Download Geology and Mineral Resources: Kamloops-Cache Creek

 Geology and Mineral Resources: Kamloops‐Cache Creek‐Pavilion Lake Field Trip • Regional Geology (BC Ministry of Energy, Mines & Petroleum Resources) Bruce Madu, Regional Geologist: Field Trip Leader • Pavilion Quarry and Lime Plant (Graymont Western Canada) Al Lucas, Plant Manager • Decor Quarry (Pacific Bentonite) John Dormer, Operator •McAbee Fossil Beds Dave Langevin (Proprietor) and John Leahy Aerial view toward Cache Creek from Pavilion Quarry Sponsored and Co‐ordinated by: MineralsEd Eric Rustand, MineralsEd partner‐teacher, Norkam Secondary, Kamloops GEOLOGIC TIME SCALE Modified from Armstrong, 1990 Introduction Geology greatly influences everything that human kind does – where we build homes and cities, where we farm and ranch, where we log, and where we mine. This geological field trip from Kamloops through Cache Creek to Pavilion Lake traverses a unique assemblage of rocks that make up the Intermontane Belt of the Cordilleran Orogen in BC (Map 1, folded). These rocks record ancient volcanism, plutonism, sedimentation, deformation and glaciation. Although they seem like they “belong here”, most do not and instead have been added to the continent by tectonic processes. The geologic history is interesting and complex, and it determines the variety and distribution of mineral resources here in this area – and everywhere else in BC and around the world. Background Information Canadian Cordilleran British Columbia lies in the Cordilleran Orogen (kord‐(y)‐air‐uhn or‐uh‐jen), a mountain belt that runs along the western edge of the continents from Alaska to Antarctica. These mountains formed over tens of millions of years as a result of tectonic collisions between the continents and crustal plates located in what is now the Pacific Ocean basin. The crustal plates included slivers (terranes) of volcanic islands, ocean floor and other small continents that collided with and remained stuck onto (accreted) the margins of the continents. These mountain‐
building collisions were marked by igneous intrusions and volcanism, deformation (folding, faulting, and metamorphism) and uplift. In British Columbia the Canadian Cordillera is made up of five, northwest‐
trending morphogeological belts: Foreland, Omineca, Intermontane, Coastal and Insular (Figure 1). They are defined by their distinct geology and the mountain‐building processes that formed them, and are separated from each other by faults. Geoscientists have determined that the rocks in the Foreland belt formed along the edge of ancient North America. However, rocks forming the belts further west formed elsewhere and were accreted to the continent between 185 and 50 million years ago. The unique geological characteristics and mountain‐building history of each belt determine the mineral resources each one contains. • Foreland Belt, represented by the Rocky Mountains, is made up mostly of a great thickness (>15 km) of ancient sedimentary rocks. Most are between 700‐
50 million years old, but some are up to 1.5 billion years old. They are composed of sediment that was eroded from and deposited along the western edge of the ancient continent. During mountain building they were thrust eastwards for at least 150 km onto the continent. • Omineca Belt, represented by several northwest‐trending mountain ranges, Figure 1 – Canadian Cordilleran is made up mostly of folded and faulted metamorphic rocks with lesser morphogeological belts (From Price, amounts of granitic rock. Most of these metamorphic rocks formed from Monger, and Roddick, 1991, in pre‐existing sedimentary rocks. Some of these are similar in composition to Armstrong, 1991) sedimentary rocks in the Foreland, while others are more similar to those in the Intermontane. This complexly deformed belt represents the exposed roots of a deeply‐eroded mountain chain. It marks a collision zone that formed when the Intermontane was accreted to North America. • Intermontane Belt, a region of high plateaus and rolling uplands, is made of ancient to Recent volcanic and sedimentary rocks that are intruded in many areas by granitic rocks. The oldest of the volcanic and sedimentary sequence (370‐180 million years) represents ocean floor and volcanic island arc terranes that formed offshore and were accreted during middle Jurassic time (165‐172 million years ago). The granitic rocks are related to ancient island arc volcanism and to later accretion of Insular belt rocks. • Coast Belt includes the Coast and Cascade mountains and extends up to the Yukon. It is made up mostly of 185 to 50 million year old granitic rocks, plus scattered remnants of older, deformed sedimentary and volcanic bedrock into which Kamloops‐Cache Creek‐Pavilion‐Decor‐McAbee Field Trip 2007
1
the granitic bodies have intruded. Similar, undeformed sedimentary and volcanic rocks occur in both the Intermontane and Insular belts.) Similar to the Omineca, this belt marks a collision zone. It represents the roots of a deeply‐eroded volcanic mountain chain that formed during accretion of Insular belt rocks to North America. • Insular Belt includes Vancouver Island, the Queen Charlotte Islands, and the bedrock forming the seafloor out to the toe of the continental slope about 100 km west of Vancouver Island. It is made up mostly of ancient (350‐180 million years) volcanic and sedimentary rocks, which are intruded locally by granitic rocks. Like those in the Intermontane, the volcanic and sedimentary rocks represent exotic terranes that formed out in the ocean basin and were accreted to the continent by mid‐Cretaceous time (100‐115 million years ago). Intermontane Belt: Kamloops Area Bedrock The Intermontane Belt in the Kamloops area is composed of three, exotic terranes1 (Cache Creek, Quesnel and Slide Mountain) which are overlain by younger, syn‐ and post‐accretion sedimentary and volcanic rocks (Ashcroft Formation, Kamloops Group, Chilcotin Group) and veneered by very young glacial deposits (Matthews and Monger, 2005; Figure 2). More detailed descriptions of the terranes and overlying sequences in the field trip area are given below. Pleistocene Sediments: (12,000‐1,000,000 years) ‐ Ice‐deposited glacial till, river deposited conglomerates and sands, and silty lake deposit Chilcotin Group: Miocene (6‐10 million years) –flood basalt (do not outcrop on this field trip traverse) Kamloops Group: Eocene (55‐45 million years) ‐ Sequences of volcanic flows and non‐marine sediments that overlie the older (Quesnel) island arc rocks in numerous, isolated fault bounded basins. Volcanics range from basalt to rhyolite and pyroclastics; sedimentary rocks include sandstone, shale, conglomerate, and minor coal. Not well lithified, poorly‐exposed. (McAbee Fossil Beds, Ranchlands ) Ashcroft Formation: (Jurassic (190‐170 million years) ‐ Deformed dark shale and sandstone that locally overlie eroded older (Quesnel) island arc rocks, and are structurally overlain (i.e. fault) by Cache Creek Group limestone. Interpreted as near shore marine, deposited on an uplifted and eroded Quesnel island arc before the Cache Creek accretionary wedge was thrust up onto the land and subduction ceased. Cache Creek: Mid. Pennsylvanian to Mid. Jurassic (300‐
220 million years) ‐ An assemblage of radiolarian chert, argillite, and basaltic volcanics – all interpreted to deep‐marine in origin, plus large masses of limestone (Pavilion Quarry) interpreted to be shallow marine. Similar in age, but different in composition to Quesnel rocks. Interpreted to be a deformed accretionary complex that formed during Quesnel island arc formation. Quesnel: Late Triassic to Early Jurassic (235‐208 million years) – Very wide‐spread sequence of island arc volcanic rocks (flows, breccias, pyroclastics) and interbedded sedimentary rocks (Nicola Group) (Ash Basalt Quarry). Cross‐cut by many dioritic intrusions, many of which are mineralized (Afton Mine; Highland Valley Copper, Craigmont). They unconformably overlie the older (Devonian through Permian) volcaniclastic, argillite, siltstone, and limestone (Harper Ranch Group) (Harper Ranch Quarry) and Slide Mountain terrane. Quesnel: Late Triassic to Early Jurassic (235‐208 Slide Mountain: Early Mississippian to Permian (~350‐270 million years) ‐ Found along the Intermontane ‐ The most widespread part of the Intermontane (Figure 2) Quesnel terrane is Omineca boundary (Figure 2), it is made up of basaltic volcanics, made up of volcanic island arc volcanics coarse clastic sedimentary and interbedded sedimentary rocks (Nicola rocks, argillite, chert and some Group) (Ash Basalt Quarry). Cross‐cut by carbonates. They are many granitic intrusions, many of which interpreted to have formed in a are mineralized (Afton Mine; Highland marginal basin behind the arc Valley Copper, Craigmont). They with influx from both the arc unconformably overlie the older (Devonian and the continent to east. through Permian) volcaniclastic, argillite, siltstone, and limestone (Harper Ranch Group)(Harper Ranch Quarry) and Slide Mountain terrane rocks. million years) Italicized names refer to mineral resource operations hosted by the rocks described in the unit. 1
Terrane: distinct assemblage of rocks (e.g. type, fossil content, ages) that originates in one palaeogeographic location, has been
transported and tectonically emplaced in another location, and is separated from other terranes by faults.
Kamloops‐Cache Creek‐Pavilion‐Decor‐McAbee Field Trip 2007
2
Figure 2 – Geological map of the Intermontane Belt in south central BC (From Mathews and Monger, 2005)
Kamloops‐Cache Creek‐Pavilion‐Decor‐McAbee Field Trip 2007
3
A schematic interpretation showing the settings where the rocks formed and how the Intermontane evolved is shown in Figure 3. Generally, these ancient rocks record of a volcanic island arc (Quesnel) that formed above an E‐dipping subduction zone. On leading edge of the island arc a carbonate shelf formed, but it and other deep water sediments and volcanics offshore became deformed together forming an accretionary wedge of sediments as subduction continued. A marine basin formed behind the arc, receiving sediments from the arc, from the ancient North American continent to the east and its own back ‐arc volcanism. Figure 3 – Schematic interpretation of the evolution of the Intermontane (oldest at the bottom; youngest at the
top. Kamloops Group volcanics and sediments filled Early Tertiary fault basins (From Monger and Price, 2000)
The Intermontane terranes are interpreted to have been accreted to North America about 180 million years ago. After that they formed the western edge of North America upon which younger volcanic arc evolved, and upon which younger, continental (i.e. non‐marine) sequences were deposited. A tectonic regime change from a subduction zone to a transcurrent fault about 50 million years ago is reflected in the onset of extensional faulting that created many small, restricted basins which filled with even younger volcanic flows and sediments (Kamloops Group) (Figure 3d). How do we know the Intermontane rocks “came from away”? Interestingly, the Intermontane rocks bear fossils that are not from “here”, that is they have no counterparts in same‐age, undisputable North American rocks. For example, the carbonates of the Marble Canyon Formation of the Cache Creek Group, which are mostly Middle Permian, are dated by a large marine foraminifera (call a fusilinid ),Yabeina, which is representative of a foreign fauna from a non‐North American part of the ancient Pacific Ocean. They are not only indicative of a warm shallow water environment, but suggest that the carbonates originated 1000‐2000km to the south (i.e. there are more similar fossils in equivalent age rocks in the SW US.) and were put in place at this latitude by long‐distance, transcurrent faulting, much like the movement along the San Andreas fault today. Kamloops‐Cache Creek‐Pavilion‐Decor‐McAbee Field Trip 2007
4
Kamloops‐Pavilion Lake Geologic Travel Log2 A geological map showing the bedrock geology between Kamloops and Pavilion Lake is provided in the back (Map 1). It shows the rock units and major faults, major towns and rivers, the locations of the main stops on this field trip, as well as several other mineral resource operations in the area. This log begins west of Kamloops centre on Hwy 1 where the Trans Canada Highway (TCH) crosses Hwy 5A and Hillside Way. 0 km Hwy 1 crosses Hwy 5A and Hillside Way .2‐6.1 km Roadcuts in massive green to purplish Nicola Group volcanics 5.7 km Hill on south side of Hwy 1 in Iron Mask Batholith (Afton Mine tip is visible), 209‐194 million year old (Late Triassic) granitic intrusion that is coeval with volcanic flows and breccias it intrudes. 6.3 km Underpass below Hwy 5 14.1 km Mill of Afton Mine on south side of Hwy 1 16.2 km Afton waste rock dump on south side of Hwy 1. Afton Mine is in the Iron Mask Batholith. This batholith consists of 4 main granitic intrusions, all of which cross‐cut and are considered coeval with Nicola Group island arc volcanic rocks. (For detailed information see MEMPR MINFILE 092INE023 at http://www.em.gov.bc.ca/Mining/Geolsurv/minfile/.) Afton was a copper, gold, and silver producing open pit mine from 1978‐
1997. During that time Afton produced >232,000,000 kilograms copper, >85,000,000 grams silver, and >14,000,000 grams gold. The mine site has been reclaimed by Teck Cominco (the open pit mine operators) since the mine ceased operation. Mineral exploration resumed on the property in 2004 by two companies, New Gold Inc. which is continuing with exploratory drilling on the site and advancing and exploration tunnel into the underground at the base of the Afton pit, and Abacus Mining and Exploration, and continues today as high metal prices encourage seeking additional resources. 16.9 km Roadcuts in rusty altered edges of Iron Mask Batholith Afton Mine open pit and portal into
underground
25.9 km Nicola Group volcanics on the north side of the Hwy 1 28.3 km Cherry Creek Valley developed above NW‐trending Cherry Creek Fault. To the south mainly granitic rocks 38.8 km HWY 1 Pullout: Nicola Group volcanics East end of outcrop: sedimentary – black to grey argillite and siltstone with small clams (Monotis) which date the rocks at ~205 million years old (Upper Triassic) West end of outcrop: volcanics, volcaniclastic turbidites with slump structures View from parking lot across Kamloops Lake: To west, bluffs of Nicola Group volcaniclastics overlain by (Cretaceous?) chert pebble conglomerate, sandstone and argillite Copper Creek with bright green and red Nicola Group volcanics, overlain to east by massive brownish cliffs of Eocene Kamloops Group 40.1‐41.3 km Nicola Group volcanics 42.8 km Savona Village 44.0‐44.7 km Roadcuts in very coarse, Nicola Group volcanic breccia 46.7 km Bridge crosses CPR tracks 46.9 km Bridge crosses Thompson River (outflow at the end of Kamloops Lake) 2
The road log is compiled from Monger and Price (2000) and Mathews and Monger (2005). Kamloops‐Cache Creek‐Pavilion‐Decor‐McAbee Field Trip 2007
5
49.0 km Cross Deadman River Enormous deposit of sand and gravel were deposited in a delta formed during fluvio‐glacial outflow from the ancestral Deadman River 57.1 km Across the Thompson River to the south quarry in Nicola Group volcanics used for railroad beds. Benches above the quarry are sedimentary rocks of the Ashcroft Formation 62.4‐63.6 km Large road cut in Nicola Group volcanics Guichon Creek Batholith (see Map 1) Large (30 by 50km) granitic body ~200‐210million years old which cross cuts and is considered coeval with Nicola Group volcanics. Same volcanic island arc as, though slightly older intrusion than, the Iron Mask Batholith. High interest due to mineralization: copper, molybdenum, gold. This rock is the host of the Highland Valley Copper mine deposits and others in that valley. 64.0‐64.6 km Nicola Group volcanics dominate exposures from here to East 68.8 km Tertiary volcanics (Kamloops Group) on north side of Hwy 1 ~69.8 km Turn off (north) to McAbee Fossil Beds McAbee Fossil Beds are a 30m thick deposit of siliceous shale that forms part of a 50 million year old (Eocene) sedimentary and volcanic sequence correlated with the Kamloops Group. The shale contains an amazingly abundant and diverse, and beautifully preserved assemblage of plant, fish and insect fossils. The plant fossils and pollen in the shale point to a forested landscape dominated by elm, birch and beech trees, with pines and cyprus also present. Although the sediments and fossils are interpreted to be deposited in quiet water rich in diatoms (which provided the silica in the deposit), it is not clear to palaeontologists whether the water was deep or shallow. See also “An excerpt from The McAbee flora of British Columbia… “ Page 9 Junior paleontolologists at McAbee Fossil Beds
70.2 km View across valley of the Thompson River (to south) with benches formed of late glacial lacustrine (lake) silts , common to many Interior BC valleys, which were deposited in ice‐dammed lakes as the glacier retreated. 71.4 km Columnar jointed Kamloops Group volcanics above north side of road 76.0 km Brownish red cliffs on north side of Hwy 1 are massive volcanic flows the Eocene Kamloops Group 79.1‐81.0 km Recessive hills formed of Jurassic Ashcroft Formation sedimentary rocks and overlain by Eocene Kamloops Group volcanics. The Ashcroft strata post‐date the Nicola volcanics and the uplifted intrusions associated with them, but they also have exotic fossils indicating a more equatorial setting and that the land mass originated much further south. 82.8 km Junction on Hwy 1 and Hwy 97 (Turn North on 97) West side hills behind the village are underlain by Cache Creek Melange. This is the eastern most exposure of the melange in the Intermontane. Road cut exposes the melange just west of the Hwy 1 and 97 junction. The recessive weathering matrix is distinct from the limestone block, the deformed beds of argillite and chert. Note the specks in the chert are radiolarians. This chaos is typical of an accretionary wedge, though some deformation here might be later too. Similar grungy rocks are seen on the west coast of Vancouver Island where a melange related to emplacement of those rocks crops out. 84.1 km White bluffs on east side are early Tertiary rhyolite intrusion 86.6 km Hills to west with out‐sized blocks of chert and limestone in Cache Creek Melange matrix 86.8‐88.4 km Bonaparte village 88.9 km Buff outcrops of conglomerate with granite pebbles, and sandstone correlated with Jurassic Ashcroft Formation Kamloops‐Cache Creek‐Pavilion‐Decor‐McAbee Field Trip 2007
6
93.6‐92.9 km East side of Bonaparte River valley are brown bluffs of Eocene Kamloops Group volcanics, mostly andesite flows interpreted as continental in origin 92.9 km Junction of Hwy 97 with Hwy 99, turn west 94.4 km Bonaparte River 95.4‐97.1 km Road cut in Cache Creek Melange with large blocks of chert and amphibolite Note: the farm road at the East end of the outcrop is the old Cariboo Wagon Road (the ranch buildings include the original hotel) 98.1 km Western most exposure of lumpy, matrix‐rich melange in the Cache Creek terrane 104.9‐106 km Outcrops of terrestrial sandstone and conglomerate, some fossil logs 113.8 km Marble Canyon Formation (Permian) limestone outcrop in the Cache Creek terrane containing huge verbeekinid fusilinds, a type of fossil foraminifera, that indicate that the rocks are not from this area and were deposited in shallow water. 114.2 km Hat Creek Road Junction Hat Creek Graben The Hat Creek Valley occupies a down‐dropped, fault bounded basin that contains a thick sequence of Early Tertiary (Kamloops Group?) sediments, including a 300 m thick, low‐grade coal sequence. The coal contains little bits of amber that are believed to contain the earliest ants and a tropical cockroach (Danner and Orchard, 2000, in Woodsworth et al., 2000). A thorough description of the coal sequence is provided by BCMEMPR Minfile 092INW047 available on line. Décor Quarry Pacific Bentonite’s recently opened Décor Quarry lies in burnt red shale beds overlying the coal which were burned by underground coal fires. Overlain by glacial till, the spontaneous combustion of the coal and burning of the shale is interpreted to be more than 10,000 years ago. This unique deposit is quarried as a source of alumina in cement manufacture and for landscaping rock. 118.4 km Pavilion Quarry and Lime Plant Graymont’s Pavilion operation is Pavilion is a combination limestone quarry and processing plant which produces lime in two unique, rotary kilns which annual produce 235,000 tonnes. The quarry taps into an ancient (Permian‐Triassic) fossiliferous limestone, part of the Cache Creek Group, that formed on the flanks of an oceanic atoll near the equator some 206‐256 million years ago! Lime produced here is used primarily for pulp and paper and mining operation applications. The Pavilion quarry and plant have been in operation 33 years, and presently employ over 40 people. It is located on the Pavilion First Nations Reserve, community members from which make up most of the operation's workforce. Pavilion Quarry and lime plant
128.1 km Pavilion Lake Outcrops on north side of Hwy 97are Cache Creek Group cherty argillite (well‐lithified mud) Pavilion Lake is maximum 65 m deep. It is renowned for unique towering stromatolites (or microbialites) growing
along its bottom. These organo-sedimentary structures are microbial mats which trapped very fine sediment
deposited from suspension. These are of great interest to geoscientists because they are very rarely found in fresh
water environments.
Excerpt from The Pavilion Lake Research Project web site: http://supercritical.civil.ubc.ca/~pavilion/index.php Pavilion Lake is approximately 420km northeast of Vancouver, B.C. The lake is 5.7km long and an average of 0.8 km in width, and is located in Marble Canyon in the interior of British Columbia, Canada (Fig. 1). It is a slightly alkaline, freshwater lake with a maximum‐recorded depth of 65m. Its beautiful clear blue waters (Secchi depths of more than 15m) and microbialite structures have made it a popular destination for recreational and commercial divers particularly over the months of May‐October. Furthermore, the lake falls within the traditional territory of the Ts’kw’aylaxw people, and Kamloops‐Cache Creek‐Pavilion‐Decor‐McAbee Field Trip 2007
7
the Pavilion First Nations Indian Band holds special heritage and spiritual connection to this lake and its surrounding land. As such, the lake was added to the Marble Canyon B.C. Provincial Park system on April 18, 2001 as a means of conserving and managing this biologically and historically important site. The basin walls of Pavilion Lake are lined with microbialite structures that are oriented perpendicularly to the shoreline, and which are found from depths of 5 meters to the bottom of the photic zone (light levels 1% of ambient; approximately 30m depth). These structures are speculated to have begun formation nearly 11,000 years ago, after the glacial retreat of the Cordilleran Ice Sheet. Excerpt from The McAbee flora of British Columbia and its relation to the Early–Middle Eocene Okanagan Highlands flora of the Pacific Northwest (2005) by Richard M. Dillhoff, Estella B. Leopold, and Steven R. Manchester, published in the Canadian Journal of Earth Sciences, Vol. 42, Pages 151–166 “McAbee fossils are preserved as impressions and carbonaceous films in siliceous shale. The shale was deposited as diatomite3 (Mustoe 2005), which has been diagenetically altered. The McAbee fossil beds consist of 30 m of fossiliferous shale within an unnamed formation of the lower to middle Eocene Kamloops Group. The shale beds are capped by flow breccia and sit atop an ash‐flow tuff. Tephra deposits bracketed by fossiliferous layers yielded K–Ar dates of 49 ± 2 and 52 ± 2 Ma from plagioclase and 51 ± 2 Ma from biotite contained within a bentonitic tuff (Ewing 1981). These dates generally support the interpretation of a late Early Eocene age. The determination that McAbee fossils were originally preserved in diatomite likely explains their preservation of fine details. A recent study of Late Eocene fossils from Florissant, Colorado (O’Brien et al. 2002) determined that those fossils were preserved within the diatomaceous component of paired couplets, which represent varves. Using scanning electron microscopy (SEM) studies the authors found evidence that diatom mats trapped floating debris and were deposited with the fossilized organisms, resulting in the preservation of fine detail at that locality. Attempts to investigate McAbee shale for a similar mechanism using SEM techniques have not yielded good results. The recrystallization of silica within the diatomite has resulted in the loss of detail at high‐level magnification. The presence of diatomite also helps to delineate the depositional environment, arguing for deep‐water deposition in a substantial body of water. In modern freshwater depositional settings, diatomite does not form in the presence of significant inputs of terrigenous sediments. Wilson (1980) used the taphonomy of fish, insect, and plant remains to establish depth and distance from shore for deposits at Horsefly and Princeton. Using his construct, McAbee also appears to have been a deep‐water environment based on the fact that fish remains are typically articulated, Dipteran insects are common and typically complete, and angiosperm leaves are abundant. This analysis is not unequivocal, however. The abundant bibionid flies and taxodiaceous remains at McAbee are consistent with near‐
shore deposition in Wilson’s model.” 3
Diatomite is a very fine grained sedimentary rock composed mostly of the tiny, siliceous skeletons of the diatoms. A diatom is a microscopic alga with a silica skeleton. Kamloops‐Cache Creek‐Pavilion‐Decor‐McAbee Field Trip 2007
8
References: Armstrong, John E. (1990) Vancouver Geology: Geological Association of Canada Cordilleran Section, 128 p. Armstrong, R. L., et al., 1991, Geology 335 Field School 1991: UBC Dept. Geological Sciences. Cordilleran geoscience ‐ the five belt framework of the Canadian Cordillera. 2005. Geological Survey of Canada. http://gsc.nrcan.gc.ca/cordgeo/belts_e.php. Danner, W.R. and Orchard, M.J., 2000, Paleontology of the Cache Creek and Quesnellia terranes, southwestern British Columbia, in Woodsworth, G. J., et al., 2000, Guidebook for the Geological Field Trips in southwestern British Columbia and northern Washington: Geological Association of Canada, pp. 117‐173. Dawson, K. M., Panteleyev, A., Sutherland Brown, A. and Woodsworth, G. J. 1991. Regional metallogeny. In Geology of the Cordilleran Orogen in Canada, ed. H. Gabrielse and C. J. Yorath, The Geology of Canada, 4:707‐
768. Geological Survey of Canada. Dillhoff, Richard M., Leopold, Estella B., and Manchester, Steven R. (2005) The McAbee flora of British Columbia and its relation to the Early–Middle Eocene Okanagan Highlands flora of the Pacific Northwest: Can. J. Earth Sci. 42: 151–166. Guidebook for Geological Field Trips in Southwestern British Columbia and Northern Washington, 2000, Geological Association of Canada Cordilleran Section, Mathews, Bill and Monger, Jim (2005) Roadside Geology of Southern British Columbia, Mountain Press Publishing Company, Missoula, MT, 404 pages Monger, J.W.H., and Price, R. A., 2000, A Transect of the Southern Canadian Cordillera from Vancouver to Calgary, Geological Survey of Canada Open File 3902, 170 Pages The MapPlace. 2006. British Columbia http://www.mapplace.ca . Kamloops‐Cache Creek‐Pavilion‐Decor‐McAbee Field Trip 2007
9
Notes: Kamloops‐Cache Creek‐Pavilion‐Decor‐McAbee Field Trip 2007
10