the north. The vein on which these claims are located is about 700 feet north of the Aurora vein and has an east and west strike with a dip of 60 degrees to the south. The formation which the vein traverses is the Aldridge formation, which here strikes northeast and dips 20 degrees to the northwest. The vein is from 4 to 5 feet wide and in one tunnel the ore was 18 inches in width. It consisted of galena, zinc-blende and some pyrite. Development work consisted of a few short tunnels. Cambrian and Mabelle Claims. The Cambrian and Mabelle crown-granted claims operated by the Cambrian Mining Company, Limited, of Moyie, B.C., embraces the territory between the St. Eugene Consolidated and the Aurora and thus lies for the most part under the waters of Lower Moyie lake. The extensive zone of Assuring, described in the general statement and which occurs on both sides of the lake, is to be expected to occur in the intervening territory. As the veins are mineralized in the St. Eugene Consolidated and in the Aurora it is logical to expect that the Cambrian and Mabelle claims will also be productive. The sounding of the lake on the Cambrian and Mabelle claims revealed thf maximum depth of water to be 140 feet and in addition 90 fet. of blue clay and hard pan cover the bottom of the lake (Figure 11). This last information was supplied by Chas. A. MacKay of Moyie, B.C., one of the directors of the company. 126 lit I -a e o ml JL 127 Society Girl. This group co.iiprises seven crown-granted claims operated by the Society Girl Mining Company, Limited. They are situated about 2 miles east of Moyie at an elevation of about 5,000 feet and adjoin the eastern boundary of the St. Eugene Consolidated. The formation in which the deposits occur, is the oldest subdivi- sion of the Purcell series called the Aldridge formation, which here strikes north and south with a dip of 25 degrees to the east and forms the eastern limb of the anticline described above. The vein, where examined, strikes N.eO" W. with a dip of 60 d^rees to the south and appears to be in the great zone of fis- suring which traverses the Moyie area. The vein is narrow where it traverses the thin-bedded argillaceous quartzites and widens out in the heavier-bedded quartzites. The upper workii^ expose an oxidized ore-body consisting of cerussite and pyromorphite, both massive, and in beauriful crystals. The cerussite is white to colourless and occurs in tabular orthorhombic crystals either singly or as penetration twins. Masmve cerussite is also present. The cerusute is often embed- ded in dense masses of limonite. The oxidized ore zone is a rare occurrence in East Kootenay. The unoxidized or primary ore, consisting of galena and zinc-blende with little or no gangue, is exposed in the lower tunnel which penetrates the ore -body 250 feet below the surface. At present the ore is hand-sorted and then sent to the smelter at Trail for treatment. For the year 1911 up to the end of September, the total output of the mine amounted to about 400 tons. The galena carries 1 ounce of silver to 4 per cent of lead while the oxidized ores carry 1 ounce of silver to 5} per cent of lead. THE KIMBERLEY AREA. Location. This area is situated near Kimberley, the terminus of the Canadian Pacific branch line from Cranbrook to Kimberley, and includes the Sullivan, Stemwinder, North Star, and several minor properties. ?l ' u$ 128 Geology. The Kimberleyarea is underlain by the argillaceous quartz- ites and argillites of the Aldridge formation. These rocks are intruded by several Purcell sills composed of gabbro, which are well exposed on Mark creek above Kimberley. The Aldridge quartzites of the Kimberley area form the eastern limb of the large anticline the axis of which is located in the vicinity of Matthew creek. It has been described in detail in the char ter on "Structural Geology." In general, the strike of the rocks near Kimberley is nearly north and south, with the most prevalent dip to the east ; but minor folds modify this simple structure, as can be well seen in the vicinity of the North Star mine, where a number of anti- clines and synclines are impressed on the eastern Mmb of the main anticline mentioned above. Character of rHE Deposits. In contrast to the deposits of the Moyie area, which are true fissure veins, the deposits of the Kimberley area are replacement deposits in argillaceous quartzites. The ore-bodies in general conform to the dip and strike of the quartzites. This relation- ship is not proved in the case of the Stemwinder. The hanging- walls and foot-walls are not usually well defined; but the ore grad- ually passes into the normal country rocks so that the distinction between rocks and ore is commercial rather than structural. Exceptions to this occur where the walls consist of the thin-bed- ded slaty quartzites which are evidently difficult to replace. The deposits are arranged in distinct zones. The centre of each body is occupied by a fine-grained mixture of galena and zinc-blende in which masses of purer galena occur as lenses. This inner por- tion gradually passes exteriorly into a fine-grained intimate mix- ture of pyrite, pyrrhotite, and zinc-blende. The sulphides grad- ually diminish in amount and finally give way to a fine-grained chert which is present where the country rock is a heavy-bedded, purer quartzite, and especially on the foot-wall of the ore-bodies. The chert passes exteriorly into the normal argillaceous quartzites. Jlj. 129 I iS .1 ?' 'l i r Mil'' .» i( 1896 and probably consi ' Company of Spokane. In building of the Marysville junction of the St. Mary rivr . SuLUVAN Mine. LMotion. — The Sullivan .ur.t! is located on the southern slope of the Sullivan hill aboi ' 2) n.ile^ by road north of Kim- berley, at an elevation of 4,6U0 ftet above sea-level. History.— The Sullivan, '''•« v d in 1895 by Pat Sullivan, Jno. Cleaver, E. C. Smi^^h, { 1 1 V^. r Burthett, was bonded to Col. Redpath and Judg> '^■..nt ot Spokane, Washington, in I' *a ^n( Sullivan Group Mining '*) . , thit company conunenced the .Tiei.tr \t MaiysviUe, B.C., at the rul'1>'' :7eek. It waa completed in 1903, but remodelled in <.9( l an. ■ ..; "r-li, ,.); xi down for good in 1908. In 1910. th - .'< a3r)Ud.'>iCA' : " .tig and Smelting Company acquired the cU^i r. ut th. Si i/an Group Mining Company, as well as many u.' he su. j '. 'lag claims. The ore is being shipped to the compati '■ sm • . Trail. The smelter at Marysville is now dismanued aud a thing of the past. Production. — ^The production of the Sullivan from 1894 to September 30, 1913, was 188.648 tonsof ore containing 1,694,402 ounces of silver, and 86,821,629 pounds of lead with a gross value of $4,364,805. The production from July 1, 1912, to September 30, 1913, was 41,284 tons of ore containing 448,379 ounces of silver and 23,411,667 pounds of lead having a gross value of $1,281,150. Equipment. — ^The mine was originally opened by a vertical shaft with levels at various intervals of 5 or 10 feet along the strike of the ore-body. On acquisition by the Consolidated Mining and Smelting Company, the 100-foot level was continued to the surface and this tunnel is now the portal to the mine. At the mouth of this tunnel, a large ore-sorting house is located. An a&ial tram from the ore-sorting house connects the mine with the Canadian Pacific railway which carries the ore to the smelter at Trail. There is a hydro-electric power plant, deriving its power from the falls on Mark creek by means of three 6-foot Pelton wheels — two connected to a 40-driIl compressor and one to a 120 kw. generator. Compressed air is conveyed to the mine through an 8-inch pipe 5,100 feet long. 131 CharaeUr ^ the Ort-BodUs. The deposit occura in the Aldridge formation which Here strikes about north and »outh with a dip of 10 degrees to 60 degrees to the east. This formation consists of thin- bedded argillaceous quartzites and heavy-bedded, purer quartzites. The ore-body conforms in dip and strike with the quartzites and cannot be called a true fissure vein, but a replace- ment deposit in which the sulphides replaced the fine-grained quartzites (Figure 12). The hanging-wall and foot-wall are not well defined and the ore grades gradually into the country rock, i0 ntt /t^w U^tkrtl \antcm fell Figure 12. IXagrammatic crow-aection of Sul! van mine. except when the country rock consists of thin-bedded slaty quartzites which are evidently difiicult to replace. In the upper workings close fdding later than the ore deposition increases the real width of the ore. This was well shown in the glory hole at the time of the writer's visit. On the 60-foot level the dip of the ore-body in places approximates 25 degrees and on the 100- foot level the dip increases to 70 degrees, which is also the dip of the surrounding quartzites. As far as exploited, the maximum stope width is 120 feet and the maximum stope length, 325 feet 132 There are 10 levels, the north level being 100 feet below the sur- face and forming the entrance to the mine. The ore-body is arranged in distinct zones which grade imper- ceptibly into eadi other (Figure 13). The centre of the lode is occupied by a fine-grained mixture of galena and zinc-blende in which masses of purer galena occur as large lenses. It is these lenses that constitute the valuable ore shoots in the mine. They occur either singly or as two parallel shoots separated by one of poorer grade. The gangue in this inner zone is absent except l-^§ IE3 normal aldrK^ ^uarttitts pyrrhotJte.pyritt, garnet, diqps/de tone (bancftdj ZOfmtt pyrite, zjncblende, Alona,tam9t tone (bSmM) >— chmrt ^ena with som* zincblonde ond garnet Figure 13. Diagrammatic longitudinal section of Sullivan ore-body. for a few idiomorphic crystals of a pink manganese-bearing garnet (Plate XI3CA). This inner zone gradually passes ex- teriorly into a fine-grained mixture of pyrite, pyrrhotite, and zinc- blende, which contains as a gangue numerous crystals of an almost colourless garnet with some grains of actinolite or possibly diopside (Plate XXIIB). The sulphidr^ gradually diminish in amount and finally give way especially on the foot- wall to a fine-grained chert which is present when the country rock is a heavy-bedded purer quartzite, and is absent when a more argillaceous slaty member constitutes the walirock. No gar- ^JL Mk 133 nets or other gangue minerals were noted in this chcrty zone. The chert gradually passes into the normal quartzite in which, with one exception, all contact minerals such as garnet, diopside, and actinolite, are absent. As mentioned, the ore deposit as a whole is a conformable replacement of fine-grained argillaceous quartzitcs by fine- grained galena, zinc-blende, and iron sulphides. Replacement is very well shown in most parts of the deposit since alternate banding of ore and quartzite is seen near the periphery of the ore masses where the relative susceptibility to replacement of the laminae of the quartzite is different. Joining these favourable bands are numerous interlacing veinlets of sulphides which, as shown in Plate XXIIIA represent an intermediate stage in the complete replacement of the quartzite. Examined microscopi- cally, the sulphides appear to have entered bttween the quartz grains of the quartzite and then to have attacked the quartz it- self. The sulphides, entering along the favourable lamime, replace the muscovite also, as shown in Plate XXI 1 1 B. Evidently muscovite has been formed previous to the introduction of the sulphides. North Star Mink. Location. — The North Star mine is located on th» cast slope of the North Star hill at an elevation of 5,260 feet above sea-level or about 1 ,500 feet above Kimberley, which lies at the foot of the North Star hill on Mark creek. History. — The North Star was discovered in September, 1912, by Bourgeois and Langill who bonded the claims to Woods Bros, of Quebec; the latter transferred four-fifths of their interest to D. P. Mann of Montreal in 1893. Subsequently, a company under the name of the North Star Mining Company was organized. In 1895, 62 tons of ore, valued at $68.70 a ton, were shipped to the United States. In 1900, the railway from Cranbrook to Kim- berley was completed and the mine was joined with the railway by an atrial tramway. During the year, 16,000 tons, averaging SO to 55 per cent lead and 20 to 25 ounces of silver, were shipped. In 1904, the mine was reported to be worked out; but the cleaning 10 f s4 I 14: 134 up of the deposit lasted until 1908, in which year 3,000 tons were shipped. The property is now closed down. Geology.— At the time of the writer's visit, the mine was abandoned and all the ore removed, so the following description is based mainly on the reports of the British Columbia Bureau of Mines, and a paper written by Mr. Corless' with additional notes on the structure by the writer. The country rocks are argillaceous quartzites of the Aldridge formation forming part of the eastern limb of the anticline described in the general descrip- tion of the Kimberley area. In the vidnity of the mine, small anticlines and synclines modify this general structure. On the whole the quartzites strike north and south and dip at various aisles to the east. In the immediate contact with the ore-bodies, the quartzites are bleached to a greyirfi white colour and were known locally as "porphyry." Oft,— (a.) The ore was primarily a very clean solid argenti- ferous galena rather fine grained with only a small amount of zinc-blende. The assay value from smelter return was, silver 23-50 to 45-3 ounces per ton, lead 53 to 68 per cent. (b) The upper part of the ore shoot was composed of a red- dish brown, black and yellow mixture of oxides and carbonates of iron and lead, with beautiful specimens of wire silver, crystals of cerussite formed by the oxidation of galena, and sulphides of iron. There was a large amount of this ore which carried a higher silver value than the crude galena. The values from smelter returns of this "carbonate" ore are as follows: silver 52 to 60 ounces per ton, lead 49 to 57 per cent. Ore-Bodies.— The main ore-bodies are the west and the east ore-bodies, 400 feet long, 70 feet wide, and 50 feet deep, and 180 feet long by 40 feet deep respectively. The longer axes of these are parallel, both striking a little east of north. These bodies apparentiy occur in synclinal basins formed of argillaceous quartz- ites. These two basins are separated by an anticline. The ore-bodies probably represent remnants of a once continuous ore-body, the larger part of which has been removed by erosion (Figure 14). iCorlcM. F.V., BuM. Cwi. Min. iMt., Vol. 5, 1902, p. 512. I ' tMmdi 135 Stemwinder. The Stemwinder is situated about one mile northwest of Kimberley on Mark creek and hence between the Sullivan group on the east and the North Star on the west. The country rock consists of argillaceous quartzites of the Aldridge formation intruded by several sills of hornblende gabbro. The ore-body is entirely enclosed by the quartzites and closely resembles the Sullivan in its occurrence and mineral- ogy. The interior of the ore-body consists of a fine-grained jS" portion of erodedore zone smf assoctated formations Figure 14. Diagrammatic c r o w e c tion of North Star ore-bodte*. mixture of galena and zinc-blende passing exteriorly into a fine- grained mixtiuv of pyrrhotito, pyrite, and zinc-blende. This is succeeded by a cherty layer which in turn passes into the normal quartzite. The amount of development consisting of a few short tunnels was not sufficient to expose the relations of the ore -body, but it is evidently of large nze. Mascot and Ecupse. These claims are situated on the east branch of Hells Roaring creek, at an elevation of 5,800 feet. The vein occurs in the argillaceous quartzites of the Creston formation; it is well defined and conforms in dip and strike with the sediments, which near \\ :&! .'I * 136 the vein strike almost east and west with a dip of 69 degrees to the north. The ore, consisting of galena, with a small amount of chalcop>rite in a quartz gangue, favours the hanging-wall, and is associated with a band of gouge about 1 foot wide. At the bottom of a shaft 56 feet deep, which opens up the deposit, the vein is s.;mewhat broken, but is still in evidence. About 200 feet down the hill from the outcrop of the vein, the sediments are intruded by a granite porphyry which contains large id.o- morphic crystals of orthoclase in an isometric groundmass of plagioclase, quartz, and hornblende. The following assays were supplied by the owners, Messrs. Tarrant and Angus:— Sample Gold saver Lead Copper Ozs. 004 016 010 0-24 01! 200 4-80 2-20 Ozs. 2-2 0-6 61 3-4 6-8 417 2-34 469 % lO'* 57-8 ■ 49-4' ■ 39 SO 32-ii' % "i-2 '4-i2' (Dump) J GOLD QUARTZ VEINS. |4t: Distribution. The gold quartz veins occur for the most part on Perry creek. A great many claims were located on these deposits on the north side of Perry creek in 1896 by prospectors in search of the source of the placer gold which had been worked with much success on the same creek. Geology. The deposits occur in the argillaceous quartzites of the Creston formation, which is well exposed on Perry creek. The quartzites are well-bedded in beds 2 inches to 2 feet in thickness, the latter separated by thin beds of meUrgillites averaging one J. 137 inch in thickness. The massive quartzites weather a light grey while the metargillites weather dark grey or rusty brown. The strata of this formation are so well cemented together that they appear massive and form steep cliffs. Character of Deposits. The deposits occur as true fissure veins. Their width aver- ages about 8 feet, but some are as wide as 20 feet. They can be traced for long distances along the strike. Mineralogy. The mineralogy of the gold quartz veins is very ample and conasts of free gold, pyrite, and quartz. Native Elements. Gold, Au. — Gold is reported as occurring native in the out- crops of the veins, but in depth is evidently associated with the pyrite. Sulphides. Pyrite, FeSt. — ^Sulphide of iron occurs sparingly throughout the quartz gangue. Oxides. Quartz, "iO|.— Quartz is the only gangue mineral noted in the deposits. Persistency. From the width of the veins and their great extension along the strike, it is almost certain that they persist in depth, cd though no workings have as yet proved this point. Values. The values in these deposits are reported to be unequally distributed. A report of a mill test on these ores given by the Provincial Mineralogist of British Columbia in the report of 1898, p. 1016, is as follows:— I4t 138 "Recognizing the futility of trusting to small samples, and that a satisfactory test of the various properties could only be determined by a practical test, Mr. J. E. Hardman. mming engineer, of Montreal, had a small stamp mill erected dunng 1897, at the mouth of Saw Mill Creek, for the purpose of making mill tests of the ore from the various properties he had under bond. The mill is a small 5-stamp battery, so constructed as to be easily porteble, manufactured in Nova Scotia, and is dnven by a small upright ei^ine supplied with steam from a vertical water-tube boiler. It is provided with the usual amalgamating plates, etc., for the coUection of any "free gold." and is, as a whole, a very complete and well-constructed little plant. This mill was set up under the roof of the old saw-mill. "Test runs were made on ore from several of the cl^ms on the creek, in lots of 5 to 10 tons each. The results obtained were not commercially satisfactory, for. notwithstanding the fact that some gold was saved, in no instance were the values obtained sufficiently high to warrant serious work on the claims. The tests, however, do not seem to have satisfied the claim owners, as the results obtained did not tally with their private assay's. I heard several complaints about the matter, regret being ex- pressed that the running of the mill had been left to inexpoi- enced men, and the values allowed to escape in the tailings. Of this I know nothing further than was told me by men who might be couMdered 'interested parties.' "It was, of course, impossible for me to form any opinion as to how the mill had been run, except by testing the tailings, which I did in the presence of a well-known engineer and mill man, Mr. Farrell, of San Francisco, who likewise made several independent tests for his own information. The tailings from the mill had run down to the creek bottom, some 100 feet, over gravel, and had been subjected to a winter's snow and rain. I panned the mixed gravel and tailings over all of this distance, and in each pan I found I could save, besides the iron sulphides to be ex- pected, a globule of mercury as large as the head of a match, and a string of amalgam in the bottom of the pan from a quarter to half an inch long. On driving off the mercury on a hot iron I found I left a very fair sized particle of gold. I collected some A 139 of the mercury and amalgam, which I turned over to the Pro- vincial Aasayer, who reports to me that the mercury carries over 2% of gold, while the 'black sand' contains $20.00 in gold and a trace of silver. Samples which I took of the tailings gave me on assay as high as $4.00 in gold. "^ the result of my investigation, I am satisfied that the mill did not save such free gold as may have been in the ores, and that the tests made were not conclusive as to the values t. ^'^H m j - X i c--\ ^ ^<.^^'^ "^^ r ^ W .w 1 ^1 Figure 15. Plan cf Running Wolf mine. Perry creek, Kootenay, B.C. : . II of these properties. I am further satisfied that only a portion of the gold is 'free,' and that some method of concentration would have to be adopted to save the gold occurring in the iron sulphides." m Detailed Description of Properties. The Running Wolf. The only property in operation at the time of the writer's visit was the Running Wolf on which considerable work had been I 140 done. It is located on French creek, a southern tributary o{ Perry creek, at an elevation of 5,000 feet above sea-level. The claim owned by the Perry Creek Mining Company contains two parallel veins, 100 feet apart, and each 20 feet wide, vertical and striking S. SO'W.; and a single vein about 30 feet wide vertical and striking S. SO" E. (Figure IS). 1., COPPER-GOLD DEPOSITS. Introduction. The copper-gdd deposits of the Cranbrook area are wide- spread and at present somewhat neglected, since they are over* ^adowed so greatly in importance by the deposits of silver-lead. Nevertheless, from their extent and character, a moderate amount of success is possible in these deposits if carefully worked. Mi Distribution. Since the copper-gold deposits are always associated with the Purcell sills, the distribution of these deposits is governed by the distribution of the Purcell sills, which occur almost ex- clusively in the Aldridge formation; the sills in the younger formations are thin and unimportant. The copper deposits which have received most attention, occur on the several branches of the St. Mary river, where ,ufficient work has been done to expose their geological relationships. Geology. The Purcell sills, with which these deposits are associated, have been described at some length in a previous chapter and only a short description here is necessary. These tabular intrusive bodies are injected along the bedding planes of the quartzitc3 and vary in thickness from 2 to 2,000 f^et. They consist mainly of hornblende gabbro with large irregular masses or differentiates of a peculiar hornblende granite. It is with 141 these irregular maaaes that some of the copper deposits are associated. Chasacter of the Deposits. The deposits are of two varieties. (1.) Large irregular masses or differentiates. (2.) Veins. The differentiates occur usually in the interior of the sills and are of varied shape and size. No single body has as yet been outlined, but they are believed to be at least 200 to 300 feet in diameter. The boundaries of these bodies with the surround- ing rocks are always gradational. The differentiates consist generally of a peculiar hornblende granite containing as a prom- inent feature, opalescent quartz. The hornblende is usually fibrous and in some cases makes up 75 per cent of the rock. The other constituent of the rock is an intergrowth of quartz and orthoclase. Tlie ore minerals chalcopyrite, pyrite, and pyr- rhotite occur sporadically throu!j:Lout the differentiates. The true veins, 2 to 4 feet wide, occur on shear zones in the sills. The hornblende gabbro, which forms the wallrock, shows the effect of shearing at the time of the formation of the shear zone by the occurrence of an alignment of the feldspar constituents of the gabbro parallel to the vein. The filling of the shear zone consists most frequently of quartz impregnated with chalcopyrite, pyrite. and pyrrhotite. The presence of a sul- phide of cobalt is indicated by the occurrence on the weathered outcrop of the vein, of erythrite, a hydrated arsenate of cobalt. Native copper sometimes occurs in the quartz. In several cases coarsely crystalline caldte formed part of the veins and from its relationships to the other constituents, was the latest filling. MlNEKALOGY. Native Elements. Copper Cu. — Native copper was noted in a vein on the Evans property on Whitefish creek. It occurred as small plates in 1 f 142 quartz. Native copper is also reported from the difierentiated ore-body on Alki creek. Sulphides. Galena, Pbs., Sulphide of Lead.— Galena occurs sparingly in the copper deposits and was found only in the Howe's claim on the south side of St. Mary lake in a vein on the contact of a gabbro sill with the underlying quartzites. Pyrrhotite, FeuSit. — Magnetic pyrites is the most abundant sulphide in the copper deposits. It occurs as small masses of irregular outline associated with pyrite and copper-bearing pyrite in both the differentiates and the true vein. Chalcopyrite, CuFeSt, Copper Pyrites.— Chalcopyrite occurs in the copper deposits as small irregular masses associated with pyrite and pyrrhotite. Pyrite, FeSt, Iron Pyrites. — Pyrite occurs abundantly in both the differentiates and in the true veins. In most cases, it apparently approaches chalcopyrite in appearance. Oxides. Quartz, SiOt, Oxide of Silicon. — Quartz is the most abundant gangue mineral in the copper-bearing veins. It occurs massive and contains the sulphide as impregnations. The quartz carrying the sulphides of iron and copper, is evidently the first vein filling. Later, a reopening of the vein occurred, as is well shown in the vein on the Evans group, allowing a later deposition of coarsely crystallized calcite, which as far as known, does not carry any sulphides. In the differentiates, quartz occurs as an opalescent variety and as an intergrowth with orthoclase in the micropegmatite. Carbonates. Calcite, CaCOt. — Carbonate of calcium is a prominent gangue mineral of the copper deposits of the vein type. In the vein on the Park claim on the St. Mary prairie, it forms 143 almost the entire gangue. It is generally white and coanely cryitallized. MahckiU, CuCO, Cu{OH)t, Basic Copper CarbonaU.— Malachite occurs as green incrustations on the outcrop of the copper-bearing veins as a result of the decomposition of chalcopy- rite and cupriferous pyritt Aturite, ZCuCOt, C«(0/f)i— Axurite occurs as a blue incrustation on the weathered outcrops of the copper-bearing depouts. SilicaUs. Pyroxene. — Pyroxene was found only in a vein on Pollens group of claims on Whitefish creek. It occurred as short pris- matic crystals of green colour. Hornblende. — Hornblende is the most common mineral in the differentiates, occurring as black lustrous crystals associ- ated with micropegmatite and the sulphides of copper and iron. Ar senates. ErythriU, CoiAst Ch SHtO, Hydrated ArsenaU of Cobalt, com- monly known as Cobalt Bloom. — Erythrite occurs as a crimson red incrustation on the oxidized outcrop of the copper-bearing veins. Although no cobalt sulphides were identified in the cop- per deposits it is very probable that they exist in small quantities associated with the other sulphides. Persistency. From the very nature of the differentiates, they cannot extend beyond the limits of the sills. In the case of the veins, the following facts tend to show that they also are either restricted to the sills or to the quartzites in the immediate neighbourhood of the sills. 1. With very few exceptions, the veins occur within the sills themselves. 2. All gradations exist between the differentiates and the true veins showing that the deposits originated from the sills. 144 3. In one case, on Mackay'n claims, the vein which was 8 feet wide in the sill pinched out in the quartzites within a few feet of the lower contact. 4. No veins have been located in the quartzites. OUGIN. The origin of the copper deposits nuiy be safely associated with the cooling stages of the Purcell sills, since all gradations exist from the normal gabbro through the differentiates to the true veins and all gradations carry sulphides of copper and iron. Also, the occurrence of the copper deposits always in association with the sills and the fact that the veins pinch out when passing from the sills to the quartzite support this idea. Age. The Purcell sills represent the intrusive phase of the Purcell lava, which was poured out at the close of the Siyeh times. Aliments have been advanced in a previous chapter, for a Pre-Cambrian ^e of the Siyeh formation; hence the Purcell lava and Purcell sills are Pre-Cambrian in age. From this, the conclusion is justified that the copper deposits are Pre- Cambrian in age. DETAILED DESCRIPTION OF COPPER PROPERTIES. Evans Geoup of Claims. The Evans group of claims, owned by C. and W. Evans, of Marysville, is situated on the western dope of Evans mountain, at an elevation of about 6,000 feet. The mountain is composed of easterly dipping Aldridge quartzites intruded by three diorite sills, the upper one forming the summit of Evans mountain. The lower claims contain a tunnel 200 feet long driven into a low grade ore-body of the differentiate type contained in a gabbro sill about 400 feet thick and forming the lowest of the three sills. The ore consists of pyrrhotite and cupriferous JU 145 pyrite impregnating a coarse-grained hornblende granite. The upper claim contains a Assure vein about 4 feet wide, striking (4. 45" E. in a sill of normal hornblende gabbro, which forms the middle of the three sills. The ore consists of chal- copyrite, pyrite, and aome pyrrhotite and native copper in a quartz calcite gangue. Work is being pursued on both grtnips of claims with a view to determine the size and relation of the two types of deposits. McKay Claims. The McKay claims are situat< d on the northern slope of Whitefish creek and about 7 miles from where it joins the St. Mary river. The country rocks consist of Aldridge quartzites intruded by hornblende gabbro sills, all dipping at an angle of 65 degrees to the northeast. The vein, 8 feet wide, which occupies a shear zone in tlic hornblende gabbro, strikes S. 85° W. and dips 79 dcgn-es to the south. That the fissure is a shear zone is supported by the alignment of the feldspars in the hornblende gabbro parallel to and in close proximity to the surface of the fissure. In tracing the continuation of the vein into the underlying quarU- ites, it was seen to pinch out within 8 feet. Sylvia Claim. The Sylvia claim is situated 2 miles east of Marysville. The country rock consists of a hornblende gabbro whose form and relationships are concealed by a covering of superficial deposits, but from a study of the surrounding district the horn- blende gabbro is believed to be in the form of a sill intruded into the Aldridge formation. The vein, 7 feet wide, strikes N. 63" E. and dips 85 degrees to the southeast. The vein filling consists of pyrite in a quartz gangue. The reopening of the fissure gave opportun- ity for deposition of calcite which, occurring in two distinct zones, gives the vein a banded appearance. i I! : I t il 146 Blue Dsacx>n Claim. The Blue Dragon claim is situated 1 mile east of the Sylvia and occurs under the same geological conditions. The vein which traverses hornblende gabbro consists of a number of ver- tical shear zones containing chalcopyrite and pyrite in a quartz calcite gangue. The vein strikes N. 60° E. The workable width of the vein is 4} feet. Black Hills Claim. 11$ The Black Hills claim adjoins the Blue Dragon and contains three main veins traversing hornblende gabbro. Two inter- secting veins 6-8 feet wide, composed of quartz, containing chalcopyrite and pyrite, strike N. 20° W. and N. 30° W. respect- ively. The weathered outcrop of the vein shows azurite and malachite. The other vein strikes S. 75° W. and dips 65 degrees to the southwest. The ore consists of chalcopyrite, pyrite, and some galena in a gangue of quartz and calcite. A shaft 45 feet deep opens up the depout. Yankee Girl Claim. The Yankee Giri property contains a quartz vein 6 feet wide striking S. 65° E. and dipping 66 degrees to the southwest, traversing hornblende dicrite. The ore consists of pyrite and chalcopyrite in a gangue of quartz and calcite. Cobalt bloom occurs as one of the products of oxidation. The following assays were supplied by Messrs. Angus and Tarrant: — Sample 1 open cut 2 open cut 3 shaft.... Gold 0-80 oz. 0-44 trace Silver 1-44 0Z. 4-20 2-80 Copper 6Q0% 32-50 A shaft 25 feet deep and an open-cut expose the ore-body. 4 147 OwNBCA Claim. The Omineca claim is situated 1 mile west of Marysvilie at an elevation of 3,100 feet. The vein which is 7 to 8 feet wide, traverses hornblende gabbro and contains chalcopyrite and pyrite in a quartz caldte gangue. PLACER GOLD. Placer deponta have been an important source of gold in East Kootenay district; but during the last few years the only activity has been on Perry creek. Gold has been obtained out of several creeks, the most important being Perry creek. Palmer Bar, Moyie river, and Weaver creek. From an examination of the tables given in the introduction to the chapter on economic geology, some idea of the importance and history of the produc- tion can be determined. The gold in the placer deposits is evidently derived from the gold quartz veins which occur in the Aldridge, but more particu- larly in the Creston formation. Free gold has been found in the weathered outcrops of these veins on Perry creek, where they reach a width of 20 feet. It might be recorded that the valley walls of Perry creek, the richest placer gold creek within the Cranbrook map-area, contain the greatest number of gold quartz veins. DETAILED DESCRIPTION OF PROPERTIES. As only one property was in operation at the time of the writer's visit and very little information could be obtained at that time, the following description is quoted from the Annual Report of the Minister of Mines for British Columbia, 1903. "Perky Ckeek Hydraulic Mining Coupany." "The 'Falls' occur in a canyon which cuts through a bluff of rock, the old channel of the stream apparently having passed on one side of this, and certainly on the right bank of the creek 148 if J 'i 4 lit ' there is an cM gravel channel on which, at the level of the creek, below the Falls, a tunnel (the old Montezuma tunnel) was driven in for from 1 ,000 to 2,000 feet, with certain workings in connection therewith of which no plan is known to exist. Whatever the course of this old channel may have been, it apparently emptied into the present creek below the Falls, as the old drifting propo- sition mentioned proved, and this work also proved that there is a paystreak which, according to 'old time miners,' was not down to bed or even rimrock, as bedrock was never reached by the tunnel. >\'hile there is unquestionably gold in such old channel, the paystreak was either not sufficiently defined or not rich enough to pay as a drifting prof)osition after it reached such consider- able distance from the surface. That the gold in this old channel is not confined to bedrock, was demonstrated by the old tunnel workings in the first place, while later prospecting work has re- vealed two or three paystreaks in the overlying bank, not rich enough for drifting but sufficiently so to induce a company to attempt to hydrauhc the whole bank. This company is the Perry Creek Hydraulic Mining Co., a syndicate formed of United States capital, and of which A. S. Trow, H. A. Bright, E. G. Brayton, and D. Halliway, of Merrillan, Wis., are the largest holders. Mr. Wm. Trow is local manager or agent, and Robert Jennings, superintendent in charge of the work. The company has secured water rights on Perry creek, taking water from the stream about 4 miles above the Falls, and having under construction a wooden flume, 4 feet wide by 3 feet high built of 11-4 inch lumber. To cut this lumber the company had erected a saw-mill at Saw-mill creek, and had let a contract for 300 M. feet of logs at $4 per M. "The clearing of the surveyed flume line was well under way at the time the property was visited, as was also the flume con- «truction, with every probability cf being completed during 1903. The flume leads aiong the right or south side-hill, attain- ing a height above the creek of about 300 feet. At the lower end of the flume, a 'siphon' of rivetted iron pipe was to be constructed over a draw, narrow but having a depth of 1 75 feet. The siphon was to deliver its water to a short ditch, leadmf to a pressure box situated on the top of the hill, from which a pipe-line was to run J" 149 down the face of the bank to the mouth of the Montezuma tunnel, where it should deliver water vmder a head of about 400 feet. The stream, from the tunnel down, is confined by steep banks and has a fall of about 3 per cent; this is not enough to carry o£f hydraulic tailings and, consequently, they will have to be sluiced away in boxes for about half a mile below the Falls. This wiU necessitate the bottom of the hydraulic pit being some 50 or 60 feet above the creek at the mouth of the Montezuma tunnel. Consequently, while the upper part of the bank can be run oS by straight sluicing methods, the lower 60 feet will have to be raised by an elevator of some sort. "The bank representing the face of this old channel has been cleared of timber to its summit. This bank is about 400 feet high and is composed of fine gravel, silt and some clay, which will wash cheaply and quickly, but will have to be handled very carefully as it has a tendency to 'slide,' a thing which, if it occurs, will choke the canycm and interrupt operations for some time. Hydraulidng operations should begin in the spring of 1904 and with judicious handling the property has a good chance of be- coming a producing mine this next season. "Above the Falls the old diannel is deep and several atteaqits have been made to test and work it by means of shafts simk in the early 90's; but. while gold has been found, these operations have net been commercial succesan. In the stream bed there is a clay or 'false' bedrock, on which gokl in paying qualities has been obtained at several points." "The East Kooxi-^^ Wl/ueml Mining Compant." "The East Kootenay PlacCT Mining company, a local com- pany, in iriiidi Dr. Bonnell, W. Ross and J. McE>aan^ of Femic and others, are interested, has secured leases aboat 4^ miles above the Falb, and has eatabKshed a steam shovdl for lifting the gravel into the sluice boxes. At the point selected for operations the creek b«d has a grade of about / r/, 3 per cent, and at a depth varying from 3 to 10 feet ther*- ocans a 'fake bedrock,' consisting of a sandy day, on and above wUdi gold in conskleraUe quantities has been found. The true bedrock is 150 believed to be at a depth of approximately 50 feet lower, since at this depth it was struck in both the old Ridgeway and Baker shafts, a short distance away. From the former of these shafts drifts were made, to its is reported, down stream for 150 feet and up for 25 feet. In the shaft $90 was said to have been found, and the drifts were stated to have paid $7 per day t» the man for a time. The Baker shaft was also drifted from for some 100 feet, but was not profitable. The original intention at the installation of the plant was to work the gravel on and above the false bedrock, and of this a patch 64 yards loi^;, 8 yards wide and 2 yards deep, equal to about 1,000 cubic yards, has been taken ?nd dumped into the rough sluice-boxes. From this small patch gold amounting to $260, as reported by the management, was obtained, being equiv- alent to 26 cents per cubic yard. "The shovel is a regular railway steam shovel (built by the Vulcan Iron Works, of Toledo, Ohio), mounted on a standard gauge car running on rails; it is self-propelling and has a bucket of 1} cubic yards capacity. The motive power is supplied by steam from a vertical boiler forming a part of the equipment. The shove), which weighs about 45 tons, was brought up from the railway as it stands and under its own steam, over tht waggon road, on moveable sections of track, an exceedingly difficult undertaking considering the road travelled over. The shovel has a rigid bucket arm long enough to load railway cars from a gravel pit, a lift of say 10 to 12 feet, and at first worked very well; but as the cuts worked upstream the bedrock ran very Hat, and the height therefrom to the sluice-boxee increased, so that event- ually the dipper Jirm was found to be too short. Operations were accordingly stopped and the superintendent, Mr. Banks, was then sent East to have a longer arm prepared to enable the shovel to take a wider cut and to lift higher. "Some difficulty has also been found in disposing of the tailings, as the stream had not sufficient grade to can-y them off and it was, therefore, found to be necessary to 'stack' them, an appliance for which was also being arranged for by Mr. Banks. These additions to the plant will not be ready until the season of 1904. 151 "If the ground worked may be taken as a sample of the values to be found above the false bedrock, and there is no reason why it should not be, there is on the lease a large tonnage of material which, with the plant modified as proposed to suit the conditions, can be handled to a good profit. The plant, as it stands at present, is realised to have too small a range to be effective, and operations had been suspended until the requisite alterations were made. In the meantime the bucket arm had been unshipped and the winding engine of the shovel was em- ployed to hoist the dirt from a shaft, which was being sunk to the bedrock proper to test it at this point. It is expected that, as work proceeds upstream, true bedrock will rise nearer the surface, and that towards the upper part of the leases it may be possible to reach it from the level. "Water for sluices is taken out of the creek about half a mile above the shovel, and is brought down in a board sluice-box 32 inches wide and 15 inches deep. "These were the only two placer mining enterprises in actual operation on the creek in August last. Some little placer pros- pecting was being done with a view of locating ground suitable for shovels, dredges, or other mechanical arrangements; this work, as yet, has not been developed into mining propositions. About half a mile below the Falls, on the right bank of the stream, a partnership of the old-time piacer miners has sunk a shaft and is drifting for bedrock. This work is only carried on in the winter when water is not troublesome. The results obtained are said to be satisfactory, yielding good wsiges to those employed. "Of the mineral claims located on Perry creek there is little to be said that is new; a general description of these will be found in the report for 1898, and, with the exception of a certain amount of additional development work, nothing of importance has transpired. A large number of the claims then mentioned have been allowed to lapse, though some new ones have been located. Sherwood's claims, there noted, are still held by him in good standing, and he has done considerable development work on them, pro\ang the continuity of the ledges, with what results aa to values has not been learned. It is understood, however, that m- 152 the claims had this past summer been bonded to eastern parties, after an examination by their representative." CLAY. The following extract from a report by H. Ries* sum- marizes the information concerning the clay deposits of East Kootenay: CKANBROOK, B.C., AND VICINITY. "The calcareous silts in the valley of St. Mary river at Cran- brouk, have been referred to in last year's report, and their similarity to the silts of the Columbia valley commented on. These materials were very calcareous, cream burning, and yielded a highly porous brick. In the year 1913 another yard was established about 2 miles west of Cranbrook by Mr. Hanson. The depout worked here, lies not in the main valley but behind a ridge, and slightly above the terrace level in the valley proper. It seems to be a separate basin or small lake deposit, of very different character from the valley silts, as it is much more plastic and of better working quality. The clay is stratified, in layers one-half to 1 inch thick, separated by thin lamime of sand, and there are only a few inches of soil overlying it. A thickness of 5 feet had been exposed. Like the valley silts it is calcareous, but not enough so to make a cream-coloured product. It is sufficiently plastic to flow through a tile die. The clay (Lab. No. 1935) worked up with 20 per cent of water, and had an average air shrinks^ of 5-4 per cent, and an average tensile strength of 87 potmds per square inch. Both wet-moulded and dry-press bricklets were made with sadfactory results. The wet-moulded bricklets biwned to a pink colour at low cones and then red if well burned, but were not steel hard unless fired to cone 05, although they had a good ring even at cone 010. The burning tests of the wet-moulded bricklete are as follows: »Rie«, H., Ged. Surv., Can., Mem. 65, 1915, p. 33. Jy 153 Laboratory Sampio So. 1933. Cone Fire thrinlcafe Abeotption % % 010 26-43 OS 1-0 20-80 1 10-7 010 3 Fused It will be seen from these tests that although the day is not suf&dently calcareous to bum buff, it nevertheless shows tome of the characteristics of a calcareous clay, in its rapid shrinkage and vitrification between cone 05 and cone 1. It should be burned at cone 05 if possible. The burning tests of the dry-press bricklets were as follows: Laboratory SampU No. 1935. Cone Fire ahrinlcage % Abioiption % 010 05 1 Too loft for use 0-3 1100 31-64 0-97 The dry-press bricklets at cone OS were pink in colour fine grained, and had a good ring, but the absorption was too high. At cone 1 the shrinkage was excessive and the colour dark Iwown. If dry-press brick were made of this clay they would probably have to be burned about cone 03 for the dual purpose of getting less absorption than at cone 05 and of avoiding the high shrinkage developed when burned at cone 1. As to the uses of this clay, it could be and is manufactured into common brick. It would, I believe also, make drain tile. It lends itself to dry pressing. Lastly the smoother portions 154 • -t Hi of the deposit could, I think, be moulded into earthenware such as flower pots. Mr. Hanson showed me some interesting and very creditable pieces of rustic pottery that had been mod- elled by hand from the material in his clay pit. At the time of my visit the product consisted wholly of common brick. The plant was equipped with pug mill, rolls, and side-cut-stiff- mud machine. Drying was done on pallet racks, and burning in scove Idlns. Along the railway track at Wycliffe station 6 miles north- west of Cranbrook, diere is a strong outcrop of Pre-Cambrian metargiliite. The material is a very hard schistose rock, which in some beds contains considerably more quartz than in others. A tunnel has been driven aln^R one of the less quartzose beds, and at this point a sample for testing was taken. The material is not at all promising looking, and the only reason it was tested was because it was said to have been used for making brick, to line the smelter at Marysville, B. C. Even when finely ground, the material (Lab. No. 1941) had no plasticity so that it could not be wet-moulded. Some of it was then ground up very fine, moistened slightly with water and dry-pressed. These tests yielded the following results: Cone 010. No ring to brick, body soft, colour red, ab- sorption 12-58 per cent. Cone 05. Little ring absorption 12-28 per cent. Cone 1. Fire shrinkage 1 per cent, bricklet barely steel hard, absorption 9 per cent. The material is not recommended for brick manufacture, for it can barely be moulded even by the dry-press process, and even then has to be very finely ground. In looking for good clays in this region, Mr. S. J. Scho- field of the Geological Survey, pointed out to the writer a bed of dark grey clay located along the north bank of St. Mary river, about 4 miles above the St. Eugene mission. The bed out- crops at the base of a high bank, and has a thickness of about 5 feet. As the overburden is considerable it could not be worked as an open pit, and could only be extracted by means of drifts. Neither is there evidence of a large quantity of the material. 155 There would, however, be enough to supply a small pottery, the idea being that the material might be used for earthenware. The clay was plastic, although it contained much very fine grit, and took 29 per cent of water for mixutg. It had an average tensile strength when air dried of 57 pounds per square inch, and an air shrinkage of 4-2 per cent. It bums to a pink colour and does not become steel hard until cone 1. The fire shrinkage is not high up to cone 05, and while the absorption appears to be it is often so in common earthenware made from some clays. The clay could probably be improved by washing, so as to re- move fine grit. The following are the fire testa on the bricklets: Laboralery SampU No. 194&—Wtt-mouUtd briekUU. Cone Fire ihriokase AtMorption % % 010 2 27-60 05 S 25-00 1 11 8-80 3 ts OW Laboratory Sample No. 1946—Dry-preu bricUttt. Cone Fire shrinkage % Abtorption % Colour 010 05 1 Soft, no riiig when ttruck Fairly hard Not steel hard 26-88 16-82 pink It would hardly be worth while to attempt making any dry-press forms of the clay. Il ' *••<% . ■ ut 1S6 CKBSTON, B.C. Goat river, a tributary of Kootenay river, joins the latter near Cretton, and the Canadian Pacific railway foUowi the narrow valley of this stream from Goatfell to Creston. Along the line of the railway there are in this distance a number of clay cuu, which have given considerable trouble by sliding. The^e cuu, which are mostly of silty, laminated clay, are especially ni'meroui between Kitchener and Erickion. Some of the cuts show stony or boulder clay, and in these there may be lenses of the laminated clays. All of these laminated clays are very silty and somewhat calcareous. The deposits are not in all cases large enouuh to be worked, nor where they outcrop along the railway track, it might not in all cases be practicable to work them. TTiey represent, however, a common type of clay in this r^on, and since they are best exposed along the railway, our samples were taken horn these points. A sample (Lab. No. 1930) was taken from along the rail- way about one mile northeast of Canyon station. It is a fine- grained silty material of fair plasticity, but at the same timt exhibits the resistance to pressure, so characteristic of silty clays. It worked up with 23-8 per cent of water, had an average air dirinkage of 3- i per cent, and an average tensile strength of 25 pounds per square inch. On account of its silly character the clay did not give results when moulded dry-press, but it did lend itself to the plastic method of working, and the test bricklcts were formed in this manner. They burned to a pink colour, but did not become steel hard until cone 1, and in fact did not give a brick with real good ring unless burned to cone 05. The other details of the burning tests are as tullows: V 1S7 UUrtlory S^mfU S: 19)0. Cone File •hriakagt AbMrptiM % % 010 18«0 OS 1 16-30 1 9-4 4-76 3 9-5 4-7 7 noriy viKous It will be seen from these tests that the clay does not be- come very dense until above cone 05 and that the great de- crease in absorption at cone 1 is accompanied by a strong in- crease in shrinkage. The clay is not plastic enough to flow through a die, and the only use suggested is for making common brick by the soft- mud process. The best clay bank exposed along the railway track in the stretch mentioned is in the large cut at Goat canyon. It is a t>'pical silty clay, which bakes to a hard mass in dry weather, and runs easily in wet weather. The clay (I^b. No. 1924) is of greyish-yellow colour, somewhat calcareous, and of fair plasticity, but not enough to flow through a tile die. It re- quired 30-8 per cent of water to work the clay up to a plastic mass, which had an average air shrinkage of 4-9 per cent. The average tensile strength when air dried was 45 pounds per square inch. The clay I'ke many other silty ones swelled slightly at cone 010, and its fire shrinkage was practically zero up to cone 05- By cone 1 the shrinkage had increased to 10-3 per cent. The absorption was high in every case except cone 1, and ran as follows— cone 010, 25-80 per cent; cone 05, 24 00 per cent; cone 1, per cent. This peculiar behaviour is due in part to its silty nature, and in part to its lime carbonate contents. The clay bums pink, but is not steel hard until fired above cone 05. It is at best only a common brick clay. ♦ J »«c»ocorr msoiution tbt chait (ANSI and (SO TEST CHART No. 2) ^^ 1653 Eosi Men 51r«t ^g ("6) ♦a2-0300-Phon. ^ ^SB (716) 2M - 5889 - To, 158 Along the road from Creston to Goat canyon, and opposite the site of Lisk and Slater's old saw mill, there is a long outcrop of reddish brown clay, with very little stony material. The deposit, as nearly as could be determined without boring, is prob- ably 15 or 20 feet thick. There is room here for a brick plant, and the locality is about 1,000 feet by an air line from the rail- way. Similar clay outcrops at other points near by. This material (Lab. No. 1920) is quite different in its nature from that in the railway cuts mentioned above, being less sandy to the feel and denser, but like the others is somewhat calcareous. It took considerable water to work it up, viz., 35 per cent, but yielded a mass that was sufficiently plastic to flow through a tile die. The average air shrinkage was 7 per cent, and the average tensile strength when air-dried, 90 pounds per square inch. This was almost double that of the Goat Canyon clay. The clay burned to a red colour, and the bricklets had a good ring even at cone 010. The fire tests were as below: Laboratory Sample No. 1920. M L Cone Fire shrinkage Absorption Colour % % 010 26-40 salmon 05 1-5 23-50 1 1-7 16-87 red 3 Fused The clay could be used for common brick as it is plastic enough to work. It bums hard at a low heat, and the only objection to it is the somewhat high absorption. However, the latter is not necessarily an irdication of low durability. The clay could, moreover, be utilized in making drain tile, provided these did not have to be vitrified, but if they were burned to cone 1, the absorption would not be excessive. Even though the absorption of the brick made from this clay is somewhat high, the clay is better than several others which are used for brick in southern British Columbia. If the project of lowering 159 the level of Kootenay lake is carried out, so as to unwater the delta lands south of xZootenay Landing, the drain tile which could be mad • from this clay should prove of value for draining these reclaimed lands. Along the Erickoon road, about 2J miles from Creston, this same kind of clay again occurs, and here is not far from ti.e railway track." IS ti 160 CHAPTER VII. PHYSIOGRAPHY. 1^ I Tabular Physiographic History. The Cordillera in the vidnity of the Forty-ninth Parallel has been subdivided from east to west by Daly into the following physiographic provinces.* '* Rangts- Rocky Mountain system < Purcell Mountain system Selkirk Mountain system Columbia Mountain system. . . < Belt of Interior Plateau Okanagan range Hozomeen range < Skagit range. Vancouver range. Physiopapkic Provinces. Front Range syncline. Galton MacDonald borst. The Purcell range. The Selkirk monocline. The Rossland Phoenix volcanic cap. The Midway volcanic cap. The Anarchist old mountain plateau. The Okanagan composite batholith. The Pasayten monocline. The Hocomeen horst. The Skagit volcanic cap. The Skagit composite batholith. The Chimwack province of folded Palxozoic sediments. The Gulf of Georgia down-warp. The Vancouver complex. The Purcell Range. The Purcell range, separated from the Selkirk range on the west by the Purcell trench and from the Rocky Mountain system on the east by the Rocky Mountain trench, is composed mainly of sedimentary rocks of varving hardness. The western part of the range is mainly made up of tough argillaceous quartz- ites with intruded gabbro sills, while the eastern pait consists of younger, well-bedded siliceous and sandy argillites. On the whole, the materials are homogeneous from east to west. > Daly, R. A., Geol. Surv., Can., Memoir 38, 1913, p. 601. 161 As mentioned in a previous chapter the structure is char- acterized principally by open folding in which the rocks form broad anticlines and synclines (see chapter on "Structural Geology") broken by a few normal faults. Tabitlar Geological History. The complete physiographic history of the Purcell range, now that the materials and structure have been briefly des- cribed, can be entered upon. Since the rocks which form the range are Pre-Cambrian in age, the processes, which have pro- duced its present surface, have extended over nearly the whole geological time scale; hence a brief geological history is here tabulated in which the periods of sedimentation, mountain tuilding, and erosion, are expressed. Period. Protesses. Present Erosion, entrenching of streams, subaerial erosion. Pleistocene Erosion and deposition, glacial, interglacial, subaerial. Tertiary Erosion, entrenching of volleys in the Cretaceous peneplain, river capture, uplift, and faulting in east. Late Mesozoic (Cretaceous). Erosion, peneplanation. Early Mesozoic Mountain building, folded mountains, igneous in- trusion. Late Palaeozoic Depoaition in east, eromon in west. Mid-Palseozoic Eroebn. Early Palsezoic Plateau uplift and erosion. Beltian Deposition of Purcell f--— Relation of Drainage to Structure. In an examination of the geological and topographical map of East Kootenay, it will be noticed in the western part of the range that the drainage lines are impressed upon the land sur- face discordant with the underlying geological structures, while in the eastern part, in the vicinity of Gold creek, the two are concordant. The St. Mary river rising on the summit of the r cuts across an anticline of Aldridge quartzites before I ing the Kootenay river. A glance at the course of the i •• 8 lii: 162 Moyie river shows that in the vicinity of the Moyie lakes it occupies the axes of an anticline then swings on to the eastern limb of the same anticline until it reaches the International Boundary line, where it occupies a fault zone. In the eastern part of the range, the drainage of Gold creek is worthy of attention. Connell cr The over deepening of the main valleys causes a break in th grade of the side streams which have canyons in their low* stretches. The great volume of r.aters which occupied the va leys as the ice retreated, were overloaded with gravel, sand, an particles of rock, deposited as a great thickness of rudely stratifie gravels and sands. In the Purcell range two advances of th ice, separated by an interglacial period of milder temperatun are indicated if the age of lignite beds with the associated plan 167 remains in the gravels of the Kootenay valley are interglacial. Since the final retreat of the ice, the streams have sunk their channels into the gravels and sand, leaving protected terraces along their courses. ORIGIN OF THE TRENCHES. PURCELL "! iE^'3. The Purcell trench, a longitudinal valley, separates the Purcell range on the east from the Selkirk range on the west. On an average, the valley is 2 to 4 miles wide and is occupied in great part by Kootenay lake. The valley in the northern United States and Canada contains the north-flowing Kootenay river which empties into Kootenay lake in Canada about 15 miles north of the International Boundary line. Kootenay lake, which is 70 miles long, has an average width of 2} miles. It is 1,760 feet above sea-level and as far as known, has a maxi- mum depth of 450 feet. The mountains, which are very pre- cipitous on each side of the lake, rise abruptly to a height of 7,000 to 8,000 feet above sea-level. The tribuary streams occupy hanging valleys and enter the lake by a series of cascades and falls. At the mouths of all tributary streams occur deltas which are occupied either by townsites like Kaslo, or by fruit farms. The drain^e of Kootenay lake is effected by the Kootenay river which drains its waters westward into the Columbia river. Geological Features The Purcell trench has been eroded into a complex of ancient sedimentary rocks which have been intruded by granites of Jurassic age. The striW of the sedimentary rocks in the r°igh- bourhood of the lake little east of north, thus cutting at a small angle across t .ake whose bearing is a little west of north. Origin of the Purcell Trench. Since it has been shown that the Purcell range was b".ilt in the late Jurassic or early Cretaceous times and peneplained n -#Sli. m 168 during the Cretaceous, and since the Selkirk range in the vi( of the Purcell trench has the same history and structure, it be concluded that the Selkirk range has a hisuHy similar to of the Purcell range. The wall of the trench in the neighbourhood of the I national Boundary line is composed of the Aldridge forma the oldest known member of the Purcell series and from E correlations mentioned in this report, it caii be deduced tha western side of the trench also has patches of Aldridge formi exposed on its slopes. The valley is floored with recent . deposits, but the underiying rocks, which Daly called Kitch exposed in the cuts on the Bedlington and Nelson railway also Aldridge, hence the fault postulated by Daly on the side of the valley on stratigraphical grounds, is not preset at least there is no field evidence for it. The fault on the wes side of the valley which, according to Daly, has a throw of 3C feet, although not examined in the field, is not postulate! very firm evidence. The Kitchener rocks mapped en the v em side of the trench are really Aldridge, the oldest memb< the Purcell series, and low down in the formation, hen« the tl of the fault, if present, would certainly not be 30,000 feet. He the Purcell trench in this locality, cannot be a "graben." Daly* has put forward the idea that the Purcell trench "graben" because a block of Kitchener quartzite has been do faulted, on the east side, with the Creston formation, and the west side with the Priest River terrane of pre-Beltian ag Summary of Origin. The region now traversed by the Purcell trench was p< plained in tlie Cretaceous, uplifted in the early Tertiary and Purcell trench was eroded by one of the rejuvenated Cretace rivers during Tertiary times. No uplift is recorded in Terti or recent times. The Tertiary valley was glaciated in Pleis cene times, giving rise to the facetted spurs and hanging vail so pro minent in the architecture of the Purcell trench. « Daly, R. ._. 3,C., Memoir 38, p. 600, 1913. s h 169 Rocky Mountain Trench. The Rocky Mountain trench lies between tlie Purceli and Rocky mountains. K extends in Canada from the Inter- national Boundary in a northwesterly direction as far north as Alaska and perhap<« to the Arctic ocean. The average width of its floor is about 5 miles, but in the neighbourhood of the St. Mary river it is 16 miles wide. It is occupied in its southern part by the south-flowing Kootenay river. Geology. The eastern face of the Rocky Mountain trench, in the neigh- bourhood of Wardner, B.C., is composed of easterly dipping locks of the Galton series of Pre-Cambrian age. The range of hills on the western side of the trench, are made up of the Purceli aeries, also of Pre-Cambrian agi while the floor is covered with Devonian limestone. The fault ^n the east side of the trench was first determined by Dawson.' The fault on the western side of the trench occurs in the valley of Gold creek, which lies within the first range of low rounded hills. The throw of the fault varies greatly and on the whole, is not large. The complexity of the structure of this down faulted block is greatly enhanced in that in the Rocky mountains, the Devonian limestone rests conformably on the lower Palaeozoic formation, while in the Purceli range the De- vonian limestone rests unconformably on the Pre-Cambrian formation. Physiographic History. Since the Rocky mountains were built in early Tertiary and the faults on both sides of the Rocky Mountain trench are referred to this period of orogenic movements, it follows i uat the valley was initiated in early Tertiary timef *>ince thci. It has been in greater part an area of erosion Touring the earlv Pleistocene it was an area of depoation, giving rise to the St. Mary's silts. The shape of the Rocky Mountain trench has been somewhat modified by glacial action. > DawMn, G.M., G.S.C., Ann. Rept., 1885, p. 150 B. II m- •*! I ■B .. p '\ ■^..-: ^: ij? 172 ■^ ii«:- I : : "' 1 1 1 .r 1- •ill EXPLANAIION OF IYATE II. The contact of the fretted and non-fretted upland surface. Note the fli areas on the upland surface in the non-fretted area. (See page 9.) .-...!,.»j| J flBHil 173 ^ote the flat ige 9.) « }5 ite liitolil r,\ ^iiirftivv) lira ,Ti-4ii1 .li/j. :-.l'ili////'k) .^vhiiPiiif^M "i S^iU S'*'-^'"-'' ."^'•f ■ ,- '.1 i ■* i :i 'I 174 Explanation of Plate III. Farming land in neighbourhood oJ Wycliffe; Mt. Baker, and focilliill Purcell range in baclcground. (See pages 9 and 10.) 175 f'% i •i'i dZl .VI 3TAJH W KOIXAttAOsiitiij^ : "^ i 11 : t- U 1 176 'tt: ExrLANATioN or Plate IV. Rucky Mountain trench from the west. South flowing Kootenay rivei tie seen in middle ground. (See pages 9, 10, and 162.) l-i* 177 tenay nvcr can n ■' r -M' gl , ' sii. i9||j' li .■* ■'■?; - ( 5*^^ Cross section of Marysvilte anticline looking ^^n ^^^tai?. > _^g^ ^ f-^ifWm^-: ■ V -. T 1 1 ^r ^^ le looking touth along its axis. (See pages 9 and 93.) Plate V. 'I' !\ ■ i. M If • :;.#■; * : xt: :^'' aU* -1 .IV jnA.ii n- creek. (See page 10.) i' - ■; i. i \ - M 181 (See 'M ^ f -1* .1 ;.4! m 182 Explanation op Plate VIII. Continental glaciated area in neighbourhood of Perry creek. Note the eve sky-line and the continuity of the intentream divides. Compji with areas of alpine topography. (See page 10.) ' 4-1 4-. )te the c\en 1. Compart m I ^f:i^^ i- 4'* [ij. Z! liT/ >0>*i •«{' b?i T;;^r.! ;aj. r* 184 KXPLANAIION OF PLATE IX. Continental glaciated area in neigh bourho' .l» ' M •^ 'i:' f 1 < (' \\ , '^* 'I Cl;"^.. ;:su>iii •.»^"■/! .Jk^'w ■{!ii5i,,<,! ,'iei rwf^ .tfi 6,<.. .. ■«i»'/*' J^!"t.,"j,j ^ ^v>f i«« ■M 116 Explanation of Plate X. Valley of St. Mary river above St. Mary lake, looking west. Note ha valleys, facetted spurs, and flat valley floor. (See pages 10 aiic ii' III 187 Note hanging ages 10 and ll.j 3i '■'. ' XWf ;X .ITAJ*; 10 ;< >n.'»fA.M -vo."> • h9?i., l**;i l'> ?>( I !i imsOt d3'ji»i f>-»r jtt# .iisCTtj'SiCir.'wifr c *^l> X-' 'S-i ^g^ I- t •; J im Explanation of Plate XI. St. Mary lake 'rom the west. Shows the entrenched valleys ami 'ip or Cretaceous croeiun surface. (See page* 10 and 11.) lys anil 'iplanrf .) iii 1 IS -M I i -•■ -A-i/, «r»^ .j'lii i^nir I ft---.^ ■'I y , mtiM 190 ExPLANAnoN OP Platb XII. St. Mary prairie looking north; shows conts ?t of Purcell range and the prairi land. St. Mary river in foreground. (See page 12.) w .; 1 1 191 id the prairie m >■ ^-k ■t J«" #»i II'; »i^ '■.-;: IVii'! -**^- .-l"^. !'« a}»' f . . .•: :-v V '1 i f ' n 192 i m^ -i If t: '■ 1 y Explanation of Plate XIII. » Upper and Lower Moyie lake*, looking north from St. Eugene mine (S page 13.) 193 i^ |l|! Ir^^^H^BS 1 V'-'.i H ^^^^^^n t; I 1 K", VJX ^n. .'! 10 VtOjTA/j. lijfij ^ 194 ofAMMii aiMin.) Em^uiMioii or ItAts XIV. kiPjnMUGiwfc CS» tm 195 PLATB XIV. u ^1i li iff li'i II I f^i^l i i ■%►. -*\ . VX ITA.I'I VI 'uii/.-i/, l|>r?i 1 xKqu] 'Ylfi- Ti!iJ<| "■■■%^.f. ' t 1% ;; K.vPLANATioN or Plate XV. A. Limestone of Kitchener formation showing peculiar weathering on the bedding plane. (S?e page 32.) B. Weathered surfari- of Kitchener limestones at right angles to bedding plane. (See page 32.) 197 Plate XV. A. ng on the D bedding B. I I f B'lli I ■■ 'ii ^CT :>'X rrtAj'l %o »..:i/..A.r!xa !'. iJiJiij »'■ ,noii(,fniol itjyi^ .»Wi£ij i.iit/ .A JX -faw; 3^) -^via U^u,^.n iUil-..,,, .noijiirnioi ri-.,-« ,«>|-itij hiiM. li. rt* ■j 198 I ' I Explanation or Plate XVI. A. Mud craciu, Siyeh formation, one-half natural size. (See page 34.) B. Mud cncks, Siyeh formatioa, one-half natural aae. (See page 34.) Ke34.) (e34.) i| >« i^^^ I I i i C:: 1:; ■ f li (m. ■ f MfX >#ti»)J|.„ , If ■l..J^-I f # 1 jy 202 i: Exn.ANATioN or Platr XVIII. Elko formation; limeatone showing coral-like markings. (See page 47.) 203 Plate XVMI. M I If I 1 I I I p '; ! > ■wr .,*' fi 204 EZFLANATIOM OT PLATE XIX. A. Idiomorphic crysul of funet embedded in fiiie-graiiied gmfena of Sullivan mine. (See page* 111 mad 132.) B. Photomicrocnph o( St. Eugene ore. Black arcaa, magnetite; greyish black, garnet; fibrous mineral, actinolitc; X16, croM nkols. (See page* 112 and 123.) 205 (mkfia uf s; greyish ol*. (See Plate XIX. B. juJid *i| I • t 1! diji ■n •>as>? *jc:i ■ >■ iflfil Bftiir- mr-.jj di • t i u 206 ExfLANATION Or PLATE XX. Moyie city and St. Eugene mine from acron Moyie lake. (See page 118.) 207 18.) ii I '!i I iff I i I : mi 206 Explanation of Platk XXI. Aurora mine from acre*. Moyie lake. (See page 123.) 209 i t I i^ li :"' ' i'i li 111 I • Wi Pi.Atl XXII ">!>iili|lij* a. .^A. MICaOCOPY RESOIUTION TBT CHART (ANSI and ISO TEST CHART No. 2) jj /APPLIED \M/«3E Inc ^ 1653 Er.sl Uoin SIrmt Ro€h«»tef. N«w York 14609 USA (716) »»2 - 0300 - Phon« ('16) JM-59e9-Fo« ''11 u 210 f i i i Explanation of Plate XXII. A. Photomicrograph of Sullivan ore. White areas, garnet, black areas, sulphides. B. Pyritic zone of Sullivan ore; shows numerous round dark patches colour- less crystals of garnet. Idiomorphic crystals of araenopyrite are present but do not show in photograph. The fine-grained matrix consists of an intimate mixture of pyrite, pyrrhotitc, and zinc blende. (See page 132.) .tt H\- I 211 k areas, s colour- nopyritc i matrix c blonde. Plate XXII. i-i r ;/?;/ '. !; '", y. Hr»ui«i m Wirty,r..Tft:: ■'■•^' •n-.iii , -i-'i a 'ft'.^---- .,f^,^..^^.^... 212 Explanation of Plate XXIII. A. Polished surface of Sullivan ore, showing methods of replacement. (See page 133.) B. Polished surface of Sullivan ore. The needle-like forms are pyrite pseudn- morph after muscovite, dark background is quartzite. (See page 133.) if #' H: : t. (See pseucln- ge 133.) 213 i ■ M Si ■ ' 1 .^ >'^-^ •i l| 214 ExrLANATION OF PLATE XXIV. l.<«kinK wMt from head of Pyramid creek. Alpine topography and frette.1 upland surface. (See page 166.) 215 I freltH I/Sf. ..„,,., I"!'.- 1>9 Ei;tl; \cy :i '■.- c > = S :ii ■ 4,i • 1 216 'iHtri M-n I EXPLANATIOK OF PlATB XXV. Glacial dique on borier between the alpine and continental gkdated upland ■urface. (See page 166 ) . k " 217 i upland i i f li -4fl ***'■ v-V- V;;.' -....-• . -, , * '■■■ . V 218 ExfLANATION OF PLATE XXVI. Glacial amphitheatres at t:e;»d of WTiitefiah creek. (See page 166.) 219 (ES i 220 Explanation of Plate XXVIl. Hanging valley and facetted spur, in the main valley of St. Maty river. (See page* 11 and 166.) 221 Plate XXVII. 16 PtATB XX vm. -aST. Panorama of vicinity of Crai ity of Cranbrook. (See page 3.) irj, •" -n^fia K. -^^rW '.^^pij. ; ^T ■i 222 Explanation of Plate XXIX. The U-shaped valley of Baker creek, looking east. (See page 11.) ■1 223 mi 1 K 1 > i ^_| 1 K^H ; til B '1 f'-l • r.'.j'f V, /(;/r/. >!/.,■!, ff -"i^r^f '■•**'"' «'"='«■*, *^"*'«ri...M'+. (Hir.. 'K-Tife^. Vi- i^V_.^«--irr^' ■■^-'s.>*;%^^^jif '"P-^^ m 226 EXFLANATION OP PLATB XXXI. Detailed view of a drque. (See ptgt 9.) 227 i ^''.t IfXXX atMf 10 wr o^^lAY.t •,.:; •'-""'^f'"'': iu hooihti-xfrhi,,^^, ^i ^^.^ * ,.--* 'w ^ mmm 22» Explanation of Plate XXXII. Looking west up the St. Mary valley in the neighbourhood of Marysville. (See page 10.) *!■ 4B I -I I 229 ) mtm ^^^^^ i- ^M * m m i\-' H m ■ fi'-.L .my. -0? -Si-** Bonnell. Dr 1*' Bootleg basin **' Bourgeois, Mr *^^ Bowles, O "® Bradford's quarry ** Brayton, E. G 1** Bright. H. A »** Brock, R. W *' Burchett, W. C »^ Burling, L. D **. ** Burton formation *^ • « age of ** • « unconformity at the base ♦* C. Calcite 60, 61, 62, 77, 81, 106, 108, 120, 142 Camarophoria explanau (McChesney) ^ Camaro'^oechia cf. C. meullica (White) '•' Cambrian "^ »<» " claim described *2S Cameron creek *' Canyon station *"* Carbonates 108, 142 Carboniferous *^ Cebatha (Cocculus) n. sp ** Cerusrite 108,109,127 Chalcopyrite 83,108,120,142 Cherry creek *^ Chlorite " Cissampelos ? " Clarke, Mr ** 235 Chy * depoiiu Claiver, Jno. . Cough, C. T. . ! C«*«»t bloom. C«»>1«. Father Coeur d'Alenei ccLmSifS::^^'^-''-''-;:::;::::::::;;;;;; Communfcation. mean* of Connell crack i"wxy; Connor, M. F. ^^^^^.^■^: Copper ; P'2*rtJe..'de.cription of." ■. pyritet nilphide. Copper-goW deporiu ...'..'. • m ' ' ' ^ •geof chai»cter of . . . «tribution lithology nieUmorphinn. ■tnicture thickneat 'Act • • 152 2 ■■■ 130 56 IS 101 143,146 119 113 2 8 3 56 162 58 •2, 118, 130 68 106 141 144 • 108 62 • • . 140 • • • . 144 • • • • 141 • . 140 • • • 141 •■. 144 • . 143 •■• 134 • • ■ 152 93, 94 45 ■ 156 99 56 ■ 28 28 29 30 31 29 101 102 236 Crctaoeout geo«yncline ■ peneplain, evidence of. Cronin, Jam:* FAOB 102 164 119 D. Daly. R. A.. 5. 20, 23, 29. 35. 37, 40, 41, 49, 50. 63. 64, 66, 68. 70. 72 77 94^ 101, luU, 102, lOo Daw«,n.G.M 5.41.43.91.96.169 Devonian Devonian-CarboniferoiM epoch lAi' ;«, 1« Diopride 106. 109, 132 Drainage, relation of to ttructure "J Dryedale.C.W *^' "J Duncan river East Kooteray Placer Mining Company J*' Fclipse claim deicribed ' Elko * formation, age of. 47 I -•- - ay correlation ,L' ,. Z, c -j^ 60. 61. 83 Epjdote ' Erickaon road •• Erythrite *"■ J* Evans group of claims described '*• Fagus, n. sp Farrell. Mr Faulting, age of. Faults Fauna Feldspar Ficus. n. sp Field work Finch, John Fissure system of Moyie area ■ * St. Eugene mine. Flora Folds Fort Steele * * mining diviaon Fossil content of the St. Eugene nha. 62 88 138 95 93 14 ,64 89 2 119 118 120 14 92 11 105 87 237 O. G«bbR> • variadomin... G«lbcaith.W.. CMtnt Galton rcriet. '**• G^t. ..'. .'*'"'°" °^ '° "* P«"*ilterie.".;: Gateway epoch. !.........'.'.'.' formation • a . , oetcnbed , * ^^"ribution.....!..,. , Uthology , "^ •tructural relationa .... General «atement Geological luMory ^^iogy, economic. Seneral ' structural..... Glacial period Gladation Glacier Goat canyon " river Gold ' Gold creek ' Creek fauit.V. '..!.■ * placer " • iiul«. ''f^P'ion of proper^ie,; .■.■.'.■.■; «juartx vemt described , • description of properties. ".'. . , , mmeralogyof , ^ persistency of f. . ' values Gramte " mine of Idaho. Granites II «gc and correlation. distribution lithology " rtnictural features.. Gumdon group of claim, descri W '...', 'AOB 51 ■■■ 39 J07, 120. ur/iM. 132, ,J 2. 20 •• 49 *♦• W. J06, 109, 120 99 42 36 36 36 37 37 1 98 104 19 92 103 103 9 157 13.94 :• 137 ". 94, 102. 161. IM 166 1. 147 147 136 139 137 137 137 63 113 78 84 78 80 82 125 238 Hmll Uke. PAGB 10,79 IN Halliway, D >*« Hanging valteyf 1* Hanton, G ' • Mr »5» Hardman, J. E ^^ Harker.A " Hell* Roaring creek 1». " Henuktite ''' Hicoria, n. ip. ? ** History, geological " Hollick, Arthur 87, lOJ Hoodoo* *' Hornblende 60, 61, 62, 66, 81 Howe'i claim **^ Hyperttbene ** IntergUcial 91. 103 Irene conglomeratet " Iron pyritea ^^ • sulphide *2 Irrigable areas ^* J. Jameaontte *^ Jefferson, age and correlation ** distribution '^ lithology ^ relation to older formations 5^ thickness ^ ( ?) limestone ^ limestone correlation *8 Jennings, Robert *** Jurasric 96.91, 101, 117 4 Kaslo 1*1 Kimberley area ^^' Kindle. E. M *8, 54 Kintia Canyon ^ i» Kitchener epoch ^ formation I I deKribed..'.'.' , " diftribution. . . , * Utholoty , * Mructure 1. thickncM. Kootenay-Columbia vaJIey Kootenay Landiiur " Uke.. ^ river River valley.... i].' PAGE 99 9, 56 31 31 32 33 32 96 159 .8, 159, 167 8, 10 '. 162. 165 Labradorite L«ke«, oxbow. ... . Langill, Mr Uad-ulver depo«t. de*»ibed i-icnite • beda.V. '....'.■ Limestone Limonite Lindgren, W......'.'" Location Luke creek........ .108, 37. 77 11 133 106 87 166 2 127 84 2 12 MacKay, Chaa. A... McConnell, R. G... McDonnell, J McEvoy, J McGillvray range McKay clain Jeacribed ' Mabelle claim described Magnetite _ " titaniferous "•alachite Mann, D. P Mark creek Marysville fault... ... ." " smelter.... Maacot claim described..... 125 84 149 5, 41, 55, 165 92 145 125 58, 64, 108, 120 64 143 133 130 94 130 135 .11, MtJ 240 PAGE Matthew creek H. M MeUUic depoeits 10* Microcline ** Micropegtnatite 61 Microperthite ^ Mineral production of East Kootenay 105 Mineralogy of copper-gold deposiu 141 • gold-quartz veins 137 " silver-lead deposits 106 Mines and prospects, description of 117 Minister of Mines, Britidi Columbia 1*7 Mispickel >07 Mississippian 56 Montezuma tunnel ^48 Moyie area ^^^ ' ' fissure system of H* • fault 94 " mountain 76 • lakes 13 • range 92 ' river 12,147,162,165 • siUs 57, 70 Mud-cracks 38 Muscovite 64, (^7, 133 N. Native elements 106, 137, 141 Nelson granite *1 Non-metallic deposits 104 North Star hUl 133 • • mine 104,106,107,108,109 • • • described 133 O. Oligodase 61 Omineca claim described 147 Orthoclase 61, 62, 67, 70, 80 Orthothetes chemungensis var. arctostriatus 48, 54 Osann, Mr 64 Oxides 108, 137. 142 241 g^War™ation.oftheP„r«U«„ge. " Bay creek "u-k claim Peavine creek Peneplain, Cretaceous! Peny creek ; Creek Hyd^ulic Mining Company. .. Perthite..."""*.^''""«"y •-. Phillips epoch formation Phosphates Physiography n. genesis of Pirsson, L. V Placer deposits. • gold mining Plagioclase Platanus, n. sp. ......' Pleistocene deposits. . Pollens' claim Populus ft*-Cambrian « « , nietargilUte I^iuln..'^'"'^'^'* ••••••■■•■•• Previous workers ^fchard formation of Idaho P™« River terrane.. P^uctella cooperensis (Swallow) * age of * correlation distribution * external relations. lithology metamorphism. ' thickness... range PAGK 53 147 93 1« 94 :: 164 10. 11. 136. 147 147 140 81 100 42 110 160 162 64,66 2 1, 147 ". ". 64r67, 77, 81 90 85 143 gfl 19.41.69,96,144,161 154 2 IS 4 70 98 56 137 76, 99 69, 78 70 76 77 76 70 •••• 77 ••8,96,98,160,163 40 242 rACB Puroell •ediments, sources of *0 series 2, 19. 23. 83 • age and correlation *1 • correlation of with Coeur d'Alene biries 51 " origin of " sills 5* « age of ** " external relations *^ « internal relations *5 " lithology 5' " relation to Purcell lava W * structure of '0 ■ summary of genesis '5 trench ***'' * origin of "' Pyramid iMsin 67. 93 IVnmid creek ** Pyrite 83, 106, 120, 128, 132, 137. 142 Pyromorphite 108. 110, 127 Pyroxene ''• 58' 1*^ Pyrrhotite »06. 107, 120, 128, 132, 142 0. Quart* 58. 60, 61, 62, 64, 67, 68, 81, 106, 108, 120, 137 Quartz-diorite or transition roclt 62 Quaternary 103 " physiographical history 166 Railways ' Ransome, F. L "3. 115 Raymond, P. E 56 Redpath, Col 130 Replacement deposits 128 Ries, H 152 Ripple marks *> ^° Roads * Rocky Mountain geosyncline 19, 95 « • system 102 • trench 8, 10, 85. 96, 169 Rocky mountains 1^ Roosville epoch 100 " formation *2 Roas,W 1*' Running Wolf claim 13' MS 8. St. Eugene mine -acr : : ; de«ribed..:::::::;: "2- »«.»<». wr. 109. m • • .,* ^"^ •y«em of . . . H8 . . 'i^' 120 fit M. iL ■«' *nd correJation of . M, 103 at. Mary lake on m ■ . »U nvBT 56 74 ." : ^ '.W.25.93.16l.i« wits 74 SaltcrystalB " ,„ Saw Mill creek... ' r « I™" - -i»*.iatula 138 '*'' ic,atElko ....".'.'.' 54 , ^ «. IW • « deKribed "^ Sphalerite W Spirifer cf. S. centronatus (Wnchdl) ** " pionenM 48, 54 l^urs 1* Square butte *♦ Stemwinder mine ^^ « « described "5 Stropheodonta 5* Structure, regional " SulUvanmine 102, 106, 107, 109, 111, 112, 114 • • deK»bed 130 • Pat 130 Sulphides..."."."...!!.!!.!!!!...! 107, 137, 142 Sulpho-Mlts 108 Sun cracks 3 Superficial deposits " Sylvia claim described 1*3 Table, corrdation, British Cc^umbia and Idaho 32 • • of ore deposits H" ■ ■ * Pioche formation, Burton shale, and Albertella 46 50 50 51 ■ * * Purcell series and Galton series by Daly ■ * * Purcell series and Galton series by Schofield • « ■ Puicell series with Coeur d'Alene • of formations 21, 85, 164 Tabular geological history 1^1 « physiographic history 160 ■ section of the Moyie mils ^1 " statement of geological record 22 Tanton, T. L 2 Tarrant and Angus, Messrs 136, 146 Temperature ^3 Terraces l^' 13 Tertiary 96.102 " physiographic history 1^ Tiger-Poorman Lode 113 Tiunite 8^ Topography ° Trenches, origin of 1*^' Trow, A .S 1*8 Turner, Judge 130 245 Ulmus n. «p. ? Upland surface, de«iipii,i,i of Vernadsky Vitia, n. sp.?... V. PACK 89 162 27 90 W. Walcott, C. D Wardner formation * age and correlation.. distribution lithology. 40,51 169 55 56 55 relation to older formations. .....".' ^^ • younger formations. . . II thickness mines Warren, C. H Watuburg station Weaver creek ^t Kootenay granite batlioMth Whitefish creek Wild Horse creek Willis, B Wind gaps Woods Bros. ... Wright,L.E... Wydiffe • drift ! Vahk anticline mountain * river Yankee Girl claim dMcribed. 55 55 115 58 56 147 19 11. 143, 145 1 37 162 133 2 154 103 .102, ..85, Y. 92 78, 103 13 146 Zinc-blende Zoisite 107, 120, 127, i28, 132 63, 70 M I 7 LIST OF RECENT Rgp^ OF GEOLOGICAL •«n^*^lS^,j;«^ the GeologiaU Survey have 2. etc. Owi^r?eSb^.T'r^^««*^e«^ -Ki their^cSnpaaJrZf^^ the puWiddag of «port. «Ited memoir.. S'^^^Pf.*" «»' the leport. have hS "der otS^^^^^^ ^^ »«t been i«ued in the «« h" been P^tS"^,*:;' '^<«. the foUowSJ of the Geok^ Survey !:; tl^^j^P^S^^ Memoin and Reports Publlahad During 19M. m REPORTS. Report on • mtdogkaX reconnaiwance of the nsioii tnvcned by the National TcanacondiKntal rulway between Uke Nipigon and CUy lake, Ont.-by W. H. CoUin* No. 1059. , u i. u i Reoort on the geoloskal pontion and chanctenatici of the oU-ahak depoelttlf Canada-V R. W.^Ells. No. 1107. v o ., o A reconnaiaance acroM the Mac ken ne mountaina on the Pelly, Rom, aad Gravd riven, Yukon and North Weet Territorica— by Jowph Keeie. No. 1097. Summary Report for the calendar year 1909. Na 1120. MEMOIRS-GEOLOGICAL SERIES. No. 1, Ceolopeal Striu. Geology of the Nipigon bMin, Ontario —by ABred W. G. WIkmi. . , , „ ^ No. 2, Coohtieai Smes. Geology and ore depodu of Hedley mining district, British Columbia— by Charles Camsell. No. 3, Geelofical S«n$s. Pabeoniscid fishes from the Albert shales y John A. DreMer. MEMOIRS-TOPOGRAPHICAL SERIES. Muon 11. No. 1, Topopapkical Series. Triaogulation and spirit levelling 1^ of Vancouver island, B.C., 1909— by R. H. Chapman. Memoin and Reports Published During 1911. REPORTS. Report on a traverse through the southern part .^ the North West TerritoriM, from Lw: Seul to Cat lake, in 1902— by Alfred W. G. Wilson. * Report on a part of the North West Territories drained by the Wnisk and Upper Attawapiskat rivers— by W. Mclnnes. No. 1080. ^ _, , . Report on the geology of an area adjoining the east side of LakeTimiskam- Ing— by Morley E. Wilson. No. 1064. Summary Report for the calendar year 1910. No. 1170. MEMOIRS-GEOLOGICAL SERIES. Miuon 4. No. 7, Geotopcal Series. Geological reconnaissance along the line of tne National Transcontittental railway in western Quebec— by W. J. Wilson. Mnioa 1. Mnioni 2. Mbmou 3. Mmon 5. Mkmou 6- Msuon 7 «ritJd. Col«™b«-|^ Will5S'H*°K3i .SXTr*^ REPORTS. ^ REPORTS, ETC. ^"c^^l^l ^«^- »-«««,„ Quebec «., u. M.riti« Guide beck Ho. i. EKuniMM in the iiei(hbwirfaood of Moatraal aiid IK) Otuwa. Guide Book No. 4 Guide Bodi Na S. Manitoulin iiland. Guide Book No. 8 ExcurvoiM in touthweMern Ontario. ExcunJoiM in the wcitcrn peninmla of Ontario and . = — -., — r,"-'- - Toronto to Victoria and return 9ia Canadian Pkdfie •^ ^S?^ ?2P*^ raUwaya: paru 1, 2, and 3. '-•»«»» ^aew r-^Sr^^^^i-^- T«?"f«>»» Victoria and return »Ai Canadian Pacific. Grand Trunk ftdfic. and National TranKontinental raUwayir^ ^^' V u£"S?_?** ^i- .*"• E«««"«>M in Northern Britiah Columbia and Yukon Territory and along the nrnh Pacific coatt. *-«»nioia ana MEMOIRS-GEOLOGICAL SERIES. Muran 17. NcU. ,C«»i2*if^*~M. Geology and econo.r.«c re«>uf«ee of the Larder Uke dirtrict, Ont., and adjoining portion* of Poottac county. Que.-by MorIe>- E. WO*>n. •" "^ " b G*A^^^^' ^*'"^ «*'*'*«• New Brunawick— N0.lO,GtohsiaaS*rits. Wheaton diatrfct, Yukon Territory— by D. D. Caimet. No. 29, GeoloriaU 5mM ReconnaiMance along the National TwMcontlnental railway in southern Quebec— by John A. ^'d'd^S^^^"^' **'***»"•«»' Atlin dietrict. B.C— by ^"•r^-Sff^Hu"^- 9^^^ o* t»«* North American 55!!!2"a^j "* forty-mnth parallel, Parte I and II— by Reginald Aldworth Daly. Memoln and Reports Published During 1914. REPORTS, ETC. Summary Repmt for the calendar year 1912. No. 1305. ^ ♦.i^^^^'r^ ^°?-A '• *• K^' "«• 8 contain artkJ. > 13 to 22 ofthe GM^ical Series of Museum bulletins, article No. ? . the Anthr«^ •^Sd^SSi.'H'^l^u^?!*"! '"IS ^'"'"P"" Series of M .-urn Bulletins WyattlSESa^ "*™"^'' No- 1: Notes on radium-bearing minerals— by MUSEUM GUIDE BOOKS. bi.-^SSrU^KiSl'^r ISo. *• -""^ ^'*^ "^ ^""^ '^'"- MEMOIRS— GEOLOGICAL SERIES. MBMoa 23. No. 23, Gtv.otical Seriu. Geology of the Coast and islands betwero t&e Stimit of Georgia and Queen Chariotte sound. B.C.— by J. Austen Bancroft. MiMom 18. Mbihhs 26. Mbmoib 29. MxHont 31. Mmon 33. MKMon 35. Mbuoib 37. MBMon 38. MSMOn 25. MBMOn 3a Mmon 20. Mnion 36. Mbmou S2. MiMon 43. MBMoa 44. MBMon 22. Mmont 32. Muoa 47. MUKMl 40. Miuoot 19. Mbmoib 39. Mraon 51. Mmon 61. Mmont 41. Mbmoib 53. Mbmoib 55. pM&a of th* wMttrn proviiicM (Part II)— by Htinrkb RIm •nd Jimph Kaci*. Nt.40,G*ei»tiealStri«t. The Ixtiiw of Nckoa tiid Chnrchill ri«era-by WUUain McIudm. . . . .,..„, No. 4t, CtolotUal S*ri*i. Gold faUa M Nova Scotk— by W. Mftlcolin. __ «..„ .M ft S».»3,GtoUtftalStrUt. Geology of tb« Victoria and SMinlch maiMuta*, Vancoavcr UUnd. B.C.— by C. H. Clapp. N«. 42, Gtotoiieal Smi$. Gcolockal nottt to accompaoy map of ShMp River gaa and oU field, Alberu— by D. B. DowUag. N:3f,G«oietiealS*riu. St. HOaire (Belodl) and Rougraioiit mountain^ Quebec— by J. J. O'Neill. ^ .^ So. 37, Goohpcal Soriu. Clay and thai* depoaitt of New B.-unawiclt-*y J. Keek. Iio.27.G«ohtiettlS*rits. Preliminary report on the lerpentinea and aiaociatcd rocla, in ■outbem Quebec— by J. A. DrcMer. No. IS, (kolotical Strtts. Portion* of Portland Canal and Skeena Mining divtiions, Slnena diitrict. B.C.— by R. G. McConnell. No. 39, Giohpcal Soriti. Clay and ihale deporiu of th« western orovincaa, PMt III— by Heinrkh Rie* No. 24, GMbrical Stri**. The Archmn geology of Rainy bin —by Andrew C. Laweon. No.26,G*oloptalS*rUs. Geology of Mother Lode and Sunaet mlnea, Boundary dirtriet, B.C.— by O.E.LeRoy. No. 35, GtclotUal Switi. Kewagama L.alce map-area, Quebec -by M. E. Wil««. , , u „ , No. 43, Gooleticat Strus. Geology of the Nanaimo map-area— by C. H. Clapp. No. 45, GeoiogUei StrUt. Mooae Mountain dietrict, aouthern Alberta (lecond edition)— by D. D. Calmea. ^ ^ ., No. 38, GtoiorUal Stritt. The "Fern Ledgei" Carbpmferoua floia of St. John, New Brunawick— by Mane C. Stppe*^ No. 44, CtototiMl Series. Coal fiekU of Manitoba, Sadcatche- wan, Alberu, and eaitem British Columbia (revised edition) — by D. B. Dowling. No. 46, Geohrieal Series. Geolosy of Field map-orea, Alberts and Britisa Columbia — by John A. Allan. MEMOIRS-ANTHROPOLOGICAL SERIES. Mmon 48. No. 2, AnikropolotUal Series. Some myths and tales of the Oitbwa of southeastern Ontario— collected by Fi»ul iudin. Mmon 45. No. 3, AnHuopolopcal Series, The inviting-in feast of the Alaska EsBmo-by E. W. Hawlws. u «, « Mmon 49. No. 4, Antkropdopcal Series. Maleate tale»-by W. H. Mechling. „. . . , ... Mmon 42. No. I, Anlhropohrical Sertes. The double curve motive in nortlwastcm Algonkian art— by Frank G. Speck. MEMOIRS— BIOLOGICAL SERIES. Mmon 54. No. 2, Biological Series. Annouted list of flowering planU and ferns of Point Pelee, Ont., and neighbouring r -" by C. K. Dodge. n Mamoin sdJ Reports PublialMd During 1915. REPORTS. ETC. SumiMnr Report for the rilencUr jreur 1913, No. 1359. Report from AnthropoloK" . ' DivtMon. Separate from Summary Report Report from Top ^aphlM Ohriaioa. Separate from Summary Report Muaeum Bui. ' . 4 :. c j^ >. 3, Anthropdotical Siri4s. Pre-hiatoric and preaent commei r ii.iung tlw ^jvtk Coaat Eddmo— N. Stcfaiuaoa. Muwum Bullet i> In. ". :' i. 4, Antkropologkal Stritt. The Klencid foiaa in the skull ol i . .' ,ai,f^ • . H. S. Knowlea. Muaeum BuUetit No. 11 A < . 5, Uialorxal Stries. The double crtntd cormonnt (Pkalaeroe. x a/ '.. Ita rela'ion to the nlmon industriet on the Gulf o< St. Lawn m -1- ^vemer. M»..' ' )1RS— t;r A. MiMOn 60. Muon 67. Muion 59. MBiioni50. ^'^v> - SERIES. . :sada island— by R. G. McCoa- <\riiaig-Antigoniah diatrict— by M. Mbiioix58. No. 4* ', u/.it/y nell Ko. 47, u. iogiefU . ern-s. Y. Wiliama. No. 49, jlo^col ler. The Yukon-Alaaka Boundary be- tween Poicupine and ^ nkon rivers — by D. D. Caimea. No. 55, Oeohfieal Series. Coal 6elds and coal leaourcea ot Canada— by D. B. Dowling. No. 51, Oeelotical Series. Upper White River District, Yukon —by D. D. Caimea. MSMon 66. No. 54, CeoUtical Series. Clay and shale deposits of the western provinces, Part V— by J. Keele. MKUOIH65. No. 53, Ceolotical Series. Clay and shale depoirite of the western provinces. Part IV— by H. Riea. Mkmou 56. No. 56, Ceolotical Series. Geology of Franklin minim camp. B. C— by Chas. W. Drysdalef Mmon 64. No. 52, Ceolotieat Series. FVeliminary report on the clay and shale deposits of the Province of Quebec — by J. Keele. Muion57. No. 50, Ceolotical Series. Corundum, iu occurrence, distri- bution, exploitation, and uses — ^by A. E. Barlow. MemoirB and Reporta In Preaa, May 8, 1915. Mnont 62. No. 5, Anikropolotieal Series. Abnormal types of Kiecch ia Nootka— by E. Sapir. MSMOnt 63. No. 6, Anlkropolotieat Series. Noun reduplication in Comooi, a Saliah language of Vancouver island— by E. Sapir. Mmon 46. No. 7. Anthrofolotieal Series. ClaasificaUon of Iraqaoiaa radicals with subjective pronominal prefizee— by C. M. Barbeau. Mmon 70. No. », Anthropoheical Series. Family hunting territories and social life of the varioua Algonldan banda of the Ottawa valley— by F. G. Speck. MsMon 71. No. 9, AnOiropolorieaf Series. Mytha and folk-kn of the T imi s k a ming Algonquin and Timagami Qjibwa— by F. G. Speck. UMMoa 69. No. 57, GeoioriaU Series. Coal fields of Bridah Columbia— 34. Il0. M, GmUtkal 5Mm. ^1m DtvoniM of toathwMUn OatMrio—by C. R. Suuffa 73. N».$t,G*iiotiutS*rU». The ?Wmoccm mmI lUcMt dqxMiu of tiM bkod of MofMiMl— by J. Sunaficld. MmotB 68. Me. S9, Cmlotieal SeriM. 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