British Columbia Geological Survey

Publication Summary

Issue ID:	B001
Title:	Aiken Lake Area, North Central British Columbia
Author(s):	Lay, D.
Series Name:	Bulletin
Publication Year:	1940
Scale:	1:400000
NTS Map Sheet(s):	094C/3,4,5,6,11,12;094D1,8,9
Place Keyword(s):	British Columbia, North Central British Columbia, Aiken Lake
Lat/Long (NSWE):	56.75, 56, -126, -125.5
Theme Keyword(s):	Geology, Mineral occurrences
Download(s):	PDF
Abstract:	Bulletin 1 discusses geology and mineral occurrences in the Aiken Lake area of north-central British Columbia. Aiken Lake area is defined as a strip of country about 30 miles long and 10 miles wide, trending northwest through and east of Aiken and Uslika Lakes. These lakes are near the headwaters of the Mesilinka and Osilinka Rivers respectively. The earliest known mining activity in this region was the discovery of placer gold on Jimmay Creek in 1899 by James May, one of the pioneer prospectors in the northern part of the Province. This was immediately followed by some work on the creek by an English syndicate. Subsequently, save for the individual efforts of a few prospectors, the region was inactive for many years. Discovery of Ferguson and Childhood's Dream to the east in about 1925, doubtless stimulated the revival of prospecting in the adjoining Aiken Lake area, to which, at that time, attention was drawn by the reports of the Geological Survey, Canada, and of the Minister of Mines, British Columbia.

Issue ID: B002Title: Placer-Gold Deposits, Wheaton (Boulder) Creek, Cassiar DistrictAuthor(s): Holland, S.S.Series Name: BulletinPublication Year: 1940Scale: 1:18000NTS Map Sheet(s): 104I/6,7Place Keyword(s): British Columbia, Cassiar District, Wheaton (Boulder) CreekLat/Long (NSWE): 58.413, 58.311, -129.039, -128.927Theme Keyword(s): Geology, Placer-gold DepositsDownload(s):
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Bulletin 2 discusses placer-gold deposits in Wheaton (Boulder) Creek, Cassiar District, in northern British Columbia. The Cassiar district has long been known for its placer and lode-gold possibilities. The discover in 1873 of rich gold-bearing gravel on Thibert Creek led to the finding of placer gold on Dease Creek in the same year, and on McDame Creek in 1874. After a long period of inactivity and small gold production, placer gold was found on Goldpan Creek in 1924. Later, in 1934, gold-bearing quartz veins were found on Quartz Creek at the head of McDame Creek. Interest in the district was again renewed by the discovery in 1937 of a 52-ounce 15 dwt. gold nugget on Alice Shea Creek, a tributary of Wheaton Creek, and the discovery in 1938 of rich, shallow pay-gravel on the Peacock lease (No. 345), on lower Wheaton Creek.

Issue ID: B003Title: Fraser River Tertiary Drainage-history in Relation to Placer-gold DepositsAuthor(s): Lay, D.Series Name: BulletinPublication Year: 1940Scale: 1:3000000NTS Map Sheet(s): 093;Place Keyword(s): British Columbia, Fraser RiverLat/Long (NSWE): 54.115, 51.709, -123.23, -121.695Theme Keyword(s): Surficial Geology, Tertiary Drainage, Placer-gold DepositsDownload(s):
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Bulletin 3 discusses Fraser River Tertiary drainage-history in relation to placer gold deposits (Part I). To supplement the report on Horsefly area published in the Annual Report, Minister of Mines, BC, 1938, fieldwork commenced at the early part of the 1939 season in Beaver Creek Valley to delineate further the Tertiary Horsefly River drainage. It then became evident, however, that the Tertiary drainage histories of the Fraser and Horsefly Rivers were so closely linked, that further investigation in the Horsefly area should be preceded by an examination in the Fraser River Valley. This was done.

Issue ID: B004Title: Saline and Hydromagnesite Deposits in British ColumbiaAuthor(s): Cummings, J.M.Series Name: BulletinPublication Year: 1940Scale: 1:400000NTS Map Sheet(s): 082;083;092;093;094;102;103;104;114Place Keyword(s): British ColumbiaLat/Long (NSWE): 60, 48, -139, -114Theme Keyword(s): Geology, Saline and Hydromagnesite DepositsDownload(s):
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Bulletin 4 describes saline and hydromagnesite deposits in British Columbia. Deposits of sodium and magnesium salts occur in various parts of the interior of BC. Most of them have been known for many years and some commercially exploited on a small scale. The more important of these deposits were investigated by the writer during the summer and autumn of 1937. This report brings together information based on this fieldwork as well as previously published reports.

Issue ID: B005Title: Mercury Deposits of British ColumbiaAuthor(s): Stevenson, J.S.Series Name: BulletinPublication Year: 1940Scale: 1:300000NTS Map Sheet(s): 082;083;092;093;094;102;103;104;114Place Keyword(s): British ColumbiaLat/Long (NSWE): 60, 48, -139, -114Theme Keyword(s): Geology, Mercury DepositsDownload(s):
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Bulletin 5 describes mercury deposits in British Columbia. This report includes geological descriptions of all the known occurrences of mercury in BC. With the exception of the reported occurrence on the Homathko River, all the deposits were examined by the writer during the field seasons of 1938 and 1939. For the sake of completeness and introductory chapter is included that describes the mineralogy, metallurgy and modes of occurrences and economics of mercury. Issue ID: B006Title: Geology of Camp McKinney and the Cariboo Amelia MineAuthor(s): Hedley, M.S.Series Name: BulletinPublication Year: 1940Scale: 1:10000NTS Map Sheet(s): 082;Place Keyword(s): British Columbia, Cariboo, Camp McKinneyLat/Long (NSWE): 49.125, 49.092, -119.229, -119.159Theme Keyword(s): Geology, Mineral DepositsDownload(s):
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Bulletin 6 describes the geology of Camp McKinney and the Cariboo Amelie Mine, Similkameen District. Camp McKinney is in the Greenwood Mining Division on Rock Creek drainage, about 9 miles north of the International Boundary and 6 miles north of Bridesville on the trans-provincial highway. A branch-road leaves the highway 3 miles east of Bridesville and passes through the camp westerly to Oliver. The camp is 6 1/2 miles from this road-junction and 22 miles distant from Oliver. Rock Creek, on the Canadian Pacific Railway (Kettle Valley Branch) is 16 miles southeast of Camp McKinney. Issue ID: B007Title: Lode-Gold Deposits of the Upper Lemon Creek Area and Lyle Creek-Whitewater Creek Area, Kootenay DistrictAuthor(s): Maconachie, R.J.Series Name: BulletinPublication Year: 1940Scale: 1:90000NTS Map Sheet(s): 082;Place Keyword(s): British Columbia, Kootenay District, Upper Lemon Creek, Lyle Creek, Whitewater CreekLat/Long (NSWE): 50.167, 50, -117.333, -117Theme Keyword(s): Geology, Lode-gold DepositsDownload(s):
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Bulletin 7 discusses lode-gold deposits of the Upper Lemon Creeks area and Lyle Creek-Whitewater Creek area, Kootenay District. Fieldwork in the area adjacent to the headwaters of Lemon Creek, undertaken during the 1939 season, was complementary to similar work completed on the lower reaches of the creek during the previous year. Similar conditions prevail generally throughout these two entirely arbitrary subdivisions and reference to the Annual Report, Minister of Mines BC, 1938, which contains data on conditions farther down the creek, will probably be of assistance and permit a broader conception of the region as a whole. The sketch map which accompanied the 1938 report (Figure 1) together with Figure 2 (which accompanies this report), cover Lemon Creek for its entire length. Lemon Creek joins the Slocan River about 6 miles south from Slocan City. Issue ID: B008Title: Preliminary Report on the Bedwell River AreaAuthor(s): Sargent, H.Series Name: BulletinPublication Year: 1940Scale: 1:100000NTS Map Sheet(s): 092FPlace Keyword(s): British Columbia, Bedwell RiverLat/Long (NSWE): 49.5, 49.333, -126, -125.667Theme Keyword(s): Geology, MiningDownload(s):
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Bulletin 8 gives a preliminary report on the Bedwell River area, Vancouver Island, BC. The Bedwell River rises in the southwestern part of Strathcona Park, and empties into the head of Bedwell Sound on the west coast of Vancouver Island. The name "Bear River" was frequently used in old reports. The head of Bedwell Sound is about 16 miles north of Tofino and Clayoquot which are ports of call about 35 miles north of the entrance to Barkley Sound. Most of the area tributary to the river is in the Clayoquot Mining Division but the eastern part lies within the Alberni Mining Division. Issue ID: B009Title: Molybdenum in British ColumbiaAuthor(s): Stevenson, J.S.Series Name: BulletinPublication Year: 1940Scale: 1:1000NTS Map Sheet(s): 082;083;092;093;094;102;103;104;114Place Keyword(s): British ColumbiaLat/Long (NSWE): 60, 48, -139, -114Theme Keyword(s): Geology, MolybdenumDownload(s):
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Bulletin 9 discusses molybdenum in British Columbia. This bulletin includes a key map and includes geological descriptions of molybdenum deposits visited during the course of fieldwork from 1937 to 1939, inclusive. With the exception of the deposit at Alice Arm, all the more important deposits and many, though not all, of the less important deposits in the Province were visited. J.T. Mandy of the Department of Mines examined the Alice Arm deposit in 1939, and a synopsis of his report is included here. An appendix is included which gives brief notes on known occurrences of molybdenite in BC that have come to the attention of the Mines Department. Issue ID: B010Title: Tungsten Deposits of British ColumbiaAuthor(s): Stevenson, J.S.Series Name: BulletinPublication Year: 1941Scale: 1:9000000NTS Map Sheet(s): 082;083;092;093;094;102;103;104;114Place Keyword(s): British ColumbiaLat/Long (NSWE): 60, 48, -139, -114Theme Keyword(s): Geology, TungstenDownload(s):
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Bulletin 10 discusses the tungsten deposits of British Columbia rewritten in 1943. This is a complete rewrite of the earlier bulletin published in 1941 with the same title. Expansion and revision was made necessary by the many new discoveries of scheelite made in the last two years which have shifted the emphasis on certain areas of the Province and on certain types of deposits. The various data are brought as much as possible up to date as of March 31, 1943, although it has been impossible to keep abreast of all current development. Issue ID: B011Title: Fraser River Tertiary Drainage-History in Relation to Placer-Gold Deposits, (Part II)Author(s): Lay, D.Series Name: BulletinPublication Year: 1941Scale: 1:2000000NTS Map Sheet(s): 093;Place Keyword(s): British Columbia, Fraser RiverLat/Long (NSWE): 54.667, 53.167, -123.333, -120.917Theme Keyword(s): Surficial Geology, Tertiary Drainage, Placer-gold DepositsDownload(s):
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Bulletin 11 describes Fraser River Tertiary drainage-history in relation to placer gold deposits (Part II). This report supplements Bulletin No. 3, 1940 and continues the investigation of the Fraser River drainage as far as the Grand Canyon, 109 miles up-stream from Prince George. The river, confined for 120 miles up-stream from this point, emerges from the Rocky Mountain Trench through a wide local break in the north-northwesterly continuity of that great valley. Issue ID: B012Title: Reconnaissance in the Area of Turnagain and Upper Kechika Rivers, Northern British ColumbiaAuthor(s): Hedley, M.S., Holland, S.S.Series Name: BulletinPublication Year: 1941Scale: 1:250000NTS Map Sheet(s): 094L; 104I/1,2,7,8,9,10,15,16Place Keyword(s): British Columbia, Northern British Columbia, Turnagain River, Upper Kechika RiverLat/Long (NSWE): 59.333, 57.75, -129.5, -126Theme Keyword(s): GeologyDownload(s):
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Bulletin 12 discusses reconnaissance in the area of Turnagain and Upper Kechika Rivers, northern BC. The Kechika and Turnagain Rivers together drain a region greater than 6,000 square miles in extent in northern BC. They unite, as the Kechika, to form a major tributary of the Liard River. Kechika River heads at Sifton Pass, latitude 58 degrees north, and flows north-westward in the Rocky Mountain Trench along the flank of the northernmost Rocky Mountains. Turnagain River heads on the west flank of the Cassiar Mountains and cuts across them in a general north-easterly direction to join the Kechika at Chee House, an abandoned trading post, about 70 miles from Liard River and 60 miles due south of the Yukon boundary. During 1939 topographic mapping of the Trench by the Department of Lands was completed from Finlay Forks to Sifton Pass, and in addition triangulation was almost completed from Sifton Pass to Lower Post on Liard River, a few miles south of the Yukon boundary. This work was continued, at a reduced rate, in 1940; the Trench was mapped as far northwest as Gataga and Terminus Mountains. Triangulation was completed to the Yukon boundary and extended up Turnagain River to within 25 miles of an existing network to the east of Dease Lake. Issue ID: B013Title: Supplementary Report on Bedwell RiverAuthor(s): Sargent, H.Series Name: BulletinPublication Year: 1941Scale: 1:70000NTS Map Sheet(s): 092FPlace Keyword(s): British Columbia, Bedwell RiverLat/Long (NSWE): 49.517, 49.333, -125.833, -125.5Theme Keyword(s): Geology, MiningDownload(s):
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Bulletin 13 gives a supplementary report on the Bedwell River area, Vancouver Island, BC. Fieldwork in 1939 and 1940, followed by office work including microscopic studies, is the basis for this bulletin, which deals with an area in the Alberni and Clayoquot Mining Divisions, Vancouver Island, BC. The geology of the area, as far as mapped in the two seasons, is represented on Figure 1, scale 1 inch to the mile, with topography in the northern part indicated by contours at 200 foot intervals. The topography is taken from part of Map No. 92F/5, released in 1939 by the BC Department of Lands, scale 2 inches to the mile, contour interval 100 feet. The base for the southern part of Figure 1 is the drainage pattern, prepared by the writer from airplane photographs borrowed from the Department of Lands. Issue ID: B014Title: Coal Analyses of British ColumbiaAuthor(s): Dickson, J.Series Name: BulletinPublication Year: 1941NTS Map Sheet(s): 082;083;092;093;094;102;103;104;114Place Keyword(s): British ColumbiaLat/Long (NSWE): 60, 48, -139, -114Theme Keyword(s): Geology, CoalDownload(s):
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Bulletin 14 gives a coal analyses of British Columbia. The tables give the analyses of BC coals and details of their adaptability for use in the pulverized form, their products under low temperature carbonatization treatment, and their indicated value by means of hydrogenation or liquification; the latter system converting a high percentage of the total weight of the treated coal into gasoline and other derivates of coal. Issue ID: B015Title: Hydraulic Mining MethodsAuthor(s): Holland, S.S.Series Name: BulletinPublication Year: 1942NTS Map Sheet(s): 082;083;092;093;094;102;103;104;114Place Keyword(s): British ColumbiaLat/Long (NSWE): 60, 48, -139, -114Theme Keyword(s): Geology, Mining, Hydraulic MiningDownload(s):
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Bulletin 15 discusses hydraulic mining methods in British Columbia. When placer gold was first discovered in BC, much of the gravel was mined by methods other than hydraulicking. Subsequently, however, with the working out of rich shallow gravel, extensive yardages of lower grade gravel were left which under favourable conditions were mined by hydraulicking. This type of mining produces the largest proportion of placer gold at present. Issue ID: B016Title: Dragline Dredging MethodsAuthor(s): Holland, S.S.Series Name: BulletinPublication Year: 1942NTS Map Sheet(s): 082;083;092;093;094;102;103;104;114Place Keyword(s): British ColumbiaLat/Long (NSWE): 60, 48, -139, -114Theme Keyword(s): Geology, Mining, Dragline DredgingDownload(s):
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Bulletin 16 discusses dragline dredging methods in British Columbia. A dragline dredge is a placer mining machine comprising two separate units (see Plates I and II). The gravel is dug by a standard dragline shovel which travels over the ground under its own power usually by means of caterpillar tracks (some of the large shovels are "walkers"). The bucket, having a capacity of from one to three cubic yards or more, is suspended from a structural steel boom 50 feet or more in length. The gravel is washed in a separate unit whose equipment is on a barge floating in a pond. For washing the gravel and separating the gold from it, the barge has a revolving screen (trommel) and riffle-tables similar to those used on bucket-line dredges. The dragline shovel digs away at the edge of the pond and casts the gravel into the hopper of the washing plant. The pond consequently advances as the digging proceeds and the barge follows by being warped along by winches with cables anchored on shore. The coarse tailings are discharged from a belt-conveyor, and sand-sluices fill the pond behind the dredge. Issue ID: B017Title: An Introduction to Metal Mining in British ColumbiaAuthor(s): Officers of the Department of MinesSeries Name: BulletinPublication Year: 1943Scale: 1:9000000NTS Map Sheet(s): 082;083;092;093;094;102;103;104;114Place Keyword(s): British ColumbiaLat/Long (NSWE): 60, 48, -139, -114Theme Keyword(s): Geology, Mining, Metal MiningDownload(s):
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Bulletin 17 gives an introduction to metal mining in British Columbia. During the ten year period ending in 1941, the annual value of the mineral production of BC averaged over $56,000,000. It is apparent that metal mining has been pre-eminent in BC's mineral production. Gold production, averaging more than $16,000,000. constituted slightly over a third of the value of the metallics and more than a fourth of the total value of all mineral products. However, because of expanding industrialization and growing population it is likely that production of structural and industrial materials will increase. Issue ID: B018Title: Specimens and Samples, Their Treatment and UseAuthor(s): Officers of the DepartmentSeries Name: BulletinPublication Year: 1944NTS Map Sheet(s): 082;083;092;093;094;102;103;104;114Place Keyword(s): British Columbia, VictoriaLat/Long (NSWE): 60, 48, -139, -114Theme Keyword(s): Geology, Samples, SpecimensDownload(s):
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Bulletin 18 discusses the treatment and use of specimens and samples in geology in British Columbia. This bulletin, written for the prospector, deals with the specimens and samples taken in the field and the treatment received in the Department of Mines laboratories in Victoria, BC. This bulletin brings out the differences between specimens and samples; the usefulness of each; how they should be taken, labeled, and shipped; and how specimens and some samples can be studied in the field. Issue ID: B019Title: The Tuya-Teslin Area, Northern British ColumbiaAuthor(s): Watson, K. DeP., Mathews, W.H.Series Name: BulletinPublication Year: 1944Scale: 1:253440NTS Map Sheet(s): 104O/3,4,5,6,12; 104N/8,9Place Keyword(s): British Columbia, Northern British Columbia, Tuya, TeslinLat/Long (NSWE): 58.917, 59.5, -132.167, -130.083Theme Keyword(s): GeologyDownload(s):
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Bulletin 19 discusses the geology of the Tuya-Teslin area of northern British Columbia. The Tuya-Teslin area, 1600 square miles in extent, is situated in the Stikine and Atlin Mining Divisions of northern BC, partly within the western margin of the Cassiar-Omineca Mountains. Although the area is accessible by several routes of travel, it is remote and transportation costs are very high. Because of the cold climate and the presence of snow in all but the summer months, prospecting can be carried out on satisfactorily for only about four months of the year. Issue ID: B020-02Title: Lode-Gold Deposits: Part I: Not published, Part II: Lode-gold Deposits, Southeastern B.C.Author(s): Mathews, W.H.Series Name: BulletinPublication Year: 1944NTS Map Sheet(s): 082F; 082G; 082J; 082KPlace Keyword(s): British Columbia, Southeastern British ColumbiaLat/Long (NSWE): 51, 49, -118, -114Theme Keyword(s): Geology, Lode-gold DepositsDownload(s):
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Bulletin 20-02 discusses lode-gold deposits in southeastern British Columbia. This is a six-part bulletin which covers separate areas. Part I - not published; Part II (20-02) - southeastern BC; Part III (20-03) - south-central BC; Part IV (20-04) - southwestern BC excluding Vancouver Island; Part V (20-05) - Vancouver Island; Part VI (20-06) - northeastern BC, Cariboo Cariboo and Hobson Creek areas. Issue ID: B020-03Title: Lode-Gold Deposits: Part III: Lode-gold Deposits, Central-southern British ColumbiaAuthor(s): Hedley, M.S., Watson, K. DeP.Series Name: BulletinPublication Year: 1945NTS Map Sheet(s): 082E; 082LPlace Keyword(s): British Columbia, Southcentral British ColumbiaLat/Long (NSWE): 51, 49, -120, -118Theme Keyword(s): Geology, Lode-gold DepositsDownload(s):
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Bulletin 20-03 discusses lode-gold deposits in south-central British Columbia. This is a six-part bulletin which covers separate areas. Part I - not published; Part II (20-02) - southeastern BC; Part III (20-03) - south-central BC; Part IV (20-04) - southwestern BC excluding Vancouver Island; Part V (20-05) - Vancouver Island; Part VI (20-06) - northeastern BC, Cariboo Cariboo and Hobson Creek areas. Issue ID: B020-04Title: Lode-Gold Deposits: Part IV: Lode-gold Deposits, Southwestern British Columbia (Exclusive of Vancouver Island)Author(s): Stevenson, J.S.Series Name: BulletinPublication Year: 1944NTS Map Sheet(s): 092;Place Keyword(s): British Columbia, Southwestern British ColumbiaLat/Long (NSWE): 52, 49, -128, -120Theme Keyword(s): Geology, Lode-gold DepositsDownload(s):
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Bulletin 20-04 discusses lode-gold deposits in southwestern British Columbia. This is a six-part bulletin which covers separate areas. Part I - not published; Part II (20-02) - southeastern BC; Part III (20-03) - south-central BC; Part IV (20-04) - southwestern BC excluding Vancouver Island; Part V (20-05) - Vancouver Island; Part VI (20-06) - northeastern BC, Cariboo Cariboo and Hobson Creek areas. Issue ID: B020-05Title: Lode-Gold Deposits: Part V: Lode-gold Deposits, Vancouver IslandAuthor(s): Stevenson, J.S.Series Name: BulletinPublication Year: 1944NTS Map Sheet(s): 092B,092C,092E,092F,092K,092L;102IPlace Keyword(s): British Columbia, Vancouver IslandLat/Long (NSWE): 48.25, 51, -128.4, -123Theme Keyword(s): Geology, Lode-gold DepositsDownload(s):
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Bulletin 20-05 discusses lode-gold deposits on Vancouver Island in British Columbia. This is a six-part bulletin which covers separate areas. Part I - not published; Part II (20-02) - southeastern BC; Part III (20-03) - south-central BC; Part IV (20-04) - southwestern BC excluding Vancouver Island; Part V (20-05) - Vancouver Island; Part VI (20-06) - northeastern BC, Cariboo BC, Cariboo and Hobson Creek areas. Issue ID: B020-06Title: Lode-Gold Deposits: Part VI: Lode-gold Deposits, Northeastern British Columbia and Cariboo and Hobson Creek AreasAuthor(s): Holland, S.S.Series Name: BulletinPublication Year: 1944NTS Map Sheet(s): 093; 094; 103; 104; 114Place Keyword(s): British Columbia, Northeastern British ColumbiaLat/Long (NSWE): 60, 52, -130, -120Theme Keyword(s): Geology, Lode-gold DepositsDownload(s):
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Bulletin 20-06 discusses lode-gold deposits in northeastern British Columbia. This is a six-part bulletin which covers separate areas. Part I - not published; Part II (20-02) - southeastern BC; Part III (20-03) - south-central BC; Part IV (20-04) - southwestern BC excluding Vancouver Island; Part V (20-05) - Vancouver Island; Part VI (20-06) - northeastern BC, Cariboo Cariboo and Hobson Creek areas. Issue ID: B021Title: Notes on Placer Mining in British ColumbiaAuthor(s): Officers of the DepartmentSeries Name: BulletinPublication Year: 1946Scale: 1:10000000NTS Map Sheet(s): 082;083;092;093;094;102;103;104;114Place Keyword(s): British ColumbiaLat/Long (NSWE): 60, 48, -139, -114Theme Keyword(s): Geology, Placer-miningDownload(s):
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Bulletin 21 discusses placer-mining in British Columbia. This bulletin contains general information about the geology, physiography, and climate of BC, the nature and formation of placer deposits, the history of placer mining, and the placer gold production of BC. It also contains brief notes dealing with placer gold areas in BC and information about prospecting for placer and describes methods of placer mining suitable for small-scale operations. Issue ID: B022Title: Geology of the Whitewater and Lucky Jim Mine AreasAuthor(s): Hedley, M.S.Series Name: BulletinPublication Year: 1947Scale: 1:9600NTS Map Sheet(s): 082F/03Place Keyword(s): British Columbia, Whitewater, Lucky Jim MineLat/Long (NSWE): 50.084, 50.016, -117.253, -117.095Theme Keyword(s): Geology, Bedrock GeologyDownload(s):
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Bulletin 22 describes the geology of the Whitewater and Lucky Jim Mine areas of southeastern British Columbia, Slocan District. This bulletin contains a structural analysis of the area between Retallack and Zincton and a detailed description of the Whitewater and Lucky Jim mines as well as six smaller properties. The area is in the slate belt, the basal part of the Slocan sedimentary series of Triassic age. The slaty rocks are cut by both granitic and lamprophyre dykes. The predominantly argillaceous rocks are in part slates but include phyllites and bands and single beds of limestone and quartzite. The regional strike is northwestward and the prevalent dip southwestward. The structure plunges westward west of Whitewater Creek and eastward east of that creek. Issue ID: B023Title: Calcareous Deposits of the Georgia Strait AreaAuthor(s): Mathews, W.H.Series Name: BulletinPublication Year: 1947Scale: 1:1000000NTS Map Sheet(s): 092F/1,2,3,4,5,6,7,8,9,10,11,12,13,14,15; 092B/5,6,11,12,13,14; 092C/8,9,10,11,14,15,16; 092G/3,4,5,6,11,12,13,14Place Keyword(s): British Columbia, Southwestern British Columbia, Georgia StraitLat/Long (NSWE): 50.5, 48, -126, -121.5Theme Keyword(s): Geology, Calcareous DepositsDownload(s):
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Bulletin 23 describes calcareous deposits of the Georgia Strait area of southwestern British Columbia. This bulletin includes reports of surveys of most of the known commercial or potentially calcareous deposits readily accessible to the industrial and agricultural areas of southwestern BC and northwestern Washington state. Limestone deposits on the west coast of Vancouver Island and on the inland passage north of the difficulty navigable waters of Seymour Narrows, Okisollo Channel, and Yuculta Rapids have not, however, been examined. Deposits more than 4 or 5 miles from tide-water have likewise been omitted from this study, except in the eastern part of the Fraser Valley and in the western part of the Cascade Range of Washington where adequate road or rail transportation is available. Unconsolidated calcareous deposits, marl, travertine, and shell, which are of some economic importance within this area, have been included in this study. Issue ID: B024Title: Geology and Coal Resources of the Carbon Creek-Mount Bickford Map AreaAuthor(s): Mathews, W.H.Series Name: BulletinPublication Year: 1947Scale: 1:19200NTS Map Sheet(s): 093O/15Place Keyword(s): British Columbia, Carbon Creek, Mount BickfordLat/Long (NSWE): 56.167, 55.533, -122.833, -122.25Theme Keyword(s): Geology, Coal ResourcesDownload(s):
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Bulletin 24 describes the geology and coal resources of the Carbon Creek-Mount Bickford map area. This report was written with the purpose of obtaining information on the coal resources of the Carbon Creek basin and of the area between this coalfield and the Hasler Creek field. Particular attention was paid to the structure and distribution of coal-bearing rocks and to any exposures of coal of possible commercial significance. Much of the area between the Carbon Creek and Hasler Creek coalfields proved to be underlain by a succession of marine sediments, hitherto virtually unknown, and a more or less detailed study of these rocks was made during the survey. Issue ID: B025Title: The Squaw Creek-Rainy Hollow AreaAuthor(s): Watson, K. DeP.Series Name: BulletinPublication Year: 1948Scale: 1:9600NTS Map Sheet(s): 114P/14Place Keyword(s): British Columbia, Squaw Creek, Rainy HollowLat/Long (NSWE): 60, 59.417, -137.167, -136.167Theme Keyword(s): Geology, Mineral occurrencesDownload(s):
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Bulletin 25 discusses the geology and mineral occurrences in the Squaw Creek-Rainy Hollow area in northern BC. The Squaw Creek-Rainy Hollow area is approximately 750 square miles in extent; lies in the Atlin Mining Division and is about 40 to 70 miles west to northwest of Skagway, Alaska. In 1943 access to the area was greatly improved by the construction through it of the Haines "Cut-off" Road, connecting Haines on Chilkoot Inlet with the Alaska Highway at a point 100 miles west of Whitehorse. Issue ID: B026Title: Report on the Stanley Area, Cariboo Mining DivisionAuthor(s): Holland, S.S.Series Name: BulletinPublication Year: 1948Scale: 1:19200NTS Map Sheet(s): 093H/4Place Keyword(s): British Columbia, Cariboo, Stanley AreaLat/Long (NSWE): 53.167, 53, -121.75, -121.583Theme Keyword(s): Geology, MiningDownload(s):
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Bulletin 26 gives a report on the Stanley area in the Cariboo Mining Division in central British Columbia. Near Stanley, two major creeks and their numerous tributaries have yielded placer gold estimated to have a value of $10,000,000 or more. The extraordinary richness of parts of the placer creeks, together with the known distribution of the placer deposits, initially suggested that there might be some demonstrable relationship, such as has been found in the Barkerville Gold Belt to the northeast, between the placer gold deposits, the known vein occurrences, the bedrock geology and the bedrock structure. Fieldwork was undertaken in the Stanley area in the hope that future prospecting and exploration might be benefited by the development of this idea. Issue ID: B027Title: Geology and Mineral Deposits of the Zeballos Mining Camp, British ColumbiaAuthor(s): Stevenson, J.S.Series Name: BulletinPublication Year: 1950Scale: 1:7200NTS Map Sheet(s): 092L/2Place Keyword(s): British Columbia, Northern Vancouver Island, ZeballosLat/Long (NSWE): 50.167, 49.917, -126.917, -126.667Theme Keyword(s): Geology, Mineral DepositsDownload(s):
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Bulletin 27 describes the geology and mineral deposits of the Zeballos mining camp of northern Vancouver Island in southwestern British Columbia. This bulletin presents data obtained from a detailed study of the areal geology of the surface and of the extensive mine workings in the Zeballos camp and presents conclusions concerning the localization of ore in the camp. Conclusions of a general nature are given in the general discussion of ore deposits, and those of a more detailed nature relating to properties are given in the individual descriptions of the properties. Issue ID: B028Title: Placer Gold Production of British ColumbiaAuthor(s): Holland, S.S.Series Name: BulletinPublication Year: 1950Scale: 1:1700000NTS Map Sheet(s): 082;083;092;093;094;102;103;104;114Place Keyword(s): British ColumbiaLat/Long (NSWE): 60, 48, -139, -114Theme Keyword(s): Geology, Mining, Placer-goldDownload(s):
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Bulletin 28 discusses placer gold production in British Columbia. This bulletin sets forth the recorded placer production for BC and for each placer stream in British Columbia. The production data and the accompanying notes are presented because of their interest and value to those who contemplate placer mining or prospecting for placer deposits in BC. Issue ID: B029Title: Geology and Ore Deposits of the Sandon Area, Slocan Camp, British ColumbiaAuthor(s): Hedley, M.S.Series Name: BulletinPublication Year: 1952Scale: 1:9600NTS Map Sheet(s): 082F/14Place Keyword(s): British Columbia, Sandon Area, Slocan Mining CampLat/Long (NSWE): 50.017, 49.942, -117.308, -117.205Theme Keyword(s): Geology, Ore Deposits, Bedrock GeologyDownload(s):
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Bulletin 29 covers the geology and ore deposits of the Sandon area, Slocan Mining Camp, British Columbia. Sandon has been a centre of production of silver-lead-zinc ores for sixty years. Mines in the area have contributed approximately half the entire output of silver and lead of the Slocan Mining Division. Mining activity has fluctuated widely with the condition of the metal market, and interest in the area has been renewed with the most recent rise in prices. The area is 2 miles north of the northern boundary of the Nelson batholith and is underlain by sediments of the Slocan series, intruded by dykes and small stocks. The Slocan series is of great thickness, only part of which is exposed within the Sandon area. In the area, tuff occurs in the upper part of the geologic column. The sediments are mainly argillites, quartzites, and limestones, or intimate admixtures of these rock types. For the most part the sediments are silty, estuarine deposits with rapid alternations in character; some are rhythmically banded. Cross bedding and evidence of turbulent deposition are common in many parts of the geologic column. The rocks are locally slaty. Intrusive bodies are for the most part sill-like and some stocks are elongated with the structure. The general rock type is a quartz diorite, with a highly variable texture. Lamprophyres of the same general composition, but relatively rich in biotite, are common and grade into the quartz diorites. Metamorphism of contact type is not marked. The principal product, which occurs locally, is a brownish rock produced by the development of biotite in some of the argillite. Silicification is widespread, affecting the rocks patchily and chiefly in the southern and western parts of the area. The rock most affected is limestone, which may be converted to a product very similar in appearance to quartzite. Silicification is not related to the lodes but to the general process of intrusion, and is only locally related to specific dykes or sills. The structure is of a type not heretofore described. It is more Alpine than has previously been recognized in British Columbia and has far-reaching regional implications, although the implications are not considered in this bulletin. Certain details of the structure are believed to be closely related to the emplacement of the Nelson batholith but, as time has prevented study of the batholith itself, the relationship has not been proved. The folding of the Slocan sediments is of recumbent type, the individual folds having axial planes with little or no dip and axial lines with little or no plunge. The entire assemblage is involved in one huge recumbent fold, striking northwesterly, which is open or concave to the southwest. This is termed the Slocan fold, and includes many smaller folds of various sizes and degrees of complexity. The large complex Slocan fold is wrapped round the northeastern end of the Nelson batholith, east of the Sandon area. South of the area, and also east of it, the rocks deviate markedly from the northwesterly strike along the general east-west course of the batholith. The folded rocks swing through a right angle in strike in a huge crumple that is termed down buckling, and ultimately meet the batholith tangentially. This folding of folded rocks is a modification of the Slocan fold structure, and there is no evidence that it was produced by a second period or separate generation of orogeny; rather, it is believed to have resulted from a progressive change in stress application during late stages of the Slocan folding. A further modification of the Slocan fold is a broad cross-warp that extends across the entire structure from the vicinity of Idaho Peak to the vicinity of Retallack. The cross-warp is anticlinal, with low regional plunges to northwest and southeast on either side of it. It extends through the main productive belt of the Slocan mining camp. Drag folds of all sizes are developed in characteristic relation to the large folds. The geometry of recumbent folding is such that all upper beds have moved relatively downward, the reverse of the movement observed in upright folds. Cleavage is developed locally, and in the main Whitewater and Payne slate belts it is produced at least in part by excessive interbed slippage which amounts to shearing. Axial-plane cleavage and shear cleavage cannot be differentiated except by structural reference, and some cleavage is of dual origin. There are many faults, all of which are related to the structural complex and the forces that produced it. Two general classes of faults are recognized: tangential and crosscutting. The tangential faults are parallel in strike to the formation and commonly are bedded. The crosscutting faults cross the regional strike at large angles. The two classes are closely related in time of origin. All faults appear to be normal, and most have a lateral as well as a normal component of movement. The displacement on the tangential faults is a consequence of the folding and bears the same relative movement as the interbed slippage of which the faults are, in a sense, an extreme expression. The crosscutting faults are tear faults with a component of underthrusting. The lodes are almost without exception crosscutting faults, of small and large size. In the Sandon area they cut across the structure but, immediately to the south in the valley of Silverton Creek, they are tangential to the down-buckled strata. It is believed that the larger faults of this class originated parallel with the down-buckled rocks as an extreme of this late phase of folding and in partial relief of the stresses that produced it. The larger faults or lodes stemmed from a focal area in lower Silverton Creek with steep dips to the northwest, rolled with the down buckle to a southeasterly dip and, in the zone of maximum curvature, continued across the northwesterly striking rocks. Most of the lodes are complex, inasmuch as they represent zones of rupture with more than one locus of movement. They are to a considerable extent influenced by the structure they cross, in both strike and dip. They are zones of both fracture and shear. Orebodies are related to zones of fracture rather than of shearing and as a rule occur in places of decreased confining pressure. The factors that may be said to have controlled ore deposition are many, and most orebodies were formed as a result of the conjunction of a number of favourable circumstances. Metal distribution within the area and within individual lodes is of great importance. Factors which might limit the occurrence of ore at depth and which might produce lateral or vertical segregation are vital to considerations of development. No marked pattern of zoning or segregation is recognized, except for the fact that the margins of orebodies are relatively richer in zinc than in lead. The control of ore deposition is structural, and temperature and load pressure due to depth are of minor importance. The most important single factor was probably that of local confining pressure in a structurally complex environment.

Issue ID: B030Title: Clay and Shale Deposits in British ColumbiaAuthor(s): McCammon, J.W., Cummings, J.M.Series Name: BulletinPublication Year: 1953NTS Map Sheet(s): 083; 092; 093; 094; 102;Place Keyword(s): British ColumbiaLat/Long (NSWE): 55, 48, -133, -114Theme Keyword(s): Geology, Clay Deposits, Shale DepositsDownload(s):
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Bulletin 30 discusses clay and shale deposits in British Columbia. This report is based on field examinations by the writers and on published data from several sources. The locations of clay deposits on which specific information is available are shown on the accompanying key map, and pertinent data are presented in tabular form. Issue ID: B031Title: Geology of the Sheep Creek CampAuthor(s): Mathews, W.H.Series Name: BulletinPublication Year: 1953Scale: 1:18200NTS Map Sheet(s): 082F/3Place Keyword(s): British Columbia, Nelson Mining Division, Sheep CreekLat/Long (NSWE): 49.192, 49.1, -117.133, -117.067Theme Keyword(s): Geology, Quartz Veins, Bedrock GeologyDownload(s):
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Bulletin 31 describes the geology of the Sheep Creek camp, which has produced almost two-thirds of the lode gold credited to the Nelson Mining Division. Although the camp is currently non-productive, it ranks as the sixth camp in British Columbia in terms of total lode gold produced to the end of 1951. The production of the camp has come from quartz veins that to the end of 1951 have yielded a total of 736,000 ounces of gold, 365,000 ounces of silver, 377,000 pounds of lead, and 312,000 pounds of zinc from 1,720,000 tons of ore. The production recorded year by year for the camp is set forth in Table VI on page 51. The accumulated gross value of the gold amounts to more than $24,000,000. Dividends paid from the profits of mines in the camp, mainly in the period 1935 to 1943, have amounted to $5,400,000. Two main periods are recognizable in the productive history of the camp. The first began in 1899, reached its peak immediately before World War I, and ended in 1916. The second began in 1928 when a new vein on a new property, the Reno, was brought into production. In the next few years conditions became very favourable for mining gold, and the former producers, the Kootenay Belle and the Queen (Sheep Creek Gold Mining Limited), and a new producer, the Gold Belt, were equipped with modern mills. Production reached its peak in 1937 and was maintained at more than 135,000 tons a year until 1942. Thereafter production was mainly from the property of Sheep Creek Gold Mines Limited, which was shut down in 1951 after seventeen years of production. The camp is now inactive except for minor leasing-type operations. Both main periods ended in times that were unfavourable for gold mining, the mines being closed after ore that had been developed under more favourable conditions had been entirely or almost entirely exhausted. The output of the camp has come almost entirely from oreshoots in quartz veins cutting folded quartzites that are part of a thick succession of Lower Cambrian and Precambrian (?) sedimentary rocks. A very small part of the total gold production has been recovered from narrow high-grade veins in limestone. The sediments are intruded by several stock-like granitic bodies, by an elongate swarm of quartz porphyry sills, and by numerous lamprophyre dykes. The granitic bodies are believed to be older than the ore and most of the lamprophyres to be younger. The quartz veins strike north-easterly across the axes of the folded sediments and generally dip steeply. The Sheep Creek gold camp is within a district that contains numerous mining camps. Adjoining and near-by areas are important sources of tungsten and of silver, lead, and zinc. Several camps have contributed lode gold in varying quantities. Properties in the several camps of the district have yielded up to 120,000 ounces of gold each. The occurrences of gold in the district are dealt with briefly in Bulletin 20. Part 1, Lode Gold Deposits, southeastern British Columbia, by W. H. Mathews, British Columbia Department of Mines, 1944. Interest in lead-zinc replacement deposits in areas adjoining the Sheep Creek camp has increased greatly since the field work for this bulletin was undertaken. Similar lead-zinc deposits have not been discovered within the boundaries of the area treated in the present report. The sedimentary rocks in the Sheep Creek camp had been highly folded prior to the intrusion of the igneous rocks, and two tight northerly trending anticlines with an intervening syncline make up the major structures of the camp. Faults belonging to four sets cut across the folded structures (1) A group of north-easterly trending, south-easterly dipping, right-hand strike-slip faults with a small normal component of movement contain all the productive veins, (2) a very few northwesterly trending left-hand strike-slip faults, (3) several northerly trending normal faults; and (4) flat faults along which the hanging walls have been thrust westward with respect to the footwalls. The veins occupy the north-easterly trending faults and consist of quartz with minor amounts of pyrite and still smaller amounts of pyrrhotite, chalcopyrite, galena, sphalerite, and gold. The quartz in the veins is probably derived in large part by recrystallization of quartzite walls. Visible gold is rare. The ore is almost without exception confined to parts of the fault zones in which one or both walls are made up of quartzite, and the orebodies are, therefore, found where the veins intersect certain stratigraphic units, notably the quartzite units referred to as Upper Nugget and Upper Navada. The Motherlode member, also quartzitic, is for some unexplained reason almost completely lacking in orebodies. The Reno formation, predominantly argillaceous, is almost devoid of ore except in the Reno mine, where the rocks have been conspicuously metamorphosed. In the veins, the ore occurs in shoots; the other parts of the veins are either too thin, or too low in grade, or both, to justify stoping. In any one vein the profitable oreshoots have been found within a vertical range of not more than 1,600 feet. This vertical range for successive veins lies within a depth zone that slopes regularly from the northern to the southern end of the camp. At the northern end it is 5,500 to 7,000 feet above sea level and at the southern end of the camp, 4 miles distant, it lies entirely below the 3,000 foot level. Above this zone the vein fracture may persist, but at least within the quartzites, the veins are too narrow to contain orebodies. At the bottom of the zone, the veins persist and may be even wider than within the zone. A few veins have been explored at depths of not more than 250 feet below the bottoms of the deepest stopes. Although these veins are of good width, the parts rich enough in gold to constitute oreshoots were too small and too widely scattered to encourage further exploration and development. Within the favourable wallrocks and within the favourable depth zone, those parts of the veins striking most nearly east are more likely to contain ore. Displacement on vein fractures is variable, and in any one vein, other things being equal, the width increases with the amount of displacement. However, the vein filling is not necessarily wide in vein fractures on which displacement has been large, nor narrow in those on which displacement has been small. The grade of vein matter is exceedingly variable, patches of high-grade ore being distributed apparently at random within a vein. The area of such a patch measured in the plane of the vein is rarely more than a few hundred square feet and commonly is much less. In general patches of ore of which the grade exceeds 5 ounces of gold per ton are larger and more common in the upper part of the productive zone than at greater depths.

Issue ID: B032Title: Geology and Mineral Deposits of the Shulaps Range, Southwestern British ColumbiaAuthor(s): Leech, G.B.Series Name: BulletinPublication Year: 1953Scale: 1:64375NTS Map Sheet(s): 092J/15,16; 092I/1,2Place Keyword(s): British Columbia, Southcentral British Columbia, Shulaps RangeLat/Long (NSWE): 51.131, 50.875, -122.7, -122.25Theme Keyword(s): Geology, Mineral Deposits, Bedrock GeologyDownload(s):
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Bulletin 32 describes the geology and mineral deposits of the Shulaps Range on the northeast flank of the Coast Mountains in south-central British Columbia. This study focused on the ultramafic rocks in the core of the Shulaps Range and only a narrow strip of the surrounding rocks was mapped. Most of the Shulaps Creek drainage basin and much of the west flank of the Range are underlain by pre-Upper Triassic argillite, chert and greenstone with local limestone layers. Their age is uncertain. Along the west flank and north of Liza Lake, argillaceous and tuffaceous sediments, impure sandstones and conglomerates with lesser amounts of dark cherty strata and limestone of the Hurley Group predominate. Chert pebble and cobble conglomerates and associated rocks of the Taylor Group underlie the area of Quartz Mountain and northward to Noaxe Creek. A greenstone-gabbro complex underlie an area southeast of Liza Lake. The Yalakom fault zone, along the eastern side of the Shulaps Range, marks the eastern limit of the ultramafic complex. East of the fault zone, greywacke, argillite, siltstone, grit and conglomerate of Triassic or earlier age and Lowe Cretaceous greywacke, shale, conglomerate, limestone and chert. The Shulaps complex contains gabbro, diopside pyroxenite, and variably fresh to serpentinized or carbonatized ultrabasic rocks, dominantly peridotites but including dunite and harzburgite. In the most important mineral deposit type, gold occurs in quartz veins. Underground development has been performed on both gold and mercury occurrences in the area. Other targets are manganese, chromium and magnesite. The gold bearing quartz fissure veins cut dioritic porphyries that intrude peridotite. Mercury mineralization, described in Bulletin 5, occurs in andesitic lavas interbedded with volcanic breccias within the Yalakom fault zone. The rocks are highly fractured and locally ankeritized. It is laced with stringers containing dolomitic carbonate and quartz. Cinnabar occurs in part of the intensely ankeritized zone as stringers, blebs and disseminated grains and fracture coatings. Note: a more recent discussion of the geology is found in Bulletin 100.

Issue ID: B033Title: Geology of the Crowsnest Coal Basin with Special Reference to the Fernie AreaAuthor(s): Newmarch, C.B.Series Name: BulletinPublication Year: 1953Scale: 1:19250NTS Map Sheet(s): 082G/6,7,10,11Place Keyword(s): British Columbia, Southeastern British Columbia, Fernie, Crowsnest Coal BasinLat/Long (NSWE): 49.513, 49.467, -115.067, -114.933Theme Keyword(s): Geology, Coal Measures, Bedrock GeologyDownload(s):
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Bulletin 33 covers the geology and coal measures of the Crowsnest coal basin near Fernie in southeastern British Columbia. The report describes the Michel strip mines and proposes a method to correlate coal seams by using spectrochemical analyses of ash from coal samples. The �Fernie Coal area�, approximately 31 square miles in area, was mapped at scale 1 inch to 800 feet. Strata ranging in age from Jurassic to recent are exposed in the Crowsnest Coal basin but only the Mesozoic section is coal bearing and was studied in detail. The Fernie Formation is mainly gray to black shale with some fine sandy layers. The shales are variably calcareous and a sandy calcareous layer with numerous belemnites provides a useful marker within the formation. The unit thickens westward and is about 3000 feet thick in the Fernie area. Its age spans most of the Jurassic period. The Kootenay Formation is the coal-bearing unit. It is Upper Jurassic or Lower Cretaceous in age. It is characterized by dark sandstones, grey and black shales, several beds of conglomerate and up to 13 coal seams of commercial thickness. The best and most persistent marker is the 45 to 60-foot thick basal Kootenay sandstone that marks the lower limit of the coal measures. The Kootenay Formation grades into the overlying conglomeratic Elk Formation. The contact has been placed arbitrarily at the base of the conglomerate that overlies the number �B� coal seam. The Elk Formation consists of cherty conglomerates, gritty sandstones and grey to black shales. The Lower Cretaceous Blairmore Formation includes all the indurated conglomerates, sandstones and shales that overlie the Elk Formation. The predominant structural trend of the region varies from north-northwest in the south, to north in the area north of Fernie. Most fold axes vary from vertical to west dipping. Most faults dip west and have west-side up movement. Near Michel Head and west of Fernie, anticlines are overturned toward the east. The area is characterized by many high angle, west dipping thrust faults and many folded faults. A broad open fold that plunges 7 degrees northward underlies the Crowsnest Coal basin. However, in detail, the picture is more complex. The eastern edge of the basin is marked by the north trending Erickson fault. Mines in the Coal Creek area produce medium volatile bituminous coking coal. Former underground mines in the Morrissey area were closed due to problems with gas outbursts. The potential for surface mineable coal was examined. In the Michel area, exploration was underway at the strip mine on Erickson ridge. Coal is thickened near a reverse fault along the core of an anticline to the west and a syncline to the east. Coal is of coking quality. On Baldie ridge, however, mining produced non-coking thermal coal. Other commodities of potential economic interest in the area include phosphate, limestone, building stone, clay and shale, gravel and sand, and oil and gas. Two new methods to correlate coal were investigated. The first involved measurements of radioactivity of coal samples. A direct correlation with ash content was found. The second involved spectrographic analysis of coal seams. Various seams from the Michel colliery were sampled to test the concept. The most useful elements for correlation were sodium, barium, silicon, vanadium and magnesium. The approach has value in a local area but more testing is needed to assess its wider applicability.

Issue ID: B034Title: Geology of the Yanks Peak-Round Top Mountain Area, Cariboo District, British ColumbiaAuthor(s): Holland, S.S.Series Name: BulletinPublication Year: 1954Scale: 1:14350NTS Map Sheet(s): 093A/14Place Keyword(s): British Columbia, Cariboo District, Yanks Peak, Roundtop MountainLat/Long (NSWE): 52.897, 52.785, -121.453, -121.257Theme Keyword(s): Geology, Gold, Bedrock GeologyDownload(s):
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Bulletin 34 discusses the geology of the Yanks Peak-Roundtop Mountain area, Cariboo District, British Columbia. Characteristic features are: 1. The Yanks Peak-Roundtop Mountain area lies at the head of several well-known placer creeks and contains numerous gold-bearing quartz veins. 2. The recorded gold production of the immediately surrounding district is 69,237 ounces of crude placer gold and 5,204 fine ounces of lode gold. 3. The area is underlain by a succession of schistose sedimentary rocks of late Precambrian and (or) Cambrian age known as the Cariboo group. 4. Formerly the Cariboo group was subdivided into the Richfield, Barkerville, and Pleasant Valley formations. These formational names have been abandoned, and the rocks of the Cariboo group now are divided into the Cunningham limestone, Yankee Belle, Yanks Peak quartzite, Midas, and Snowshoe formations. 5. The few intrusive rocks are dykes of diabase, diorite, rhyolite porphyry, and lamprophyre. 6. The rocks of the area are involved in a major syncline flanked by two overturned anticlines and in detail are intricately folded. The original structural interpretation of Bowman and Uglow of a broad, simple anticlinorium involving huge thicknesses of rock must be abandoned. 7. The rocks are cut by northerly and north-easterly striking normal faults. Some faults have a lateral displacement of 800 feet, and in most instances the eastern block has dropped downward. 8. The area contains several centres of gold mineralization. 9. The localization of veins is dominantly the result of structural rather than stratigraphic factors. 10. The numerous quartz veins are grouped according to their strike into: - (a) Northerly striking veins occupying faults or shears. (b) North-easterly striking veins occupying tension fractures that may have formed originally as extension joints but which were reopened subsequently by tensional forces resulting from movement along the northerly faults. (c) Easterly striking veins occupying shear fractures related to the northerly striking faults. 11. Most quartz veins are associated in one way or another with northerly striking faults; either they occupy the fault, or they occupy north-easterly or easterly striking fractures that are related to it. The three vein directions represent fracture directions that are genetically related, being two complementary directions of shear and the associated direction of tension. 12. The quartz mineralization of the three vein directions was essentially contemporaneous. 13. Ankerite is a common gangue mineral of the quartz veins. Sulphide mineralization is generally sparse and consists of pyrite, galena, and sphalerite. Scheelite, arsenopyrite, and tetrahedrite have been found. 14. Gold is associated with pyrite, and in outcrops becomes visible when the pyrite has been leached. 15. The gold mineralization is considered to be post-Jurassic in age. 16. The most productive placers were on Keithley, Little Snowshoe, Cunningham, and Harvey Creeks just beyond the limits of the area. 17. The erosion of veins within the area is thought to have contributed placer gold to local accumulations, but the chief placer stretches derived their gold from bedrock sources outside the area and closer to the placers. 18. In recent years several new mineral discoveries have been made, but future lode prospecting must be largely devoted to the finding of veins that are covered with overburden. The association of gold-bearing veins with northerly striking faults should provide a basis for close prospecting. 19. It is unlikely that placer prospecting will result in the finding of placer deposits better than small unworked remnants suitable for individual sniping or small-scale operation.

Issue ID: B035Title: Geology of the Stanford Range of the Rocky Mountains, East Kootenay District, British ColumbiaAuthor(s): Henderson, G.G.L.Series Name: BulletinPublication Year: 1954Scale: 1:64375NTS Map Sheet(s): 082J/4,5,12; 082K/1E�,8E�,9E�Place Keyword(s): British Columbia, Kootenay District, Stanford RangeLat/Long (NSWE): 50.626, 50.139, -116.047, -115.602Theme Keyword(s): Geology, Bedrock GeologyDownload(s):
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Bulletin 35 covers the geology of the Stanford Range of the Rocky Mountains, Kootenay District, British Columbia. Features that characterize the area are: 1. The Stanford Range is one of the western ranges of the Rocky Mountains lying between the Rocky Mountain trench and the Kootenay River, about midway between Cranbrook and Golden. 2. The range has a maximum relief of over 6,000 feet and an average local relief of about 3,000 feet. Although it contains no glacial erosion features, the presence of erratics at high elevations indicates that at one time at least it was covered with ice. 3. All the rocks in the Stanford Range are sedimentary. They range in age from Late Precambrian to Middle Devonian and consist mostly of limestones, dolomites, argillaceous limestones, and limy shales. The remainder of the section, about 30 per cent, is made up of black shales, quartzites, argillites, slates, conglomerates, and rock gypsum. 4. The industrial mineral gypsum occurs in a thick section interbedded with occasional calcareous members, and the whole comprises a new formation for which the name Burnais is proposed. The age of the Burnais formation is between Middle Silurian and Middle Devonian. 5. A unique metamorphic rock, resembling a phyllite, is developed within a mile-wide zone of shearing that follows the Kootenay and White Rivers on the northeastern side of the map area. This shearing is associated with a regional longitudinal fault named the White River break, and remains within the limits of McKay group strata throughout its exposed length. 6. The Stanford Range is divided into three fault blocks by two longitudinal faults, the Redwall and Stanford, which extend throughout the length of the range. The fault blocks are named the eastern, central, and western, and each contains distinct types of structures. 7. The Eastern fault block, between the Kootenay River (White River break) and the Stanford fault, contains the lower limb of a southwesterly overturned, almost recumbent fold, which is locally contorted into large nappe-like drag folds. 8. The Central fault block, between the Stanford and Redwall faults, is characterized by upright, inclined, and overturned anticlines which arc separated from each other by faulted synclines. 9. The Western fault block, between the Redwall fault and the Rocky Mountain trench, contains complex, longitudinal trending folds that are intricately dissected by a network of faults. In addition, a large area is underlain by obliquely trending, imbricate thrust structures. These are indicative of shortening of the range along an axis almost parallel with its trend. 10. The Redwall and Stanford faults, as well as many of the other faults in the range, are characterized by wide red- or brown-coloured breccia zones. The movement on the Redwall fault is large and is mostly strike-slip. Strike-slip movement may also have occurred on the Stanford fault, but, unlike the Redwall fault, this cannot be proved. 11. Metamorphism in the Stanford Range is generally restricted to areas of tight folding and the border zones of major faults. With the exception of the intense alteration of McKay group rocks along the White River break, the effects of metamorphism are limited to those usually attributed to low-grade dynamic metamorphism. 12. The Rocky Mountains at this latitude are composed of four separate structural sub-provinces for which the following names are proposed: Foothills sub-province, Front Ranges sub-province, Main Ranges sub-province, and Western Ranges sub-province. Each of these contains distinct structure, stratigraphy, and topography. 13. The Stanford Range forms part of the Western Ranges sub-province, which is distinct from the other sub-provinces inasmuch as the folds are overturned toward the southwest instead of the northeast, the structures are a great deal more complex, and the structural trend is about 10 to 15 degrees oblique to the trend of the Rocky Mountains and the Rocky Mountain trench. 14. The Western Ranges sub-province is separated from the Main Ranges sub-province by a major longitudinal fault zone that extends from Blaeberry southeastward along the Beaverfoot, Kootenay, and White Rivers for at least 120 miles. The name White River break is proposed for this fault. The sub-province is bounded on the southwest by the Rocky Mountain trench. 15. The White River break separates the southwesterly overturned structures of the Western Ranges sub-province from flat to gently folded strata of the Main Ranges sub-province. It also marks a distinct break in the stratigraphic continuity of the western Rocky Mountains. 16. The White River break appears to dip southwest. It is interpreted as a thrust fault of younger age than the southwesterly overturned structures of the Western Ranges sub-province, which are believed to have been formed by a major wedge uplift of the Main Ranges sub-province. 17. Gypsum of commercial grade occurs in enormous quantities within the map area, particularly along Windermere Creek and the Kootenay River. It is in the form of sedimentary rock gypsum, and the evidence of primary origin is conclusive. 18. A preliminary graph is presented showing the stability relationships of gypsum and anhydrite as functions of temperature and pressure. Under average thermal conditions, gypsum appears to be metastable at depths below 3,500 feet, and in the presence of a water solution should be converted to anhydrite. In the presence of a salt solution, transformation should occur at shallower depths. 19. The thickness of the known strata overlying the primary gypsum suggests that there was no post-Middle Devonian deposition in this part of the Western Rocky Mountains.

Issue ID: B036Title: Coal Reserves of the Hasler Creek-Pine River Area, British ColumbiaAuthor(s): McKechnie, N.D.Series Name: BulletinPublication Year: 1955NTS Map Sheet(s): 093;Place Keyword(s): British Columbia, Hasler Creek, Pine RiverLat/Long (NSWE): 56, 55.5, -122.5, -122.417Theme Keyword(s): Geology, Coal ReservesDownload(s):
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Bulletin 36 describes the coal reserves of the Hasler Creek-Pine River area of British Columbia. This report describes the results of an exploration, by means of geological mapping, trenching, and diamond drilling, of coal deposits in the Peace River District about 100 miles west of the village of Dawson Creek. The coalfield extends from about 1 mile north of the Pine River to some 18 miles southeastward, a little beyond Hasler Creek. The object of the work was to provide an estimate of the tonnage of mineable coal that might be available contiguous to a proposed route of the Pacific Great Eastern Railroad into the Peace River District. Issue ID: B037Title: Geology of the Cowichan Lake Area, Vancouver Island, British ColumbiaAuthor(s): Fyles, J.T.Series Name: BulletinPublication Year: 1955Scale: 1:63360NTS Map Sheet(s): 092C/16Place Keyword(s): British Columbia, Southern Vancouver Island, Cowichan LakeLat/Long (NSWE): 49.12, 48.77, -124.65, -124Theme Keyword(s): Geology, Bedrock GeologyDownload(s):
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Bulletin 37 describes the geology of the Cowichan Lake area of British Columbia. The area referred to in this report as the Cowichan Lake area includes about 280 square miles of mountainous country on southern Vancouver Island lying mainly north and northwest of Cowichan Lake. Fault-line scarps and fault-controlled valleys are the most prominent physiographic features of the region. The north side of Cowichan Lake is a fault-line scarp; and Rift Creek, the west fork of Cottonwood Creek, and the upper part of South Nanaimo River flow in fault controlled valleys. The continental ice-sheet covered the entire region. The ice appears to have moved southward. The oldest rocks in the area belong to the Sicker group. They include thin-bedded, cherty, argillaceous, and feldspathic tufts; limestones; coarse and fine breccias; and minor intercalated amygdaloidal basalt flows. Crinoidal limestones at the top of the Sicker group contain Lower Permian fossils. The Sicker group is conformably or disconformably overlain by the Vancouver group. The lower part of the Vancouver group is made up of a thick sequence of massive, pillow, and amygdaloidal basalt flows and related sills, dykes, and irregular bodies of diabase. The intrusive masses are equivalent to the Sicker gabbro-diorite-porphyrite described by Clapp. The upper part of the Vancouver group includes the Sutton limestone, which contains Upper Triassic fossils, and an overlying sequence of clastic sediments. Rocks of the Sicker and Vancouver groups are highly deformed into northwesterly trending folds, many of which are overturned with both limbs dipping southwestward. Plutons of Saanich granodiorite belonging to the Coast intrusions cut the Sicker and Vancouver groups. They are dominantly quartz diorite and granodiorite, but a roof facies of granite and aplogranite occurs near the top of Mount Buttle. The plutons are mainly steeply dipping, elongate bodies that are less than 2 miles wide and several miles long. In cross section they cut across structures in the pre-granitic rocks; in plan, long axes are parallel to fold axes in the older rocks. Close to plutons of granodiorite the pre-granitic basaltic rocks have been metamorphosed, exhibit granoblastic textures, and contain minerals characteristic of the granodiorite. Farther from granodiorite plutons, pre-granitic rocks have undergone a low grade of regional metamorphism that appears to be spatially related to the granodiorite. Erosional remnants of Upper Cretaceous detrital sediments belonging to the Nanaimo group unconformably overlie the Saanich granodiorite and pre-granitic rocks. The Nanaimo group has been gently folded and displaced by steeply dipping faults. Most of the movement on the faults appears to be parallel to the dip, and the dip slip on several is more than 1,000 feet. Small irregular masses of gabbro, possibly of Tertiary age, intrude rocks of the Sicker group and The Saanich granodiorite. Copper has been shipped from the Blue Grouse property on the south side of Cowichan Lake, and manganese from the Hill 60 deposit 4 miles east of Lake Cowichan. Copper occurs in chalcopyrite-skarn deposits at the Blue Grouse property and on the divide between Widow Creek and Chemainus River. Quartz veins near bodies of granodiorite commonly contain molybdenite. On the Allies property on Mount Buttle, quartz-molybdenite veins have been prospected by trenches and open pits. Shear zones in massive volcanics of the Vancouver group on El Capitan and the northeast slopes of Mount Service contain sulphides and gold. They have been explored by underground workings on the Silver Leaf and El Capitan properties. At many places cherty rocks of the Sicker group contain manganese silicates, mainly rhodonite and manganese garnets. Within a few feet of the surface the silicates have been oxidized, and siliceous manganese oxides have been mined at the Hill 60 deposit.

Issue ID: B038Title: Geology of the Antler Creek Area, British ColumbiaAuthor(s): Sutherland-Brown, A.Series Name: BulletinPublication Year: 1957Scale: 1:32000NTS Map Sheet(s): 093A/13,14; 093H/3,4Place Keyword(s): British Columbia, Cariboo District, Antler DistrictLat/Long (NSWE): 53.157, 52.919, -121.627, -121.29Theme Keyword(s): Geology, Bedrock GeologyDownload(s):
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Bulletin 38 describes the geology of the Antler Creek area in the Cariboo District of east-central British Columbia about halfway between the northwesterly and southerly flowing parts of the Fraser River. The area adjoins the Roundtop Mountain-Yanks Peak area on the north. The area is in a region transitional between the Interior Plateau to the west and the Cariboo Mountains to the east. A mountain ice-sheet covered the entire area at least once and, although the ice must have been almost static, some movement to the southwest occurred. The geology is complex and there have been a number of interpretations of the structure and stratigraphy of the Cariboo group. The Cariboo group underlies the greater part of the area. Characteristic rocks of the group are phyllite, micaceous quartzite, and limestone. The group is divided into five formations, which are, from oldest to youngest, the Cunningham limestone, Yankee Belle formation of brown phyllite and lesser amounts of fine quartzite, Yanks Peak quartzite, Midas formation of black phyllite and metasiltstone, and the Snowshoe formation of micaceous quartzite, phyllite, and lesser amounts of limestone. No fossils have been found in the group within the area, but just beyond it an Early Cambrian fauna has been collected from the Cunningham limestone. The Cariboo group is overlain with unconformity and great structural discordance by the Slide Mountain group of Carboniferous age. The Slide Mountain group is composed dominantly of conglomerate, argillite, chert, and diabasic pillow laws and flow breccias. The group is divided into two formations-the basal Guyet formation, composed of conglomerate, flow rocks, argillite, and minor crinoidal limestone, and the Antler formation, composed of chert, argillite, and pillow lavas. The chert of the Antler formation appears to have originated by more than one process and the silica originated from more than one source. Small acid dykes, the Proserpine dykes, cut the Cariboo group but not the Slide Mountain group. Basic intrusive rocks, the Mount Murray intrusions, cut both groups but are rare in the Cariboo group except adjacent to the Slide Mountain group. Sills in the latter group are composed of spilitic diabase, which is related spatially, texturally, and chemically, and hence probably also in age and origin, to the flow rocks of the group. A great difference in manner and intensity of folding of Cariboo and Slide Mountain groups exists. The Cariboo group has been closely compressed into northwesterly trending complex folds, which are overturned toward the southwest in the Antler Creek area. A regional secondary foliation is developed in the Cariboo group essentially parallel with axial planes. Component grains have been flattened parallel to the schistosity. Fold structures of the Wells mining camp are asymmetrical and complex and cannot be mapped without interpretation. In contrast, the Slide Mountain group has been folded into simple, upright, and open structures parallel to folds in the Cariboo group. The rocks are neither schistose nor greatly deformed. The Antler Creek area is an important source of lode and placer gold. The Cariboo Gold Quartz and Island Mountain mines at Wells have produced more than 32 million dollars in bullion from 1932 to the end of 1953. Placer mining has probably produced an equivalent amount, although only 15 million dollars is officially recorded because accurate statistics were not kept until thirteen years after the original gold rush of 1861. Current yearly lode-gold production (1954) has a value greater than 1.5 million dollars, whereas current placer-gold production ranges between one-tenth and one-fiftieth of this figure. This report is limited to lode. Placer was not studied because Bowman�s maps of the placer creeks (1895) and Johnston and Uglow�s report are accurate and thorough, and little could be added to them. The lode deposits of the Antler Creek area are gold-bearing pyritic quartz veins and bedded replacements. These two types of orebodies are related in origin. Lodes have been found only within the Cariboo group. Replacement deposits have been found to date only in the Wells camp, and only at limited horizons and localities. Most deposits are in the Baker limestone beds of the Snowshoe formation, between the Rainbow fault and the northwest boundary of the Island Mountain property. Other thin limestone members intercalated in the Snowshoe formation are common, but have not yet been very productive. Some rare bedded orebodies replace argillaceous rocks. Quartz veins are common and are widely distributed in the Cariboo group. Although some veins are very large, most are small and in some places are closely spaced. In general the sulphide content is low, but in certain areas they contain a fairly consistent quantity of pyrite with attendant gold. The replacement deposits consist of massive fine-grained pyrite, which has entirely or selectively replaced the rock. Coarse grey ankerite commonly forms an envelope surrounding a deposit and may occur as streaks within it. Siliceous replacements and other sulphide minerals are rare. Replacement orebodies may be pencil-shaped or tabular, the form depending chiefly on the fold structures of the host rock. The mineralogy of the quartz veins and replacement bodies is similar. Gold is the mineral of value. Silver is relatively unimportant because the ratio by weight of gold to silver in both types of ore is approximately 10 to 1. The precious metals are chiefly contained in pyrite, the dominant and commonly the sole sulphide mineral. A number of other minerals occur in minor amounts, including galena, sphalerite, cosalite, bismuthinite, scheelite, pyrrhotite, arsenopyrite, and chalcopyrite. The gold mineralization is believed by the writer to be later than the formation of quartz veins. The veins are later than most of the northerly fault movement because they are concentrated beside the northerly faults, they occur in a conjugate set of fractures related to the faults, and they actually occur within the faults themselves. The major faulting and the vein formation took place later than the major folding of the Cariboo group and after the deposition of the Slide Mountain group. The mineralization is older than the gold-bearing Tertiary gravels. Therefore, on the evidence in the map area the gold mineralization may have occurred between the Carboniferous and Early Tertiary. Outside the map area auriferous quartz veins occur in the Quesnel River group (Late Triassic to possibly Early Cretaceous). It is not unlikely that those of the map area are of Mesozoic age.

Issue ID: B039Title: Geology of Lower Jervis Inlet, British ColumbiaAuthor(s): Bacon, W.R.Series Name: BulletinPublication Year: 1957NTS Map Sheet(s): 092G/12,13; 092F/9,16Place Keyword(s): British Columbia, Southwestern British Columbia, Coast Mountains, Jervis InletLat/Long (NSWE): 50.017, 49.617, -124.117, -123.833Theme Keyword(s): Geology, Mineral DepositsDownload(s):
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Bulletin 39 notes that the flanks of the Coast Mountains have long been recognized as favourable prospecting grounds and the eastern flank, which is entirely in Canada, has proved to be particularly favourable, with the discovery of the Tulsequah, Granduc, Premier, Alice Arm, Bridge River, and B.C. Nickel deposits. In contrast, the core has failed to receive comparable attention. It is difficult to estimate the possibilities of finding new ore deposits in the core of the Coast Mountains because large areas are completely unmapped and the regional geology is relatively unknown. Nevertheless, the available information provides some basis for cautious optimism. Within the area under appraisal important mineral deposits have been found in four localities: Howe Sound (Britannia mine), Observatory Inlet (Hidden Creek mine), Ecstall River, and Princess Royal Island (Surf Inlet mine). The Surf Inlet deposits were gold-bearing quartz veins that averaged 0.39 ounce of gold per ton and 0.3 per cent copper for 1,012,067 tons mined. They proved sufficiently productive to sustain a profitable operation for many years. The veins occur largely in quartz diorite, but it is probable that the shear zone in which the veins occur was localized by a narrow septum of older rock. Gold-bearing quartz veins have been found elsewhere in the granitic rocks. In addition, minor amounts of chalcopyrite, magnetite, molybdenite, and scheelite have been found but, generally speaking, developments to date have yielded little to encourage exploration of the granitic rocks, except along contacts with rocks that they intrude. The copper-bearing sulphide deposits of Howe Sound, Observatory Inlet, and Ecstall River occur in roof remnants of layered rocks that are surrounded in plan by younger granitic rocks. The deposits of Observatory Inlet and Howe Sound have each yielded more than 100 million dollars in mineral wealth, and the Ecstall River deposits are known to contain at least 8,000,000 tons of similar ore but of lower grade. It is thus apparent that the rocks in which these large sulphide deposits occur are worthy of some scrutiny, and it is therefore important to consider what proportion of the core of the Coast Mountain is composed of them. From existing maps it would appear that there is definitely a higher proportion of granitic rocks in the Vancouver-Skeena River interval of the Coast Mountains than in the Skeena River-Portland Canal interval. A recent estimate (Bostock, 1948, p. 82), however, that more than nine-tenths of the Coast Mountains core south of Skeena River is composed of granitic rocks would appear to be too high. An interpretation of the latest geological map of British Columbia (Geol. Surv., Canada, Map 932A, 1948) is that, at shoreline, at least 15 per cent of the region south of Skeena River is composed of non-granitic rocks. Moreover, it is perhaps reasonable to expect that, at higher altitudes, a greater percentage of these rocks will be found. Furthermore, the work in Jervis Inlet has shown that small areas of older rock have been overlooked in the rapid coastal survey, and that stretches of coast barren of outcrop are more likely to be under-lain by sedimentary or volcanic rocks than by the more durable granitic rocks. Thus, although a great deal more work is required before an accurate estimate can be made, it is probable that as much as 20 per cent of the Coast Mountains core south of Skeena River is composed of non-granitic rocks. It has been shown that in Lower Jervis Inlet the non-granitic rocks occur largely in narrow, steeply dipping belts that persist over a vertical range of several thousand feet with little change in width. This generalization, applicable to an area chosen at random, demonstrates that the septum or deep remnant is not unique to Britannia or Ecstall River. It should not be assumed, however, that all the roof remnants persist to depths of several thousand feet. The Caren Range body of the Sechelt Peninsula is regarded as a true roof pendant, and other remnants probably occur with essentially the same shallow irregular form. The point, however, is that certain of the remnants do persist to depths of several thousand feet with little evidence of diminution in size and, because they do, there is no justification for a generalization that most deposits found in the older rocks will necessarily bottom in granitic rocks at depths of a few hundred feet. The remnants of older rock found in the core of the Coast Mountains are small compared to their very productive counterparts in the Canadian Shield. Nevertheless, they are of sufficient size to accommodate very large ore deposits. For example, at Britannia the remnant in which eight very productive orebodies have been found is much smaller in area than some of the other known remnants in the Coast Mountains. In summary, several points have been presented as a basis for appraisal of the economic potential of the interior of the Coast Mountains. They are:- (1) Three localities are known in which large sulphide deposits occur. (2) The sulphide deposits are of similar type; in all, copper is an important constituent. (3) The sulphide deposits occur within remnants of the eroded roof. (4) Probably 20 per cent of the core of the Coast Mountains south of Skeena River consists of roof remnants; the proportion of roof rocks in the Skeena River-Portland Canal interval is considerably higher. (5) Some of the remnants persist to depths of several thousand feet and should not be regarded as roof pendants in the usually accepted sense of that term. (6) Some of the remnants are of sufficient size to accommodate large deposits. The logical conclusion is that, pending evidence to the contrary; roof remnants in the Coast Mountains are definitely worthy of consideration in the search for new deposits of mineral, particularly copper. Prospecting in the area has shown that rocks of the Jervis group contain small deposits of copper, zinc, lead and gold. Very small amounts of copper and gold have been found in the batholithic rocks; in addition, occurrences of molybdenite were observed southeast of Sakinaw Lake. Nothing has been found, however, to suggest that the granitic rocks of the map area warrant further attention by prospectors. Readily accessible dolomitic limestone, in sufficient quantity to be of potential economic importance occurs on the Cambrian Chieftain property. Issue ID: B040Title: Calcareous Deposits of Southwestern British ColumbiaAuthor(s): Mathews, W.H., McCammon, J.W.Series Name: BulletinPublication Year: 1957Scale: 1:1000000NTS Map Sheet(s): 092;Place Keyword(s): British Columbia, Southwestern British Columbia, Texada Island, Vancouver IslandLat/Long (NSWE): 50.5, 48.25, -126, -121.5Theme Keyword(s): Geology, Calcareous Deposits, Limestone, QuarryingDownload(s):
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Bulletin 40 discusses the calcareous deposits of southwestern British Columbia, which exist mainly on Vancouver and Texada Islands. The origins, possible modifications to and weathering of limestones affect their economic potential. The composition and impurities are critical elements in the value and uses of the limestone. Common impurities are magnesium, silica, iron, sulphur and carbon. Quarrying and Processing is influenced by the presence of impure beds and igneous bodies. Topography controls stripping ratio that strongly impacts on quarrying costs. Distance from market and nearness to tidewater are also vitally important. Further, marketing expertise is needed. Typical uses are in the building industry (Portland Cement, Builders' Lime and Building stone), agriculture, metallurgy and the pulp and paper industry. Field criteria for recognizing calcium- and magnesium-rich limestones, sampling techniques and chemical analysis are discussed. Deposits occur in the Cascade Mountains, on Texada Island and on Vancouver Island. Triassic host rocks are the most productive, but marl, travertine and shell deposits in younger rocks have been investigated. Limestone bodies enclosed in granitic rocks also have potential. The Texada Island deposits in the Marble Bay formation have been very important and production there began in the late 1890s. Issue ID: B041Title: Stratigraphy and Structure of the Salmo Lead-Zinc AreaAuthor(s): Fyles, J.T., Hewlett, C.G.Series Name: BulletinPublication Year: 1959Scale: 1:2000NTS Map Sheet(s): 082F/03Place Keyword(s): British Columbia, SalmoLat/Long (NSWE): 49.333, 49, -117.667, -117.083Theme Keyword(s): Geology, Stratigraphy, StructureDownload(s):
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Bulletin 41 describes the stratigraphy and structure of the Salmo lead-zinc area. The map is at a scale of 1 inch equals 2000 feet. The Salmo lead-zinc area is in the Nelson Mining Division of southeastern BC. The mines are in a belt of lead-zinc mineralization extending from the International boundary west of the border crossing point of Nelway to the vicinity of Porcupine Creek, 18 miles north of the boundary. The principal community is the village of Salmo, on the west side of the area 13 miles north of the boundary. Salmo is on the Nelson - Fort Sheppard branch of the Great Northern Railway and the Nelson - Nelway highway, a branch of which runs west to Trail. It is 26 miles by road south of Nelson and about the same distance east of Trail. Geologically, the Salmo lead-zinc area is near the southern end of a structural belt that extends southeast from Revelstoke, south along Kootenay Lake, and southwest across the International boundary. It has been referred to as the Kootenay arc and may be described as a curving belt of heterogeneous lime-bearing sedimentary rocks bowed around the eastern margin of a major batholithic area. Issue ID: B042Title: Geology of the Kemano-Tahtsa AreaAuthor(s): Stuart, R.A.Series Name: BulletinPublication Year: 1960Scale: 1:64375NTS Map Sheet(s): 093E/12Place Keyword(s): British Columbia, Northwestern British Columbia, Kemano, TahtsaLat/Long (NSWE): 53.75, 53.512, -128, -127.667Theme Keyword(s): Geology, Engineering Geology, Surface Geology, Bedrock GeologyDownload(s):
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Bulletin 42 describes the geology and engineering geology in a panel along the route of the Kemano hydroelectric tunnel in the Kemano-Tahtsa area built to provide power for the Aluminum Company of Canada�s Kitimat smelter. The area is 110 miles southeast of Prince Rupert in northwestern British Columbia. Work was done during construction of the tunnel. The surface geology of a 40 square mile area along the route of the tunnel was mapped at 1 inch to � mile scale and an additional 140 square miles at 1 inch to � mile. Underground workings were surveyed at scale 1 inch to 50 feet. The oldest exposed rocks comprise the pre-Middle Jurassic Tahtsa igneous complex, which consists of hornblende diorite and quartz diorite cut by quartz monzonite stocks, granodiorite dykes and basic dykes that is exposed as a window in the Hazelton rocks around the west end of Tahtsa Lake. The area is underlain in large measure by Middle to Lower Jurassic(?) Hazelton Group volcanic and sedimentary rocks and their metamorphic equivalents that unconformably overlie the Tahtsa complex. Volcanics, mainly andesitic lavas, breccias and tuffs, dominate Hazelton stratigraphy in the east. To the west, and lower in the section, these are joined by lenticular limestone beds and metamorphosed argillites and siliceous sediments. Metamorphic grade varies from greenschist to amphibolite facies. In the easternmost part of the area, Lower Cretaceous marine sandstones and shales overlie Hazelton volcanics. These form a 5000 foot section in a monoclinal panel. The contact is probably structural rather than an unconformity. The Coast intrusions are post-Middle Jurassic and occupy the northern and western parts of the map area. They also form dykes and stocks in the older rocks. Intrusive types are gabbro, diorite, quartz diorite, granodiorite and an albite granite stock on Tahtsa peak. Intrusions range to batholithic dimensions. The Kemano gneiss, a zone of mixed granites and gneisses along the Kemano river, crosscut and metamorphose Hazelton strata. The Horetzky diorite and quartz diorite dyke varies from 4000 to 8000 feet in width and dips steeply. It intrudes the Tahtsa complex and Hazelton Group rocks. This dyke is important because more than half the hydroelectric tunnel is within it. From an engineering perspective, rocks of the Coast intrusives were the most satisfactory and those of the Hazelton Group the least satisfactory and Tahtsa complex rocks more variable. The tunnel penetrated the Hazelton rocks near the footwall contact of the dyke, where they are sheared and fractured, which likely accounts for these results.

Issue ID: B043Title: Geology of the Rocher D�boul� RangeAuthor(s): Sutherland-Brown, A.Series Name: BulletinPublication Year: 1960Scale: 1:64375NTS Map Sheet(s): 093M/3W,4EPlace Keyword(s): British Columbia, West central British Columbia, Hazelton MountainsLat/Long (NSWE): 55.25, 55, -127.75, -127.25Theme Keyword(s): Geology, Bedrock GeologyDownload(s):
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Bulletin 43 describes the geology of the Rocher Deboule Range in west-central British Columbia and forms part of the Hazelton Mountains. The range is elliptical in plan, 20 miles by 15 miles, and is isolated by wide valleys from adjacent mountain masses. The range is highly dissected with a total relief of 7,400 feet. During the glacial maxima the high peaks of the range probably rose above the general level of the Cordilleran ice-sheet. The Rocher Deboule Range is underlain entirely by rocks of the Hazelton group and the Rocher Deboule stock of the Bulkley intrusions, but the adjacent valley contains in addition some Tertiary rocks. Only the upper two divisions of the Hazelton group occur in the map area. They are here named the Red Rose formation and the Brian Born formation. The Red Rose formation includes 7,500 to 8,000 feet of marine and non-marine sedimentary rocks of the greywacke suite. In the map area the formation is divided into four members as follows: Member: Lithology; Thickness Feet D: Conglomerate. Greywacke, and shale: partly marine; 50-500 C: Alternating greywacke, siltstone, and shale: partly non-marine; 1000-1200 B: Shale and siltstone; probably marine; 4,000 A: Alternating greywacke, siltstone, and shale with some pebble beds and coal; non-marine; 2,500+ The Brian Boru formation includes 5,000 to 6,000 feet of purple, green, or grey porphyritic andesite breccias and massive flows with minor hornblende porphyry andesite flows and some pyroclastic rocks. The ages of these formations are not known accurately, but the Red Rose formation is probably of latest Jurassic and earliest Cretaceous age and the Brian Boru formation of early Cretaceous age. The Hazelton rocks are intruded by the Rocher Deboule stock, which underlies 27 square miles in the north-central part of the range. The stock is formed of two phases, a slightly porphyritic granodiorite that underlies 24 square miles and a fine-grained quartz monzonite that underlies 3 square miles at the north end of the stock. The quartz monzonite appears to be the younger phase, but closely related in age and origin to the granodiorite. Fortuitous exposure reveals the upper part of the stock to be elongate in shape, a composite of two domes with a connecting saddle, oriented north 25 degrees west. Jointing throughout the stock is pronounced, regular, and patterned. Three sets of joints form an orthogonal system, one set parallel to the contact, a second set striking normal to the contact and radial, and a third set dipping normal to the contact and intersecting it horizontally. The joints are believed to have resulted from cooling contraction of the stock. The Rocher Deboule stock was emplaced passively after the folding of the Hazelton group, between mid-Lower Cretaceous and late Upper Cretaceous. The mode of emplacement may have been by piecemeal stoping. Rocks of the Hazelton group have been thermally metamorphosed by beat from the Rocher Deboule stock and a hornfelsic aureole has been created, with increasing grade toward the stock. The most pervasive new mineral is a purply brown biotite, which occurs in a zone that is 2,000 to 5,000 feet wide horizontally. Higher-grade minerals such as zoisite, amphibole, pyroxene, garnet, sillimanite, and axinite are more erratically distributed than biotite and do not form concentric high-grade zones between the biotite line and the granodiorite contact. In the Bulkley Valley several hundreds of feet of poorly lithified non-marine Paleocene greywacke and shales occur that are intruded and overlain by about 200 feet of columnar andesite flows. The Rocher Deboule Range is a fairly homogeneous structural unit. Folding is moderate, with bedding dips as a rule less than 45 degrees, but details of the pattern are complicated. The major fold is a large scoop-shaped syncline with diverging limbs and an axis trending about north 55 degrees east and plunging 10 to 20 degrees northeast. This fold is less noticeable than the subsidiary folds parallel to the diverging limbs. Fold axes in the Hazelton and Skeena Mountains swing in a large smooth curve, from east in the southwest through northeast at Rocher Deboule, to northwest in the Skeena Mountains in the northeast. The Rocher Deboule Range represents a point of major flexure in this curve. The range is cut by three large, northerly trending normal faults that raise the centre of the range as a horst. The rocks of the range are dropped in relation to neighbouring mountain masses. Faults in the valleys that isolate the range may form a complete elliptical system. The youngest Hazelton rocks, the volcanic breccias and flows of the Brian Boru formation, are preserved within the range and essentially nowhere else. The fundamental structure of the range may be a volcano-tectonic depression. Ores worth eight million dollars have been produced from the range, chiefly tungsten and copper ores. The known mineral showings are concentrated peripherally about the stock, particularly around the northern dome of porphyritic granodiorite. They are chiefly veins filling minor shears which are extensions of joints of the orthogonal system. The veins have been mineralized in three stages. The first stage is primarily pegmatitic and characterized by hornblende with scheelite and ferberite; the second stage is primarily sulphide characterized by chalcopyrite, arsenopyrite, and cobalt-nickel sulpharsenides; the third stage is characterized by milky quartz with sphalerite, tetrahedrite, galena, and chalcopyrite, forming entities which distinctly cut mineralization of the first two stages. The veins probably owe their origin to the stock and their distribution to factors resulting from its cooling history, including the evolution of the joint system, minor shearing forces, and thermal control of deposition. The principal producing properties are the Rocher Deboule copper mine and the Red Rose tungsten mine. These mines and the other prospects are described.

Issue ID: B044Title: Geology of the Fraser River Valley Between Lillooet and Big Bar CreekAuthor(s): Trettin, H.P.Series Name: BulletinPublication Year: 1961Scale: 1:31680NTS Map Sheet(s): 092I/12,13; 092J/16; 092O/1; 092P/4Place Keyword(s): British Columbia, Fraser River, Lillooet, Big Bar Creek, Bowman RangeLat/Long (NSWE): 51.333, 50.692, -122.25, -121.583Theme Keyword(s): Geology, Bedrock GeologyDownload(s):
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Bulletin 44 describes the geology and mineral deposits of a 550 square mile area between Lillooet and Big Bar, British Columbia. The area was mapped at a scale of 1 mile to the inch. In the southern part of the Bowman Range four members are recognized in the Middle (?) and Upper Permian Marble Canyon formation, which is partly composed of reefal limestone. This formation forms a northwesterly trending anticlinorium overturned to the northeast. The cherts, argillites, limestones and volcanic rocks west of the Bowman Range, originally referred to the Permo-Pennsylvanian Cache Creek group, are shown to be Permo-Triassic and are here assigned to the Pavilion group, a new group that is made up of two divisions. Microscopic and stratigraphic evidence is given that the cherts of this group are of radiolarian origin. The Lower Cretaceous Lillooet group here is subdivided into three units. Divisions A and B are shown to form a northwesterly trending anticline. Three members are now recognized in Division A of the Lower Cretaceous Jackass Mountain group. The Lower Cretaceous Spences Bridge group is subdivided into several local and stratigraphic units. Two units previously assigned to the Spences Bridge group are correlated with the Kingsvale group on the basis of new fossil collections. Some volcanic and sedimentary rocks originally referred to the Miocene Kamloops group are here correlated with Miocene to Pleistocene rooks of the Quesnel map area. West of Lillooet a belt of serpentinite was mapped that has structural and lithological similarities to the Upper Triassic ultrabasic intrusions of the Shulaps Range. Granitic rocks of three ages are recognized and range from early Lower Cretaceous or older to mid Lower Cretaceous. It had earlier been shown that the Fraser River fault zone consists of several normal faults with relative downward movement to the east. East of these faults the author recognizes another fault with relative downward movement to the west. Lower Cretaceous and early Tertiary rocks thus occupy a graben between Permo-Triassic units to the northeast and to the southwest. This graben probably controlled the deposition of Divisions B and C of the Jackass Mountain group. The faulting may be related to the isostatic rise of adjacent granitic masses. Evidence is given that the latest movement on one of the faults took place in mid Tertiary time.

Issue ID: B045Title: Geology of the Ferguson Area, Lardeau District, British ColumbiaAuthor(s): Fyles, J.T., Eastwood, G.E.P.Series Name: BulletinPublication Year: 1962Scale: 1:31680NTS Map Sheet(s): 082K/11,12,13,14Place Keyword(s): British Columbia, Southeastern British Columbia, Lardeau District, Ferguson AreaLat/Long (NSWE): 50.75, 50.606, -117.65, -117.25Theme Keyword(s): Geology, Stratigraphy, Structure, Bedrock GeologyDownload(s):
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Bulletin 45 describes the geology of the Ferguson area, Lardeau District, British Columbia, which is in southeastern British Columbia, about 40 miles southeast of Revelstoke and 80 miles north of Nelson. The area is near the north end of the Kootenay arc, a curving belt of complexly deformed sedimentary', volcanic, and metamorphic rocks extending from Revelstoke southeast and south across the International Boundary. This report is primarily a study of the structure and stratigraphy of part of the Kootenay arc and is one phase of a broader study of the arc that is continuing. The area lies within the Selkirk Mountains. The highest summits have elevations just over 9,000 feet; the lowest point in the area, Trout Lake, has an elevation of 2,345 feet. The valleys of Gainer, Ferguson, Lardeau, and Wilkie (Trout) Creeks, which cut across the formational strike, provide good structural and stratigraphic cross sections. The area contains a thick sequence of highly deformed sedimentary and volcanic rocks intruded by small masses of diorite. Most of the rocks belong to the Hamill group, Badshot formation, and Lardeau and Milford groups. The Badshot is probably Lower Cambrian, though no fossils have been found in it. Rocks of the Milford group contain Mississippian fossils. The oldest rocks are found in the northeastern part of the map area. They strike northwest and are complexly folded into tight and isoclinal synclines and anticlines with low plunge. The folds produce a cumulative dip to the southwest, and regionally the stratigraphic top is to the southwest. The stratigraphic succession as exposed northeast of Trout Lake is summarized in a table of formations on page 13. This report gives the first detailed account of the succession within the Lardeau group. Little is known of the stratigraphy and correlation of rocks in the area southwest of Trout Lake. Most of the area contains a succession of grey argillites, phyllites, and grits that are complexly folded and contain no distinctive markers. Two distinctive units, a light-grey dolomite and a green volcanic rock, are exposed along the southwestern edge of the map area. The structure of the Ferguson area is dominated by complex folds. The folds are isoclinal in phyllitic rocks below the Ajax formation and are asymmetric or overturned in the overlying more competent formations. Northeast of Trout Lake, fold axes plunge at low angles both to the northwest and southeast and axial planes dip steeply. Southwest of Trout Lake fold axes plunge 20 to 40 degrees to the northwest, axial planes are essentially vertical, and many of the folds are isoclinal. The largest folds in the area are an anticline and complementary' syncline known as the Silvercup anticline and Finkle Creek syncline. The anticline is southwest of the syncline and separated from it by a series of strike faults named the Cup Creek fault zone. The Silvercup anticline and the Finkle Creek syncline, though complicated in detail, have a general cross sectional shape looking northwest of a letter "N." Southwest of the anticline and northeast of the syncline, the folds have the same general form and are smaller than the anticline and syncline. The pattern of folding implies a relative movement of the southwest side upward and over the northeast. The principal mineral deposits in the area contain silver, lead, and zinc. Most deposits were discovered before 1900, and a great deal of the exploration and mining was done before 1920. Total production amounts to 44,259 tons. Gross contents: Gold, 6,941 ounces: silver, 2,205,383 ounces; copper, 5,439 pounds; lead, 9,056,174 pounds; zinc, 435,033 pounds. As early as 1903, it was recognized that the mineral deposits in the Lardeau district fall into three belts - the lime dyke belt, the central mineral belt, and the southwest mineral belt. The most common deposits in the lime dyke belt contain galena in siderite, which has replaced limestone. In this belt are the Molly Mac, Index, White Quail, and Silver Chief properties, which are in the Lade Peak limestone and limestones in the Index formation. More than 85 per cent of the ore mined in the Ferguson area has come from the central mineral belt. The polymetallic veins of the Silver Cup, Triune, Nettie L, and True Fissure mines account for most of the production. These deposits and others from which there has been little or no production are veins and lodes containing galena, argentiferous tetrahedrite, sphalerite, and locally chalcopyrite. They are southwest of the Cup Creek fault zone and near the crest of the Silvercup anticline. Descriptions of many of the deposits within the area and their relationship to the regional structure and lithological types are given in Chapter 1V.

Issue ID: B046Title: Late glacial history and surficial deposits of the Okanagan Valley, British ColumbiaAuthor(s): Nasmith, H.Series Name: BulletinPublication Year: 1962Scale: 1:100000NTS Map Sheet(s): 082E; 082LPlace Keyword(s): British Columbia, Okanagan ValleyLat/Long (NSWE): 50.55, 49, -119.84, -119Theme Keyword(s): Surficial Geology Map, Surficial Deposits, Surficial GeologyDownload(s):
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Bulletin 46 describes the late glacial history and surficial deposits of the Okanagan Valley in British Columbia. The fieldwork on which this report is based was originally undertaken at the request of the Department of Agriculture in order to assess the possibilities of obtaining groundwater to supplement surface waters for irrigation in the Okanagan Valley. This report presents an account of the late glacial history of the Okanagan Valley, when the last remnant of the Pleistocene ice-sheet wasted away and disappeared. The main body of the report deals with six map areas showing the distribution of late glacial features, and each map area is accompanied by a description of each feature and an interpretation of its significance in relation to other features in the same map area.

Issue ID: B047Title: Geology of the Cariboo River Area, British ColumbiaAuthor(s): Sutherland-Brown, A.Series Name: BulletinPublication Year: 1963Scale: 1:126720NTS Map Sheet(s): 093A/14,15; 093H/2,3,6,7Place Keyword(s): British Columbia, East central British Columbia, Cariboo Mountains, Cariboo River Area, Quesnel HighlandsLat/Long (NSWE): 53.333, 52.75, -121.5, -120.16Theme Keyword(s): Geology, Bedrock GeologyDownload(s):
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Bulletin 47 discusses the geology of the Cariboo River area, British Columbia, which includes about 1,000 square miles of dissected plateau of the Quesnel Highlands and alpine peaks of the Cariboo Mountains in east-central British Columbia. The area is underlain by three groups of stratified rocks. The Kaza Group is a thick succession (17,000+ feet) of gritty feldspathic micaceous quartzites and silvery green schists of Late Proterozoic age. It is overlain conformably by the Cariboo Group of Cambrian, Ordovician (?), and later age. This group is composed of 7,000 to 9,000 feet of phyllites, micaceous quartzites, and limestones and is divided into six formations. Carbonate and fine elastic rocks are dominant in the lower part of the group, whereas coarser elastic rocks are dominant in the upper. The Slide Mountain Group is composed of at least 5,000 feet of basal conglomerate, pillow basalts, and bedded chert, and is probably of Mississippian age. Tectonism rose to a peak toward the end of Kaza deposition, but stable shallow marine conditions persisted throughout early Cariboo deposition. Tectonism increased again erratically but progressively toward the close of Cariboo deposition. Folding and metamorphism preceded deposition of the Slide Mountain Group. The structure of the region culminates in a broad northwest-trending anticline, the Lanezi arch, which exposes the Kaza Group. This fold is flanked on the northeast by the Isaac Lake synclinorium, a system of moderately tight folds and parallel normal and thrust faults. Individual folds are overturned to the southwest, and the intensity of overturning and compression increases toward the Lanezi arch (southwest). The synclinorium exposes chiefly Cariboo Group and some Kaza Group. The Lanezi arch is flanked on the southwest by a folded belt of Cariboo Group, and this is overlain in part by the trough of the Slide Mountain Group. Folds in the Cariboo Group are gentle on the flank of the Lanezi arch but increase in overturning and compression to the southwest, becoming isoclinal toward the Little River. All folds plunge gently northwestward. A system of strike faults is related to folds of the Isaac Lake synclinorium. Northerly and north-easterly normal faults are widely distributed and compensate in part for the northwestward plunge of folds. All elastic rocks except those of the Slide Mountain Group are schistose, but the degree varies widely with locality and rock type. Schistosity is generally related to fold axial planes. In the Lanezi arch it is related to the axial planes of some of the larger secondary folds of the flanks, but progressively changes to bedding schistosity toward the main axis. In general, Kaza rocks are in the biotite-chlorite subfacies and Caribou rocks in the muscovite-chlorite subfacies of the greenschist facies. Toward the southwest, Cariboo rocks have been raised locally to amphibolite facies in association with a belt of small plutons at the edge of the area.

Issue ID: B048Title: Landforms of British Columbia, A Physiographic OutlineAuthor(s): Holland, S.S.Series Name: BulletinPublication Year: 1964Scale: 1:1900800NTS Map Sheet(s): 082;083;092;093;094;102;103;104;114Place Keyword(s): British ColumbiaLat/Long (NSWE): 60, 48, -139, -114Theme Keyword(s): Geology, LandformsDownload(s):
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Bulletin 48 is an authoritative account of the major land subdivisions of British Columbia. It defines the boundaries of the various mountain, plateau, or plain areas, many of them for the first time. Agreement has been reached with the Canadian Permanent Committee on Geographical Names, with Provincial Government officials, and with geologists and the various sorts of map-makers whose knowledge of the Province is most thorough. The form of presentation, and much of the subject-matter, is a reflection of the mind and the interests of the writer, who was a field geologist with a broad knowledge of the Province. Concluding are five short essays that are written to clarify the text, and complete glossary of terms. In 2009 Mitch Mihalynuk, a project geologist with the BC Geological Survey, digitized the PDF map, and the Manifold map and Shape files are provided with this publication. The Manifold map includes the BC border and symbolized boundaries between physiographic regions. Issue ID: B049Title: Geology of the Duncan Lake Area, Lardeau District, British ColumbiaAuthor(s): Fyles, J.T.Series Name: BulletinPublication Year: 1964Scale: 1:63360NTS Map Sheet(s): 082K/2,3,6,7Place Keyword(s): British Columbia, Kootenays, Purcell Trench, Lardeau District, Duncan Lake AreaLat/Long (NSWE): 50.45, 50.15, -117.1, -116.8Theme Keyword(s): Geology, Structural Setting, Lead-zinc Deposits, Bedrock GeologyDownload(s):
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Bulletin 49 covers the Duncan Lake area, which includes about 200 square miles in southeastern British Columbia containing Duncan Lake and the north end of Kootenay Lake. The area straddles the Purcell trench, the western part lying along the eastern slope of the Selkirk Mountains and the eastern part lying in the Purcell Mountains. Rocks of the area form part of the Kootenay arc, a curving belt of complexly deformed sedimentary, volcanic, and metamorphic rocks extending from Revelstoke southeast, south, and southwest across the International Boundary. This report is primarily a study of the structure and the structural setting of lead-zinc deposits developed recently at the Duncan mine. Rocks in the area belong to the Hamill and Lardeau Groups and are highly deformed sedimentary and volcanic rocks. The lithology and stratigraphy are summarized in the table on page 32. They are very similar to rocks of the Ferguson area 50 miles to the northwest, with which they have been correlated. Many of the formations can also be readily correlated with rocks in the Salmo area, 150 miles to the south, and the Rogers Pass area, 100 miles to the northwest. Though no fossils have been found in the Duncan Lake area, the rocks are known to be pre-Mississippian, and the Badshot Limestone, a prominent marker in the area, elsewhere contains Lower Cambrian fossils. Sills of felsite, which are common in the southwestern part of the area, dykes of lamprophyre, and small sill-like bodies of amphibolite constitute the only intrusive rocks. Within the area the grade of regional metamorphism increases from low grades characteristic of the northwesterly trending part of the arc northwest of Duncan Lake to garnet and higher grades characteristic of rocks along Kootenay Lake. The garnet isograd trends north from near the northwest corner of Kootenay Lake to the northern end of Duncan Lake. Complex folds dominate the structure of the area. Several stages of folding are recognized, which probably all belong to one orogenic period, thought to be Mesozoic. The oldest folds recognized, called Phase I folds, are isoclinal and plunge at low angles to the north. Most of these folds cannot be seen, and are reconstructed from studies of the distribution of rock sequences and the mapping of formations. The limbs and axial planes of these folds are curved and have been folded by Phase II folds. The principal Phase I folds are, from east to west, the Howser syncline, the Duncan anticline, the St. Patrick syncline, and the Meadow Creek anticline. Phase II folds are more open than Phase I folds. The folds plunge mainly to the north and northwest at angles as great as 30 degrees, but most plunge between north 15 and 25 degrees west at 5 to 10 degrees. Phase II folds are clearly visible in many outcrops and are defined by the layering of the rocks and by the attitudes of the formations. Strike faults, many of which are parallel to the cleavage planes in Phase II folds, are common. Some faults are related and subordinate to the folding; others are superimposed on it. The most important mineral deposits in the area are relatively low-grade zones of lead-zinc mineralization that have been developed recently but not mined. They are referred to as the Duncan type of deposit, from the Duncan mine. Essentially all the deposits of the Duncan type are in the Badshot Formation on the Duncan anticline. Some 15 to 20 mineralized zones of this type are known within the map area. They consist of pyrite, sphalerite, galena, and minor pyrrhotite disseminated in dolomite and siliceous dolomite. They are lenticular zones with gradational but, in general, well-defined margins. The attitude is essentially parallel to that of the enclosing formations; the largest dimension is parallel to the strike, and the intermediate dimension is parallel to the dip. The longest axes of the mineralized zones plunge at low angles to the north, parallel to the axes of Phase II folds. The greatest plunge length found so far is more than 3,000 feet, The height may be as great as 500 feet, and the thickness is generally a few tens of feet but may be as much as 100 feet. The average grade is less than 10 per cent combined lead and zinc, and the grade of the zinc is greater than that of the lead. Dolomite and siliceous dolomite in which The Duncan type of deposits are found are dark-grey rocks with mottled, flecked, and banded textures resulting from deformation. The mineralized zones appear to be structurally controlled replacements of the dolomite. Relatively thick and continuous dolomite layers on the Duncan anticline have localized mineralization. The only production from mines in the area has been from a number of silver-rich lead-zinc deposits of various types. Total production from the area amounts to 2,100 tons from five properties. Four of these properties are veins and replacements in limestone and dolomite. The fifth property contains quartz veins carrying tetrahedrite.

Issue ID: B050Title: The Devonian Slave Point, Beaverhill Lake, and Muskwa Formations of Northeastern British Columbia and Adjacent AreasAuthor(s): Griffin, D.L.Series Name: BulletinPublication Year: 1965Scale: 1:700000NTS Map Sheet(s): 094;Place Keyword(s): British Columbia, Northeastern British Columbia, Slave Point, Beaverhill lake, Muskwa FormationsLat/Long (NSWE): 60, 48, -124, -120Theme Keyword(s): Geology, Stratigraphy, Bedrock GeologyDownload(s):
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Bulletin 50 describes the geology and stratigraphy of the Devonian Slave Point, Beaverhill Lake, Muskwa Formations and adjacent area. This area lies in northeastern British Columbia. Issue ID: B051Title: Jurassic and Cretaceous Strata of the Bullhead Succession in the Peace and Pine River FoothillsAuthor(s): Hughes, J.E.Series Name: BulletinPublication Year: 1964NTS Map Sheet(s): 093O; 094A,094BPlace Keyword(s): British Columbia, Northeastern British Columbia, Pine River, Peace RiverLat/Long (NSWE): 56.5, 54.667, -123, -121.5Theme Keyword(s): Geology, Stratigraphy, Bedrock GeologyDownload(s):
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Bulletin 51 describes the Jurassic and Cretaceous strata of the Bullhead Succession in the Peace and Pine River foothills. The map scale is one inch equals one and a half miles. Issue ID: B052Title: Geology of the Pine Valley, Mount Wabi to Solitude Mountain Northeastern British ColumbiaAuthor(s): Hughes, J.E.Series Name: BulletinPublication Year: 1967Scale: 1:64000NTS Map Sheet(s): 093O/8,9,10; 093P/5,12Place Keyword(s): British Columbia, Northeastern British Columbia, Pine Valley, Rocky Mountain FoothillsLat/Long (NSWE): 55.75, 55.459, -122.608, -121.5Theme Keyword(s): Geology, Stratigraphy, Bedrock GeologyDownload(s):
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Bulletin 52 describes the geology of the Pine Valley area from Mount Wabi to Solitude Mountain in northeastern British Columbia. The map area covers the Pine Valley, in the Rocky Mountain Foothills or northeastern British Columbia, from latitude 55 degrees 30 minutes to latitude 55 degrees 45 minutes north. The exposed rocks are Triassic, Jurassic, and Cretaceous in age. The succession (Ladinian to Cenomanian) is between 10,000 and 20,000 feet thick, and mostly of marine deposition. Most stratigraphic units thicken westward. In the Triassic, the Grey Beds contain limestones, dolomites, siltstones, and sandstones; and the overlying Pardonet Formation, argillaceous limestones with fossil shell beds of Halobia and Monotis. The Fernier Group of Jurassic age consists of: thin limestone, interbedded shale's and siltstones with cherty banding, the Nordegg Beds; followed by the Middle Shales; and in the upper part, interbedded shale's, siltstones, and sandstones, the Transition Beds, which mark the change to Beaudette deposition. The Beaudette Group of late Jurassic to early Cretaceous age has three formations; the Monteith, thick sandstones mostly, and with quartzites in the upper third part; the Beattie Peaks, interbedded shale's, siltstones, and sandstones; and the Monach Formation, sandstones, with or without quartzite beds at the top. Facies changes and incomplete outcrops make it advisable to map Beaudette strata as an undivided unit to the west. Coal measures overlying Beaudette strata are described by the term Crassier Group. The group is a continuous sequence of deposits in the field. They have a complex lithology: shale's, mudstones, siltstones, sandstones, grits, conglomerates, and coals, laid down in cyclic repetition. The sequence is undivided to the west. Eastward it can be divided into the Brenot, Dresser, and Gething Formations, according to their sand/shale ratios, the nature of the cyclothems, and the distribution of the coarser clastics. The map area covers the Pine Valley, in the Rocky Mountain Foothills or northeastern British Columbia, from latitude 55 degrees 30 minutes to latitude 55 degrees 45 minutes north. The exposed rocks are Triassic, Jurassic, and Cretaceous in age. The succession (Ladinian to Cenomanian) is between 10,000 and 20,000 feet thick, and mostly of marine deposition. Most stratigraphic units thicken westward. In the Triassic, the Grey Beds contain limestones, dolomites, siltstones, and sandstones; and the overlying Pardonet Formation, argillaceous limestones with fossil shell beds of Halobia and Monotis. The Fernier Group of Jurassic age consists of: thin limestone, interbedded shale's and siltstones with cherty banding, the Nordegg Beds; followed by the Middle Shales; and in the upper part, interbedded shale's, siltstones, and sandstones, the Transition Beds, which mark the change to Beaudette deposition. The Beaudette Group of late Jurassic to early Cretaceous age has three formations; the Monteith, thick sandstones mostly, and with quartzites in the upper third part; the Beattie Peaks, interbedded shale's, siltstones, and sandstones; and the Monach Formation, sandstones, with or without quartzite beds at the top. Facies changes and incomplete outcrops make it advisable to map Beaudette strata as an undivided unit to the west. Coal measures overlying Beaudette strata are described by the term Crassier Group. The group is a continuous sequence of deposits in the field. They have a complex lithology: shale's, mudstones, siltstones, sandstones, grits, conglomerates, and coals, laid down in cyclic repetition. The sequence is undivided to the west. Eastward it can be divided into the Brenot, Dresser, and Gething Formations, according to their sand/shale ratios, the nature of the cyclothems, and the distribution of the coarser clastics. The Fort St. John Group contains alternations of shale formations, the Moosebar in the lower part, the Hasler, and the Cruiser, with sandstone formations, the Commotion, and the Goodrich. These units are largely marine, with the exception of thin non-marine beds and coal measures in the Commotion Formation. The Dunvegan strata are mostly non-marine, and they form the youngest formation of the Cretaceous in the map area. The sedimentary rocks were deformed and uplifted in the Rocky Mountain orogeny, one phase of the Laramide revolution. The Rocky Mountain Foothills in the Pine area are in two parts: the Inner (or Western) Foothills and the Outer (or Eastern) Foothills. The structures of the Inner and Outer Foothills represent different tectonic styles. Close folding and thrusting prevailed in the Inner Foothills, and the deformation resembles that of the Rocky Mountains on the west. The Outer Foothills contain long anticlines separated by wide synclines, and here the deformation was restricted to the anticlinal folding, and faulting along the anticlines. The Outer Foothills belong to the orogenic foreland. Their structures can he ascribed to block faulting in the basement, though positive evidence is lacking. Folding in the Foothills is of parallel type. The fold forms are concentric, or angular. The angular folds (that is, parallel folds of non-concentric form) include those of cuspate and lambdate forms, in the writer's classification. Two types of concentric folds are distinguished-those of low and high fold amplitude respectively. Concentric anticlines of low fold amplitude occur in the Outer Foothills. The Commotion anticline is the only example that has been drilled to depth. Its surface and subsurface structures differ considerably, and they are separated by a low angle thrust, or d�collement, or a zone of complex folding and shearing. High-amplitude concentric anticlines have fold centres at shallow levels, and may be underlain by cuspate and angular folds, as well as d�collements. Concentric folds of high amplitude, cuspate, and angular folds occur together in the Inner Foothills. According to the writer's view, cuspate anticlines developed by replacing concentric anticlines during the folding compression. Lambdate folds are not specially related to concentric folds, and the few examples noted lie close to fault planes. The structures of the Pine Valley area form part of a larger tectonic frame-work, which includes: the junction of the northern and southern parts of the Rocky Mountains; and in the Plains, the junctions of three tectonic units of the foreland, the Halfway block, the Fort St. John arch, and the Alberta syncline. The junction of tectonic units of the foreland now occupy the site of the Peace River embayment, a paleotectonic basin of differential subsidence and sedimentation lying transversely to the former miogeosyncline along the site of the Rocky Mountains and Foothills. Observations, and analyses of structural geology presented here, are of use in exploring for petroleum and natural gas. Natural gas has been discovered in the Pine River anticline. Important reserves of coal occur in the Pine Valley.

Issue ID: B053Title: Geology of the Ainsworth-Kaslo Area, British ColumbiaAuthor(s): Fyles, J.T.Series Name: BulletinPublication Year: 1967Scale: 1:12000NTS Map Sheet(s): 082F/10,15; 082K/2Place Keyword(s): British Columbia, Southeastern British Columbia, Kootenays, Ainsworth, KasloLat/Long (NSWE): 50.15, 49.667, -117, -116.895Theme Keyword(s): Geology, Structure, Structural Setting, Lead-zinc Deposits, Bedrock GeologyDownload(s):
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Bulletin 53 covers the geology and mineral deposits of the Ainsworth-Kaslo area, which is along the western side of Kootenay Lake 40 to 60 miles northeast of Nelson in British Columbia. It is in the central part of the Kootenay Arc, a curving belt of complexly deformed sedimentary, volcanic, and metamorphic rocks extending from Revelstoke southeast, south, and southwest across the International Boundary. The map area is in the northerly trending part of the arc adjacent to the eastern margin of the Nelson batholith. This report is primarily a study of the structure and the structural setting of lead-zinc deposits in the Ainsworth mining camp. The rocks of the area range from Lower Cambrian to Upper Triassic and include medium- and fine-grained mica schists, limestones and marbles, hornblende schists and quartzites. They are intruded by sills and lenses of fine-grained granite, granite pegmatite, the Nelson granitic batholith, and by lamprophyre sills and dykes. Details of the lithology are summarized in the report and tentative correlations are shown. The rocks belong to the Lardeau, Milford, Kaslo, and Slocan Groups. The grade of regional metamorphism increases toward the east, from biotite near the Nelson batholith to sillimanite grade along the shore of Kootenay Lake. Throughout the area the rocks, which are strongly foliated, dip at moderate angles to the west and are split by strike faults essentially parallel to the foliation. In each fault slice, isoclinal folds are the oldest structures recognized and are referred to as Phase I folds. They have a low plunge, dominantly to the north, and mainly west-dipping curved axial planes. More open folds, called Phase II, are also found in each fault slice. They have a low plunge to the north and have axial planes with a low to moderate dip to the west. In general they cause the west-dipping foliation to steepen upward. They have the form in profile of a modified S when viewed from the south. Late folds, which in general plunge at moderate angles to the west and northwest, and have steeply dipping axial planes that strike between west and northwest, are found locally. Phase I and Phase II folds are tentatively correlated across the fault slices and with the same sort of structures in the Duncan Lake area 20 miles to the north. The Ainsworth Camp contains more than 50 properties from which silver-lead-zinc has been produced. In addition, there are many other showings from which there has been no production. Total production since the first shipment in 1889 has amounted to 763,858 tons of ore to the end of 1964. The deposits are mainly simple quartz carbonate veins containing shoots and lenses of galena, sphalerite, pyrite, and locally pyrrhotite. The veins form three fairly well defined systems and two or three clusters, or poorly defined systems. The vein systems are zones of faulting. The Florence trends north 70 to 75 degrees west and dips 45 degrees to the south. The Highland strikes northwest and dips steeply to the southwest, and the Highlander strikes north and dips 45 degrees west parallel to the foliation. The attitudes of the veins and mineralized fractures are summarized in Figure 8. The vein fractures are normal faults with a maximum displacement of a few hundred feet. In veins that transgress the foliation, sulphides tend to be concentrated (a) where the veins pass from one rock type to another, (b) where the veins branch or split, and � where the veins have tended to open by displacement during mineralization. Commonly these situations are combined. In the veins parallel to the foliation, the control of mineralized shoots is more difficult to determine. Individual orebodies are small. The largest stoped areas are about 600 feet along the strike, 800 feet parallel to the dip, and 4 to 6 feet wide. Judging from production figures, grades of more than 50 per cent lead and 20 per cent zinc were obtained in ore sorted for direct shipping, whereas grades of about 5 per cent lead and 2 per cent zinc were obtained in ore mined in quantity for milling. The silver content amounts to one-half to one-third of an ounce per ton for every unit of lead. Replacement deposits of galena, sphalerite, pyrite, and pyrrhotite in fractures in the Ainsworth limestone and Early Bird Formation constitute the largest known reserve in the camp. They are geologically like the Bluebell deposits on the eastern shore of Kootenay Lake directly across from the north end of the Ainsworth Camp. On the Lakeshore property in the Ainsworth Camp, where this type of deposit has been extensively explored by Cominco Ltd., five groups of fractures along which sulphides have replaced the lower Ainsworth limestone strike between north 65 and 75 degrees west and dip steeply to the south. Replacement mineralization has spread out from the fractures a few inches to a few feet along the foliation at several horizons within the limestone. This study of the Ainsworth-Kaslo area has shown that the fault and fracture system containing the Ainsworth deposits is superimposed on a complexly folded group of rocks. The fracture system itself and its subsequent history controlled the distribution and attitude of the veins and oreshoots.

Issue ID: B054Title: Geology of the Queen Charlotte IslandsAuthor(s): Sutherland-Brown, A.Series Name: BulletinPublication Year: 1968Scale: 1:125000NTS Map Sheet(s): parts of (103B/W�; 103C/NE; 103F/E�; 103G/W�; 103J/4; 103K/SE)Place Keyword(s): British Columbia, Queen Charlotte IslandsLat/Long (NSWE): 54.2, 51.91, -133.05, -130.95Theme Keyword(s): Geology, Structural, Mineral Resources, Bedrock GeologyDownload(s):
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Bulletin 54 discusses the geology and mineral deposits and considers the exploration potential of the Queen Charlotte Islands, which are at the western edge of the continental shelf seaward of central British Columbia. The islands have a land area of about 3,840 square miles, which is divided into three main physiographic units: the Queen Charlotte Ranges on the southwest, Skidegate Plateau in the centre, and Queen Charlotte Lowlands on the northeast. In the Pleistocene the islands were intensively glaciated. The fundamental structural unit of the Queen Charlotte Islands is a thick (15,000+ feet) pillowed basalt of Late Triassic age. The basalts are separated by a flysch-like sequence of Latest Triassic and Early Jurassic age from an explosive porphyritic andesite of Middle Jurassic age and largely marine deposition. Two Cretaceous sedimentary units, the first flysch-like and the second mollasse-like, were deposited and are successively less involved in deformation. A final Early Tertiary period, largely of subaerial volcanism, deposited some 18,000 feet of intercalated columnar alkali basalt floods and sodic rhyolite ash flows. These are gently warped, eroded, and overlain by up to 6,000 feet of Mio-Pliocene sands and shale's. Large lineal bodies of hornblende diorite to quartz diorite were emplaced in the Mid to Late Jurassic and a more varied sequence of quartz diorite to soda granite in the Early Tertiary, mostly along major lineal faults. Crustal fracturing has been the dominant mechanism of deformation, controlling volcanism, sedimentation, intrusion, and secondary folding. Major north westerly lineal faults form a pattern related to the Queen Charlotte fault. The trace of the latter is along the continental slope. The major northwesterly faults have been active since at least the Early Cretaceous, and generally they combine right-hand wrench movement with normal east-block-down displacement. The mineral resources of the islands are extensive. At present pyrometasomatic iron-copper deposits are the most important by several orders of magnitude but the potential for gold mineralization is high. Mineable reserves have a gross value of about $200 million. Production has come from two main properties-Tasu and Jedway.

Issue ID: B055Title: Geology of the Kennedy Lake Area, Vancouver Island, British ColumbiaAuthor(s): Eastwood, G.E.P.Series Name: BulletinPublication Year: 1968Scale: 1:32200NTS Map Sheet(s): 092F/3,4Place Keyword(s): British Columbia, Western Vancouver Island, Kennedy LakeLat/Long (NSWE): 49.1, 49, -125.62, -125.4Theme Keyword(s): Geology, Bedrock GeologyDownload(s):
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Bulletin 55 describes the geology of the Kennedy Lake area, Vancouver Island, British Columbia, which includes a land area of about 27 square miles around the main part of Kennedy Lake, on the west coast of Vancouver Island. It includes parts of the Estevan Coastal Plain and the Vancouver Island Mountains. The northwest half of the area is largely underlain by andesite lavas of the Karmutsen Group, and the southeast half by batholithic intrusive rocks of intermediate composition. Sedimentary rocks of the Quatsino Formation and mainly pyroclastic rocks assigned to the Bonanza Group form a relatively narrow belt trending northeast through the middle of the area, largely separating the Karmutsen and batholithic rocks. A roof pendant or large inclusion of the Quatsino sedimentary rocks occurs in the batholithic rocks in the eastern part of the area, and is host to the magnetite orebodies of Brynnor Mines Limited. Some Quatsino limestone is infolded in the Karmutsen lavas in the northwest part of the area. The Quatsino Formation overlies the Karmutsen Group and underlies the Bonanza Group. In the Kennedy Lake area it comprises a lower Limestone member, at least 2,000 feet thick, a middle argillite member, 800 feet thick, and an upper limestone member, 350 feet thick. The contacts are gradational. The limestone members contain few impurities and are thick bedded to massive. The argillite is feldspathic and probably tuffaceous. It is thin bedded and commonly markedly banded by the alternation of beds of contrasting colour. The formation is of Upper Triassic age. The sedimentary and volcanic rocks have been successively intruded by andesite, an Older Porphyry, the batholithic rocks, a Younger Porphyry, and basalt and gabbro. With the exception of the batholithic rocks, these rocks occur mostly as narrow dykes and sills; a few small stocks of andesite, Older Porphyry, and gabbro are present. The andesite is particularly common in the lower limestone. The batholithic rocks include diorite and tonalites, which appear to be contemporaneous, and granodiorite-quartz monzonite, which intrudes the diorite. A minor part of the diorite, and possibly part of the mafic tonalite, apparently resulted from recrystallization and metasomatism of andesite, but most of the batholithic rocks were evidently intruded as magma. A potassium-argon date of 167 million years was obtained from the granodiorite. The diorite and tonalites are older by from a few thousand to a few million years. A potassium-argon date of 121 million years was obtained from a dyke of Younger Porphyry. The sedimentary and volcanic rocks were folded about northeast- to north-trending axes. The best-defined folds are a syncline through Salmonberry Mountain, just south of Kennedy Lake, and an anticline in the pendant of Quatsino rocks in the east part of the area. For the most part, these folds plunge gently southwest, but at the mine the anticline is buckled sharply downward and backward. This down-buckle is probably a later structure superimposed on the primary folding. The rocks have been broken by many faults of small displacement, and by several with displacements measurable in miles or fractions of a mile. The largest strikes north along the foot of Salmonberry Mountain and displaces the Karmutsen-Quatsino contact between 1 and 2 miles to the left. It appears to branch under Kennedy Lake, and to the south it curves away to the southwest. Almost all the displacement took place prior to batholithic intrusion, although granodiorite has been sheared adjacent to the fault by renewed movement. Lesser faults have offset the Salmonberry Mountain syncline and truncated an infold of limestone west of the lake. A fault in the open pit appears to have displaced the limestone-argillite contact about 200 feet. The only economic mineral in the area is magnetite, and of seven occurrences described, only the Brynnor mine deposit is commercially significant. It comprises two irregular orebodies that more or less follow the down-buckled faulted contact between the lower limestone and the argillite. The upper orebody, west of the fault, has been mined by open-pit methods. The lower orebody, east of the fault, was partly developed for underground mining before the project was abandoned.

Issue ID: B056Title: Geology and Geochronology of the Guichon Creek BatholithAuthor(s): Northcote, K.E.Series Name: BulletinPublication Year: 1969NTS Map Sheet(s): 092I/6,11Place Keyword(s): British Columbia, Guichon CreekLat/Long (NSWE): 50.369, 50.159, -121.369, -120.687Theme Keyword(s): Geology, Geochronology, Bedrock GeologyDownload(s):
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Bulletin 56 describes the geology and geochronology of the Guichon Creek area. Mapping is done at the one inch to two mile scale. See also Bulletin 62 and Preliminary Map 30 for more information. Issue ID: B057Title: The Jordan River Area near Revelstoke, British Columbia (A Preliminary Study of Lead-Zinc Deposits in the Shuswap Metamorphic Complex)Author(s): Fyles, J.T.Series Name: BulletinPublication Year: 1970Scale: 1:24000NTS Map Sheet(s): 082M/1,2Place Keyword(s): British Columbia, Revelstoke, Jordan RiverLat/Long (NSWE): 51.8, 51.05, -118.93, -118.26Theme Keyword(s): Geology, Lead-zinc Deposits, Bedrock GeologyDownload(s):
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Bulletin 57 describes the structure and lithology of rocks associated with conformable lead-zinc deposits in the Shuswap Metamorphic Complex northwest of Revelstoke, British Columbia. This type of deposit contains large reserves of lead and zinc, but, to date, none of the deposits has been mined. The most important properties include the Big Ledge northwest of Nakusp, the Wigwam 20 miles southeast of Revelstoke, the Cottonbelt 30 miles northwest of Revelstoke, the Ruddock Creek property 60 miles north of Revelstoke, and the King Fissure in the Jordan River area. The Jordan River area is about 15 miles northwest of Revelstoke on the southeastern flank of the Frenchman Cap gneiss dome. Rocks within the area include quartzite, mica schist, quartz-feldspar, and calc-silicate gneiss, and minor amounts of marble in the amphibolite facies of regional metamorphism. The lithological succession is given in Table I, page 14. Nepheline-syenite gneiss and syenite gneiss form concordant layers within calc-�silicate gneiss. Granitic gneiss intrudes the metasedimentary rocks and undeformed lamprophyre dykes follow a system of northerly trending fractures. Granitic gneiss of uncertain origin forming the core of the Frenchman Cap dome occurs along the northern edge of the area. Schist, quartzite and paragneiss lie above the granitic gneiss, and these metasedimentary rocks contain the lead-zinc deposits. Rocks of the Jordan River area are complexly folded. Three phases of deformation are recognized. The oldest or Phase 1 folds are isoclinal, recumbent, similar folds with warped axial planes and axes which plunge at various angles dominantly to the southwest, west, and east. Phase 2 folds are overturned with axial planes dipping southwest and south. The style and plunge of the folds varies in relation to the position of the folds on the curving flank of the Frenchman Cap dome. A broad curvature of the foliation around the southeastern corner of the dome is referred to as a Phase 3 fold. The lead-zinc layer and the nepheline-syenite gneiss have been deformed by all three phases of folding. The lead-zinc sulphide layer occurs in a group of rocks known as the lead-zinc sequence, which consists of a quartzitic part lying structurally beneath a cal�careous part. The calcareous part contains mica schist, calcareous mica schist, calc-silicate gneiss, and at least three distinct layers of marble, each a few feet thick. The sulphide layer is a few tens of feet from the quartzitic part of the sequence. It is very closely confined stratigraphically; it ranges from less than an inch to 25 feet thick but is normally less than 10 feet thick. It consists of fine-grained pyrrhotite, sphalerite, galena, and pyrite with lenses of quartz and locally barite and marble in a calc-silicate gneiss. The sulphide layer occurs on the King Fissure property where reserves arc estimated to be more than 3 million tons having an average grade of approxi�mately 1 ounce per ton silver, 5 per cent lead, and 5 per cent zinc. The layer is also present on the eastern slope of Frisby Ridge, where it is less than 1 foot thick. Molybdenite associated with syenite gneiss and syenite pegmatite is found near the margins of a mass of nepheline-syenite gneiss west of the King Fissure property. This molybdenite is currently being mined. The Ruddock Creek area, 60 miles north of Revelstoke, is on the northwestern flank of the Frenchman Cap dome. Rocks in the area are mica schist, sillimanite, and calc-silicate schist and gneiss with intercalated layers of marble. These rocks form highly folded discontinuous layers and lenses engulfed in granite-pegmatite. The dominant folds in The Ruddock Creek area plunge 20 to 30 degrees to the west and are of two ages. The later or Phase 2 folds are recumbent, having rounded hinges and a modified concentric style varying from sub-isoclinal in the east to relatively open in the west. One older, or Phase I fold, has been mapped with axis almost parallel to the axes of the Phase 2 folds. This fold described as a syncline is shown diagrammatically on Figure 8, page 49. The sulphide member on the Ruddock Creek property consists of calc�-silicate gneiss, quartzite, marble, and sulphides, and ranges from 5 to 15 feet thick without structural repetitions. At the main (E) showing it is repeated by folding and is more than twice this thickness. The sulphide layers contain sphalerite, pyrrhotite, galena, pyrite, and minor chalcopyrite with quartz, calcite, and locally barite and fluorite. Much of the sulphide layer is very fine grained and contains rounded knots of quartz. Other mineralization is medium grained and massive. The deposit is estimated to contain several million tons of material grading approximately 10 percent combined lead and zinc and less than 1 ounce per ton silver. The conformable lead-zinc deposits in the Shuswap Metamorphic Com�plex have several parallel and some contrasting features. They arc closely confined stratigraphically, but are not in the same lithological succession and probably not in the same time-stratigraphic unit. The mineralogy, textures of the sulphides, and mineral associations are similar at all the deposits. All the deposits have been deformed and metamorphosed. Locally they are replaced by pegmatite.

Issue ID: B058Title: Geology and Mineral Deposits of the Stewart Area, British ColumbiaAuthor(s): Grove, E.W.Series Name: BulletinPublication Year: 1971Scale: 1:31680NTS Map Sheet(s): 103O/16; 103P/13; 104A/4; 104B/1Place Keyword(s): British Columbia, Northwestern British Columbia, Stewart, Boundary RangesLat/Long (NSWE): 56.255, 55.802, -130.143, -129.827Theme Keyword(s): Geology, Bedrock GeologyDownload(s):
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Bulletin 58 describes the Stewart map area, one of the major metal-mining districts in western Canada, which is located 100 miles north of Prince Rupert, and covers an area of about 220 square miles in the Boundary Ranges in northwestern British Columbia. It lies within a terrain of Mesozoic rocks across the contact between plutonic rocks of the Coast Crystalline Belt and the west-central portion of the Bowser Basin. The purpose of this study was to determine the lithological and structural relationships of these rocks to the younger mineral deposits and to obtain background information essential to the study of the Stewart Complex. The oldest Mesozoic rocks in the district are non-marine Hazelton volcanic epiclastics and sedimentary strata that constitute part of a thick-layered Lower Jurassic succession. This succession is overlain by predominantly marine sedimentary Bowser strata of Middle to Upper Jurassic age. The two assemblages are separated by lower Bowser rhyolite flows, limestones, littoral materials, and red beds that mark the onset of basin subsidence and rapid, dominantly marine sedimentation. A variety of intrusive rocks comprising part of the Coast Crystalline Belt cut all the layered rocks of the district. Individual plutons range in composition from augite diorite to quartz monzonite and in size from discrete dykes and stocks to extensive batholiths. Plutons of the Coast Crystalline Belt have been shown to represent at least two episodes of intrusion in the Stewart area. One is represented by the Mesozoic Texas Creek granodiorite and the second by the Tertiary Ryder quartz monzonite. The dyke swarms, which have been divided into four textural and compositional groups, represent the latest phases of igneous activity in the area. The Mesozoic rocks are folded along arcuate northerly trending nearly horizontal axes. The major fold involving Hazelton rocks is an upright, broad anticline upon which Bowser rocks are preserved as structural remnants. The major fold in the Bowser rocks is an upright, canoe-shaped syncline that bisects the map area. The majority of minor folds and the cogenetic lineations in the Hazelton rocks are nearly at right angles to the major structure. Minor folds in the Bowser rocks include styles varying from simple to complex or confused, which express deformation resulting from gravity sliding and from extensive igneous intrusion. Cataclasites form extensive northerly trending zones cutting Hazelton volcanic epiclastics. The major Cascade Creek zone has been intruded and altered by igneous material and extensively mineralized. Numerous extensive fractures which cut all the country rocks and major structures have been grouped into four major systems along which most of the known vein deposits have been localized. The mechanical competency of the lithologic units has been examined in terms of structural studies and certain volcanic conglomerates have been shown most favourable to deformation, alteration, and mineralization. More than 50 properties in the Stewart district produced in excess of 5.6 million tons of gold-silver-lead-zinc ore between 1910 and 1968. Of this total the Silbak Premier mine alone produced over 4.7 million tons and paid in excess of $21 million in dividends. In addition there are at least 100 more known mineral deposits that have not been mined. The mineral deposits are mainly simple quartz-breccia veins and transitional vein-replacement systems, which contain irregular lenses and shoots of sulphide mineralization. The primary sulphide minerals are pyrite, galena, and sphalerite, with accessory gold and silver minerals. Native silver, electrum, and gold are locally important and contributed significantly to mine production. The veins and vein systems form three well-defined groups related to well-defined fracture systems in both Hazelton and Bowser rocks. Wallrock alteration related to the mineral deposits includes simple silicification, carbonatization, and pyritization, as well as examples of propylitization, hornblendization, and potassium feldspar alteration. Country rock alteration patterns are generally simple and relate to igneous intrusion and low-grade deformation coupled with crystalloblastesis, as well as to the mechanical nature of the materials involved. Variable induration, silicification, pyritization, hornblendization, and potassium feldspar alteration are common contact and shear-zone effects. Evidence for regional metamorphism is slight and consists of rare, sporadic fine-grained andalusite developed in certain Bowser siltstone units, as well as extensive medium-grained hornblende developed in Hazelton volcanic conglomerates spatially unrelated to known or visible plutons. This suggests a lower amphibolite facies environment but may imply selective metasomatism. This study of the Stewart area has revealed in part the complex interplay between elements of the Coast Crystalline Belt and the Bowser Basin and the relationship of mineral deposits to specific structural and lithological situations in that environment.

Issue ID: B059Title: Geology of Copper MountainAuthor(s): Preto, V.A.Series Name: BulletinPublication Year: 1972Scale: 1:12000NTS Map Sheet(s): 092H/7,8Place Keyword(s): British Columbia, Princeton, Copper Mountain, Southcentral British ColumbiaLat/Long (NSWE): 49.374, 49.259, -120.589, -120.455Theme Keyword(s): Geology, Structure, Stratigraphy, Bedrock GeologyDownload(s):
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Bulletin 59 describes the geology of a 50-square-mile area centered on Copper Mountain, 10 miles south of Princeton, British Columbia. Particular attention is paid to the structure, stratigraphy, and alteration of volcanic and sedimentary rocks of the Nicola Group, to the Copper Mountain intrusions, which cut them, and to the setting of copper deposits in this environment. Nicola Group rocks consist of a volcanic succession that includes massive flow units, coarse to very fine-grained pyroclastic units and some pillow lava, and of a sedimentary succession that includes siltstone, argillite, conglomerate, and some reefoid limestone. The volcanic rocks are generally andesite to basaltic andesite in composition. Their age, as indicated by fossils, is Upper Triassic. The Copper Mountain intrusions cut the Nicola rocks and consist of a series of differentiated quartz-poor calc-alkalic rocks that range in composition from pyroxenite to syenite. These intrusions include the Copper Mountain, Smelter Lake, and Voigt stocks and the Lost Horse intrusions, and have been dated radiometrically at 193�6 million years. Copper deposits are found near Copper Mountain in a narrow belt of strongly altered and fractured Nicola rocks that is bounded on the south by the Copper Mountain stock and on the north by the Lost Horse intrusions. Mineralization is controlled by faulting and fracturing, suitable alteration, and, in most cases, by the proximity of rocks of the Lost Horse intrusions, which appear to have been the immediate source of hydrothermal and mineralizing fluids. The copper deposits are regarded by some as being pyrometasomatic, and by others as being partly skarns (Ingerbelle) and partly complex porphyry copper gold deposits (Copper Mountain). Typical rock alteration includes an early development of biotite followed by extensive albite-epidote replacement and later veining by potash feldspar and scapolite. Post-mineral intrusions include a quartz monzonite mass that has been radiometrically dated at 99.5�4 million years and a later swarm of northerly trending felsitic dykes. Middle Eocene sedimentary, volcanic, and intrusive rocks of the Princeton Group unconformably overlie and cut all the previously mentioned rock units. Deformation in the area consisted of mostly broad northerly to northwesterly trending folds, and intense faulting. At Copper Mountain faults may be separated into distinct sets which, in order of decreasing relative age, trend east-west, northwest, and northeast. Later northerly trending normal faults dissected the area and divided it into two distinct blocks, the western of which has been down dropped and appears to be devoid of intrusive rocks of the Copper Mountain type at the present level of erosion. Particular attention is paid to the structure, stratigraphy, and alteration of volcanic and sedimentary rocks of the Nicola Group, to the Copper Mountain intrusions, which cut them, and to the setting of copper deposits in this environment. Nicola Group rocks consist of a volcanic succession that includes massive flow units, coarse to very fine-grained pyroclastic units and some pillow lava, and of a sedimentary succession that includes siltstone, argillite, conglomerate, and some reefoid limestone. The volcanic rocks are generally andesite to basaltic andesite in composition. Their age, as indicated by fossils, is Upper Triassic. The Copper Mountain intrusions cut the Nicola rocks and consist of a series of differentiated quartz-poor calc-alkalic rocks that range in composition from pyroxenite to syenite. These intrusions include the Copper Mountain, Smelter Lake, and Voigt stocks and the Lost Horse intrusions, and have been dated radiometrically at 193�6 million years. Copper deposits are found near Copper Mountain in a narrow belt of strongly altered and fractured Nicola rocks that is bounded on the south by the Copper Mountain stock and on the north by the Lost Horse intrusions. Mineralization is controlled by faulting and fracturing, suitable alteration, and, in most cases, by the proximity of rocks of the Lost Horse intrusions, which appear to have been the immediate source of hydrothermal and mineralizing fluids. The copper deposits are regarded by some as being pyrometasomatic, and by others as being partly skarns (Ingerbelle) and partly complex porphyry copper gold deposits (Copper Mountain), Typical rock alteration includes an early development of biotite followed by extensive albite-epidote replacement and later veining by potash feldspar and scapolite. Post-mineral intrusions include a quartz monzonite mass that has been radiometrically dated at 99.5�4 million years and a later swarm of northerly trending felsitic dykes. Middle Eocene sedimentary, volcanic, and intrusive rocks of the Princeton Group unconformably overlie and cut all the previously mentioned rock units. Deformation in the area consisted of mostly broad northerly to northwesterly trending folds, and intense faulting. At Copper Mountain faults may be separated into distinct sets which, in order of decreasing relative age, trend east-west, northwest, and northeast. Later northerly trending normal faults dissected the area and divided it into two distinct blocks, the western of which has been down dropped and appears to be devoid of intrusive rocks of the Copper Mountain type at the present level of erosion.

Issue ID: B060Title: Geology of the Akolkolex River AreaAuthor(s): Thompson, R.I.Series Name: BulletinPublication Year: 1979Scale: 1:48280NTS Map Sheet(s): 082K/13; 082L/16; 082M/1; 082N/4Place Keyword(s): British Columbia, Selkirk Mountains, Kootenay Arc, Akolkolex RiverLat/Long (NSWE): 51.025, 50.82, -118.167, -117.83Theme Keyword(s): Geology, Structure, Lead-zinc-silver Deposits, Bedrock GeologyDownload(s):
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Bulletin 60 reports the structural history and exploration potential for lead-zinc-silver mineral deposit in the Akolkolex River area, which encompasses approximately 200 square miles on the western margin of the Selkirk Mountains of British Columbia. It forms the northwestern limit of the Kootenay Arc, a narrow arcuate belt of severely deformed sedimentary and volcanic rocks, and is part of the structural-metamorphic transition between the Shuswap Metamorphic Complex to the west and the Selkirk Mountain Fold and Thrust Belt to the east. Two structural levels are evident in the Akolkolex River area. They are separated by the Standfast Creek fault, a low-angle fault that cuts obliquely upward through the stratigraphic succession from southwest to northeast. The upper structural level contains quartzite1 calcareous phyllite, limestone, and carbonaceous phyllite and argillite of Early Paleozoic age that can be regionally correlated with the Hamill Group, Mohican Formation, Badshot Formation, and Index Formation of the Lardeau Group respectively. This succession has been deformed into a pair of large recumbent folds: the Akolkolex anticline and the Drimmie Creek syncline. These nappe-like structures have an amplitude approaching 4 miles, have a relatively constant interlimb thickness of 2,500 feet or less, and occupy approximately 40 per cent of the area mapped. They are nearly cylindrical in form and plunge gently in a southeasterly direction. The lower structural level contains quartzite and pelitic schist, which appear to be part of the Hamill Group and possibly part of the Horsethief Creek Group of Hadrynian age. Individual structures are difficult to define due to the lack of distinctive stratigraphic markers; however, a large recumbent fold, like that in the upper structural level, is inferred from structural and stratigraphic data. Granodioritic gneiss. Which forms a nearly conformable subhorizontal limit to the stratigraphic succession established in the map area, contains local tightly appressed infolds of the overlying metasedimentary rocks. Folds are cylindrical throughout the map area, and a statistical analysis of the orientation of fold axes shows a pervasive southwesterly trend and low plunge which changes progressively to a west-northwesterly trend in the northwestern part of the area. Although the map area is on the southern flank of the Clachnacudainn salient, a domal culmination of high regional metamorphic grade, fold orientation, and style appear little influenced by it. Metamorphic grade increases from chlorite-bearing phyllites in the upper structural level, to staurolite and kyanite-bearing schists close to the gneiss. A large temperature interval at pressures above the alumino-silicate triple point is indicated. Synkinematic metamorphic textures are present throughout much of the lower structural level. Lead-zinc mineralization in the area is restricted to the thickened hinge zone of the Drimmie Creek syncline. Most mineral showings are on the Wigwam property, located on the north slope of the Akolkolex River. Pyrrhotite, pyrite, galena, and dark brown sphalerite occur as lenses in close association with fine-grained silicified zones within the limestone. Severe folding and local attenuation obscure definition of the lateral extent of the sulphide mineralization. The main structures of the Akolkolex River area appear to be the result of vertical shortening and horizontal extension, like those in the Shuswap Complex, and are in contrast with the upright folding and high-angle faulting of the Selkirk Mountains and Kootenay Arc; however, the grade of regional metamorphism is typical of that in the Selkirk Mountains. Deformation at a deeper structural level may account for the contrast in structural style with adjacent areas to the east and south.

Issue ID: B061Title: Geology of the White Lake BasinAuthor(s): Church, B.N.Series Name: BulletinPublication Year: 1973Scale: 1:50000NTS Map Sheet(s): 082E/05Place Keyword(s): British Columbia, White Lake BasinLat/Long (NSWE): 49.387, 49.273, -119.8, -119.525Theme Keyword(s): Geology, Bedrock GeologyDownload(s):
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Bulletin 61 describes the volcanic geology of the White Lake basin. The object of this study was to establish the stratigraphy, structure, and petrology of Early Tertiary rocks in the White Lake area near Penticton, British Columbia. This was achieved by field mapping and laboratory work performed mainly as a thesis study for the Department of Geology, University of British Columbia. Early Tertiary rocks of the White Lake area consist of five main stratigraphic subdivisions, which are from the base as follows: 1. discontinuous beds of basal breccia and conglomerate, 2. a thick and widely distributed succession of volcanic rocks of diverse composition - mainly phonolite, trachyte, and andesite lavas, 3. discontinuous volcanic beds - mainly rhyodacite lava, 4. locally thick volcanic sandstone and conglomerate beds interdigitated with lahar and pyroclastic deposits, 5. local deposits of slide breccia and some volcanic rock overlain by fanglomerate beds. The maximum aggregate thickness of the sequence is about 12,000 feet, and it is all believed to be of Eocene age. Each subdivision rests with some angular or erosional unconformity on older rock. The preservation of the sequence from erosion is partially explained by regional downfaulting. The greatest downward movement is near the Okanagan Valley where it is estimated that basal beds locally exceed depths of 5,000 feet below mean sea level. In general, beds are tilted easterly as if rotated downward forming a trap-door-like structure. Locally, folds are developed but these are without regional pattern and may be the result of simple flexures in the basement rocks. Petrographic and chemical data indicate a three-fold division of igneous rocks: 'A' series - mainly plagioclase porphyries; lavas of rhyodacite and andesite composition. 'B' series - mainly two-feldspar porphyries with co-existing plagioclase and sanidine; lavas of trachyte and composition. 'C' series - mainly an orthoclase porphyries; lavas of phonolite composition and some tephrite. Phase diagrams and subtraction plots indicate that 'A' and 'C' series rocks were probably formed by crystal fractionation. In the case of 'A' series, precipitation of mainly plagioclase and pyroxene from andesite produces rhyolite; and for 'C' series, precipitation of mainly pyroxene and some biotite from tephrite produces phonolite. Rocks of 'B' series are intermediate in composition to 'A' and 'C' and were probably formed by mixing of magmas. The Dusty Mac gold-silver prospect is the main mineral deposit in the area. A detailed investigation shows that mineralization of the White Lake Formation near Okanagan Falls accompanied a pulse of silicification prior to a period of movement and brecciation on faults and shear zones. Study of the volcanic rocks of the White Lake Basin leads to consideration of general problems of classification of volcanic rocks, particularly fine-grained rocks, and hence a new classification scheme is presented.

Issue ID: B062Title: Gravity, Magnetics, and Geology of the Guichon Creek BatholithAuthor(s): Ager, C.A., McMillan, W.J., Ulrych, T.J.Series Name: BulletinPublication Year: 1972NTS Map Sheet(s): 082; 092Place Keyword(s): British Columbia, Southcentral British Columbia, Guichon Creek BatholithLat/Long (NSWE): 50.667, 50.167, -121.333, -120.667Theme Keyword(s): Geology, Gravity SurveyDownload(s):
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Bulletin 62 summarizes the results of a detailed gravity survey of the metal-rich Guichon Creek batholith in south-central British Columbia. Gravity measurements were taken at half mile intervals along three lines across the batholith. Elevation control was provided by triple leveling the lines. Density terms used in the interpretation were derived from nearly 1500 specific gravity measurements made on rock samples collected throughout the batholith. From the data, the three dimensional geometry of the batholith was interpreted. Gravity anomalies are located at the coordinates of the observation station. They are not reduced to any datum, but have been corrected for effects down to a datum. It is therefore clear that the anomaly values are located on an irregular surface, and any mathematical treatment of the data must consider this point. This is of special importance in mountainous regions. The use of linear filter operators on potential fields greatly enhances the interpretation of the data and provides a useful means of anomaly separation. This is most clearly evident on the filtered magnetic map where regional magnetic features are highly resolved. Another use of filtering is to define the second vertical derivative gravity map from which the configuration of the boundary of the source may be inferred. In particular, the second derivative map suggests that the batholith terminates with a vertical contact to the north, where it underlies the Kamloops volcanic rocks. On the basis of the gravity and density data, only two subdivisions of the batholith can be made: (1) The Hybrid phase and country rock, and (2) The Highland Valley, Bethlehem, and Bethsaida phases. An estimate of the average depth of the Tertiary Kamloops volcanic rocks overlying the north edge of the batholith was made from the regional ?g map. Using ? = 2.60 gm/cm3, a depth of 1.0 kilometre was determined. Interpretation of the gravity data led to a density model for the batholith. Its gross shape can be likened to that of a flattened funnel-like structure. The axis of symmetry for the model is tilted about 10 degrees from the vertical and plunges in an east-northeast direction. The maximum depth of the central core is more than 12 kilometres. Probably the most important result of this study in terms of mineral exploration is the striking correlation between the locations of large-scale porphyry copper-molybdenum deposits, such as the Highmont, JA, Lornex and Valley Copper deposits, and the surface projection of the interpreted root zone of the batholith. Issue ID: B063Title: Geology and Mineral Deposits of the Unuk River-Salmon River- Anyox AreaAuthor(s): Grove, E.W.Series Name: BulletinPublication Year: 1986Scale: 1:100000NTS Map Sheet(s): 103O/8,9,16; 103P/5,6,11,12,13,14; 104A/3,4,5; 1104B/1,7,8,9,10Place Keyword(s): British Columbia, Northwestern British Columbia, Unuk River, Salmon River, Anyox RegionLat/Long (NSWE): 56.75, 55.25, -130.75, -129.25Theme Keyword(s): Geology, Tectonic Evolution, Metallogenesis, Bedrock GeologyDownload(s):
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Bulletin 63 represents new data on the geology of the Unuk River-Salmon River-Anyox region, much of which is relevant to the tectonic evolution of the Western Cordillera and to the concepts of metallogenesis in northwestern British Columbia. The study area includes part of the contact of the eastern Coast Plutonic Complex with the west-central margin of the successor Bowser Basin. Sedimentary, volcanic, and metamorphic rocks bordering the Coast Plutonic Complex range in age from Paleozoic to Quaternary. Geologically, geographically, and economically the country rocks of the area form a well-defined entity that the writer has called the Stewart Complex. Mineral exploration in the area is for vein, massive sulphide and porphyry deposits. The most important metals sought are gold, silver, lead, zinc, copper and molybdenum.. Several distinct periods of metamorphism, plutonism, volcanism, and sedimentation marked by deformation and erosion have been identified. The intensity of deformation has apparently decreased since the mid-Triassic Tahltanian orogeny although plutonism has increased in activity since the Triassic and reached a climax in the Tertiary along the eastern margin of the Coast Plutonic Complex. Neogene volcanic activity marked by alkali olivine basalt flows has occurred periodically along major north-south, north-easterly, and east-west fractures. Within this orogenic cycle metallogenesis is related to volcanic, sedimentary, and plutonic processes during each major tectonic phase, and these processes have combined to produce broad mineral zoning and a large array of mineral deposits that characterize this portion of the Western Cordillera. The numerous fissure vein and replacement vein deposits in the Stewart Complex, including the Silbak Premier mine, comprise a common group of simple ore and gangue minerals. The major massive sulphide deposits include the Granduc property at Granduc Mountain, and the Hidden Creek, Double Ed, Redwing, and Bonanza properties at Anyox. Porphyry deposits include the molybdenum deposit at Kitsault and the copper-molybdenum property at the Mitchell-Sulphurets Creeks.

Issue ID: B064Title: Porphyry Copper and Molybdenum Deposits, West-central British ColumbiaAuthor(s): Carter, N.C.Series Name: BulletinPublication Year: 1981Scale: 1:3000000NTS Map Sheet(s): 093E;093L;093M;103H;103I;103PPlace Keyword(s): British Columbia, West central British ColumbiaLat/Long (NSWE): 56, 53, -130.25, -124.75Theme Keyword(s): Geology, Porphyry Copper, Molybdenum DepositsDownload(s):
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Bulletin 64 describes porphyry copper and molybdenum deposits in west-central British Columbia that are associated with plutons of Late Cretaceous and Tertiary age that intrude Mesozoic volcanic and sedimentary rocks of the Intermontane Tectonic Belt. The porphyry deposits are contained in an area bounded on the west by granitic rocks of the Coast Plutonic Complex, and on the east and southeast by a belt containing Mesozoic granitic stocks and an extensive area of Tertiary volcanic rocks. The porphyry intrusions take the form of small stocks, plugs, dykes, and dyke swarms generally not exceeding 1 square mile in surface area. The intrusions are commonly multiple and range in composition from quartz diorite to granite. Copper and molybdenum sulphides occur as fracture fillings and as veinlet stockworks within and adjacent to the intrusive bodies. Sulphide and alteration minerals exhibit concentric zoning patterns. Volcanic and sedimentary rocks marginal to the intrusions are thermally metamorphosed to biotite hornfels. These intrusive contacts, mineralized fractures, alteration patterns and contact metamorphism provide important mineral exploration guidelines. Results of potassium-argon dating indicate four crudely parallel north to northwest-trending belts of porphyry intrusions, each being distinctive in age, rock composition, and contained metallic mineralization. From west to east these include: (1) Alice Arm intrusions - 50 m.y. molybdenum-bearing quartz monzonite and granite intrusions; (2) Bulkley intrusions - 70 to 84 m.y. copper-molybdenum and molybdenum-bearing porphyries of granodiorite to quartz monzonite composition; (3) Nanika intrusions - 50 m.y. copper-molybdenum and molybdenum-bearing intrusions of quartz monzonite composition; (4) Babine intrusions - 50 m.y. copper-bearing intrusions of quartz diorite and granodiorite composition. Potassium-argon analyses were carried out mainly on biotite separates from the mineralized porphyry phases within the deposits. Dating of intermineral and post mineral porphyry phases, common at many of the deposits, yielded ages equivalent to, or 2 to 3 m.y. younger than, the mineralized phases, indicating that the age of mineralization is essentially synchronous with the age of intrusion. Limits of analytical errors in these potassium-argon analyses are within 3 per cent of the calculated ages. The distribution of potassium-argon ages for porphyry deposits in west-central British Columbia does not fit well the plate tectonic theories proposed for the origin of similar deposits elsewhere in the Cordillera of North and South America, in which deposits are progressively younger in a given direction Here, four crudely parallel belts of porphyry intrusions display a reversal in age from 50 m.y. to 70-64 m.y. to 50 m.y. in an eastward direction. This distribution of ages may have been caused by periodic movement from Late Jurassic to Tertiary time along a subduction zone beneath the Coast Plutonic Complex that forms the west border of the area containing the porphyry deposits, Issue ID: B065Title: Surficial geology and sand and gravel deposits of Sunshine Coast, Powell River and Campbell River areasAuthor(s): McCammon, J.W.Series Name: BulletinPublication Year: 1977Scale: 1:1000NTS Map Sheet(s): 092F/09; 092F/15; 092F/16; 092G/05; 092G/06; 092G/11; 092G/12; 092K/03Place Keyword(s): British Columbia, Southwestern British Columbia, Sunshine Coast, Powell River, Campbell RiverLat/Long (NSWE): 50.15, 49.384, -125.45, -123.47Theme Keyword(s): Surficial Geology Map, Surficial Geology, Sand Deposits, Gravel DepositsDownload(s):
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Bulletin 65 describes the surficial geology and sand and gravel deposits on the Sunshine Coast, Powell River, and Campbell River areas. Mapping is done at the 1 to 1000 scale. Due to the decline in available supplies of sand and gravel in the Vancouver area and increasing demand, recently there has been considerable interest in possible new sources of these materials. The Geological Survey of Canada has published various maps and bulletins that provide information on much of the Georgia Strait region but not for the Sunshine Coast from Howe Sound to Lund not for the area north of Campbell River. Accordingly, a program to map these areas was initiated in 1974 and completed in 1975. The results of the survey are presented in this bulletin in three sections: Sunshine Coast area, Powell River area, and Campbell River area. In the Sunshine coast area, the survey reviewed only the area below 300 metres elevation. Unconsolidated materials are of glacial, glaciomarine, marine and fluvial origin. Postglacial sea level was at least 180 metres above the present level. Of the 35 gravel pits examined, one is in glaciofluvial material, six are in pre-Vachon beds and the rest are in Capilano fluvial sands and gravels. The survey indicates that most of the gravel sources in this area are being exploited. The major undeveloped source is the delta complex at the mouth of Chapman Creek. In the Powell River area, the same survey strategy was followed. A variety of unconsolidated materials left by glaciers, streams and the sea mantle the area. Most pits in the area are small. In the 38 examined, sand is more abundant than gravel. In the east, the aggregates are in Capilano fluvial deposits, in the west they are in pre-Vachon materials. It is unlikely that large undiscovered deposits occur in the area surveyed; good gravel deposits are scarce but sand is abundant. In the Campbell River area, the survey area is within the Nanaimo Lowland. The highest point of land is at 319 metres. Glaciers moved southeast and left a mixed variety of debris, normally till above 189 metres elevation. Below 180 metres, the ground is covered with unconsolidated glacial, glaciomarine, marine and fluvial deposits. The study examined 35 pits. Twelve of these, including the largest, are in the large glaciofluvial delta east of McIvor Lake. The largest apparent concentration of gravel in the area surveyed is in the glaciofluvial delta across the east end of Campbell Lake.