USGS Professional Paper 1697 - Alaska Resources Library

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242 Metallogenesis and Tectonics of the Russian Far East, Alaska, and the Canadian Cordillera margin of Jurassic quartz diorite and younger Cretaceous and early Tertiary granitoid rocks of the Talkeetna Mountains batholith, and also locally in mica schist. The Willow Creek district consists of several mines and many prospects, most in an area about 12.8 km long and 6.2 km wide along southern portion of the Talkeetna Mountains batholith. The mine at the deposit contains several thousand meters of underground workings and produced about 18,400 kg Au from 1909 to 1950. Ore grade ranged from about 17 to 69 g/t Au. Origin of and Tectonic Controls for Talkeetna Mountains Metallogenic Belt Hydrothermal micas from the Gold Bullion and Lucky Shot mines in the Willow Creek district exhibit K-Ar isotopic ages of 66 and 57 Ma, respectively (Madden-McGuire and others, 1989). These ages are interpreted to indicate that gold mineralization in the Talkeetna Mountains metallogenic belt occurred in the Late Cretaceous or early Tertiary. Three different tectonic events might be the cause of mineralization—(1) Late Cretaceous and early Tertiary underthrusting of the Chugach and Prince William accretionary-wedge terranes along the Contact fault in southern Alaska, (2) as favored herein, early Tertiary underthrusting of the spreading Kula Ridge under the southern margin of coastal Alaska (Plafker and others, 1989), and (or) (3) early Tertiary dextral-slip faulting along on the Castle Mountain Fault system. Chugach Mountains Metallogenic Belt of Au Quartz Vein Deposits (Belt CM) Southern Alaska The Chugach Mountains metallogenic belt of Au quartz vein deposits (fig. 103; tables 3, 4) occurs on Kodiak Island, the southeastern Kenai Peninsula, and in the central and eastern Chugach Mountains in southern Alaska. The Au quartz vein deposits occur mainly in the Late Cretaceous flysch of the Valdez Group and Kodiak Formation where these units were metamorphosed to greenschist facies (Goldfarb and others, 1986, 1997, 1998; Nokleberg and others, 1994c, 1997c, 1989b). To a lesser extent, the belt also occurs (1) in the northern margin of the early Tertiary Orca Group of the Prince William terrane where locally metamorphosed to lower greenschist facies, (2) in metasedimentary rock of the Orca Group within a few kilometers of granitoid plutons, (3) along the southern margin of the Late Triassic through mid-Cretaceous McHugh Complex on the Kenai Peninsula, and (4) in Eocene and Oligocene granitoid plutons intruding the Valdez and Orca Groups. The deposits in this belt are of small tonnage but locally high grade. For this widespread group of mines and deposits, a unique mineral deposit model for Chugach-type low-sulfide Au quartz veins has been developed by Bliss (1992). The significant deposits are at Cliff, Alaska Oracle, Chalet Mountain, Crown Point, Kilpatrick, Gold King, Granite, Jewel, Kenai-Alaska, Lucky Strike (Palmer Creek), Mineral King (Herman and Eaton), Monarch, and Ramsey-Rutherford (table 4) (Nokleberg and others 1997a,b, 1998). Substantial Au production occurred in this district until the early 1940’s; recent exploratory work has been conducted at the Cliff Mine near Valdez, the largest of the many known deposits. Cliff Au Quartz Vein Deposit The Cliff Au quartz vein deposit (Johnson, 1915; Pickthorn, 1982; Jansons and others, 1984) consists of quartz veins, as much as 3 m thick and 515 m long, containing gold, pyrite, galena, sphalerite, arsenopyrite, and stibnite. The veins are hosted in metagraywacke and minor phyllite of the Late Cretaceous Valdez Group. The veins occur in a complicated system of intersecting faults. Sulfide minerals are about 3 to 5 percent of the ore. The mine contains a few thousand meters of underground workings. Production occurred mainly from 1906 to 1940. The average grade ranged from 34 to 69 g/t Au, and the mine at the deposit produced about 1,610 kg Au from about 25,000 tonnes of ore. Origin of and Tectonic Controls for Chugach Mountains Metallogenic Belt The Au quartz veins generally occur in the younger of two generations of quartz fissure veins (Richter, 1963; Goldfarb and others, 1986, 1997, 1998; Nokleberg and others, 1989b). The older and mostly barren veins are approximately parallel to the regional schistosity and to axial planes of minor and major folds. Their strike varies from northwest in the east to northeast in the west. The younger Au veins generally occur in a set of tensional cross joints or fractures and are normal to the older, barren quartz veins. Both sets of quartz veins generally dip steeply to vertically. Hydrothermal muscovite from Au-bearing veins has been dated at 53 Ma in the Port Valdez district (Winkler and others, 1981b), at 52 Ma in the Hope- Sunrise district (Mitchell and others, 1981), and at 57 Ma in the Nuka Bay district (Borden and others, 1992). These field relations and isotopic ages are interpreted as indicating that the deposits formed during early Tertiary regional metamorphism and anatectic granite plutonism. Regional tectonic and isotopic studies suggest that the Au veins formed in the Orca and Valdez Groups in response to subduction of the spreading Kula-Farallon Ridge beneath the southern Alaska continental margin (Plafker and others, 1989; Bradley and others, 1993; Haeussler and Nelson, 1993; Haeussler and others, 1995; Goldfarb and others, 1995; 1997; Goldfarb, 1997). Baranof Metallogenic Belt of Au Quartz Vein Deposits Southeastern Alaska (Belt BN) The Baranof metallogenic belt of Au quartz vein deposits occurs in southeastern Alaska and consists of a 250-km-long belt hosted in the Chugach subduction-zone terrane (fig. 103; tables 3, 4) (Brew, 1993; Monger and Nokleberg, 1996; Goldfarb and others, 1997, 1998). The significant deposit in the belt are Apex and El Nido, Chichagoff, Cobol, Hirst-Chichagof, and Reid Inlet (Nokleberg and others 1997a,b, 1998). The principal
deposits, at Chichagoff and Hirst-Chichagof are quartz-sulfide veins controlled by faults in metagraywacke and argillite of the Cretaceous Sitka Graywacke of the Valdez Group (Reed and Coats, 1941; Nokleberg and others, 1994a). The Bauer, Silver Bay, Cache, and Lucky Chance mines of the Sitka district have similar graywacke-hosted quartz-pyrite-pyrrhotite-arsenopyrite veins (Berg and Cobb, 1967). Located near the northern end of Chichagof Island, are the Apex-El Nido and Goldwin fissure quartz-sulfide vein mines that are hosted in Tertiary diorite plutons and amphibolite (Reed and Coats, 1941). Chichagoff and Hirst-Chichagof Au Quartz Vein Deposit The Chichagoff and Hirst-Chichagof Au quartz vein deposit consists of tabular to lenticular quartz veins that are a few meters thick, extend a few hundred meters along strike, and are as much as a few thousand meters depth along plunge. The veins are mainly ribbon quartz containing minor pyrite, arsenopyrite, galena, sphalerite, chalcopyrite, and some scheelite and tetrahedrite locally (Berg, 1984; Bundtzen, Green, Deager, and Daniels, 1987; Brew and others, 1991). Ore shoots occur mainly in shear and gouge zones along the Hirst and Chichagof Faults, especially along undulations in fault planes. The deposit is hosted in metagraywacke and argillite of the Cretaceous Sitka Graywacke. The mine produced about 24.6 million g Au, 1.24 million g Ag, and minor Pb and Cu from 700,000 tonnes of ore. Average grade is 7.2 g/t Au and 2.0 g/t Ag. Reserves are 91,000 tonnes of ore grading 41.2 g/t Au in several ore bodies. Apex and El Nido Au Quartz Vein Deposit The Apex and El Nido Au quartz vein deposit consists of quartz fissure veins as much as 2 m thick and stockworks containing sparse pyrite, arsenopyrite, chalcopyrite, galena, sphalerite, tetrahedrite, and gold (Still and Weir, 1981; Johnson and others, 1981). The mine at the deposit produced an estimated 622,000 g Au and 93,300 g Ag. The host rocks are an altered Mesozoic diorite pluton and an amphibolite mass within the pluton. The pluton intrudes late Paleozoic low-grade pelitic and intermediate volcanic rocks. Minor sulfides occur in the altered diorite wall rocks. The deposit also contains disseminations, veinlets, and small masses of scheelite. The vein system is symmetrical around a vertical fault that bisects the deposit. Origin of and Tectonic Controls for Baranof Metallogenic Belt The Au quartz vein deposits of the Baranof metallogenic belt occur mainly in the Late Cretaceous flysch of the Sitka Graywacke (part of the Valdez Group) where these units are metamorphosed to greenschist facies. The Au-quartz vein deposits also occur in early Tertiary granitoid plutons (with isotopic ages of about 51 to 52 Ma) that intrude the Chugach terrane; hydrothermal muscovite from Au-bearing veins has been dated at about 52 Ma (Taylor and others, 1994). As described above for the origin of the Chugach Mountains metallogenic belt, theAu quartz veins of the Baranof metallogenic belt are interpreted as forming in response to subduction of the spread- Late Cretaceous and Early Tertiary Metallogenic Belts (84 to 52 Ma) (figs. 102, 103) 243 ing Kula-Farallon Ridge beneath the southern Alaska continental margin (Plafker and others, 1989; Bradley and others, 1993; Haeussler and Nelson, 1993; Haeussler and others, 1995; Goldfarb and others, 1995; 1997; Goldfarb, 1997). Juneau Metallogenic Belt of Au Quartz Vein Deposits (Belt JU), Southeastern Alaska The Juneau metallogenic belt (also referred to as the Juneau gold belt) of Au quartz vein deposits (fig. 103; tables 3, 4) (Twenhofel and others, 1949; Twenhofel, 1952; Goldfarb and others, 1997, 1998) occurs in the Coast Mountains of southeastern Alaska. The belt, which was first defined by Spencer (1906) and redefined by Brew (1993), occurs in two areas. The northern part of the belt contains significant deposits at Alaska Juneau, Jualin, Riverside, Sumdum, and Treadwell. The southern part of the belt contains smaller deposits.The belt occurs along strike for about 250 km and is hosted in the Yukon-Tanana and Stikinia terranes, the Gravina-Nutzotin Gambier overlap assemblage, and younger, early Tertiary granitoid plutonic rocks. The significant deposits in the belt are at Alaska-Juneau, Gold Standard (Helm Bay), Goldstream, Jualin, Kensington, Riverside, Sea Level, Sundum Chief, and Treadwell (table 4) (Nokleberg and others 1997a,b, 1998). Most of the deposits occur in the western, greenschist facies part of a belt of inverted, regional-grade metamorphic that occurs to the west of, and underneath of a extensive, foliated tonalite sill that intruded along the western edge of the Yukon-Tanana terrane and the Wrangellia superterrane (Brew, 1994; Gehrels and Berg, 1994). Alaska-Juneau Au Quartz Vein Deposit The Au-quartz vein deposit consists of a network of lenticular quartz veins a few centimeters to 1 m thick that contain sparse scattered masses of gold, pyrite, pyrrhotite, arsenopyrite, galena, with minor sphalerite, chalcopyrite, and silver (Goldfarb and others, 1986, 1988, 1991, 1997; Newberry and Brew, 1987, 1988; Light and others, 1989; Brew and others, 1991; Miller and others, 1992). The Alaska-Juneau mine produced 108 tonnes Au, 59 tonnes Ag, and 21,800 tonnes Cu from 80.3 million tonnes of ore mined between 1893 and 1944. Reserves of 61.6 million tonnes grading 1.8 g/t Au remain (Alaska Mineral Industry, 1993, p.13).The vein lode system is about 5.6 km long and 600 m wide. The deposit consists of a series of parallel quartz stringers that are hosted in several units in (1) phyllite and schist near the contact between the Late Triassic Perseverance Slate; (2) amphibolite derived from late(?) Mesozoic (meta)gabbro dikes and sills; and (3) the informally named Gastineau volcanics of Permian and (or) Late Triassic age. Most of ore occurs in quartz veins, some in adjacent altered metamorphic rocks. Jualin Au Quartz Vein Deposit The Jualin Au-quartz vein deposit consists of four or five major quartz fissure veins and pipe-like stockworks that con-
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USGS Prepared in collaboration with
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U.S. Department of the Interior Gal
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iv Hart River SEDEX Zn-Cu-Ag Deposi
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vi Specific Events for Middle Throu
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viii Metallogenic Belts Formed Duri
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x Origin of and Tectonic Controls f
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xii Toodoggone Metallogenic Belt of
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xiv Slate Creek Serpentinite-Hosted
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xvi Left Omolon Belt of Porphyry Mo
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xviii Origin of and Tectonic Contro
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xx Chukotka Metallogenic Belt of Au
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xxii Plutonic Rocks Hosting East-Ce
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xxiv Skeena Metallogenic Belt of Po
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xxvi Bee Creek Porphyry Cu Deposit
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xxviii 36. Wellgreen gabbroic Ni-Cu
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xxx 87. Partizanskoe Pb-Zn skarn de
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Metallogenesis and Tectonics of the
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format (Nokleberg and others, 1996)
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logenesis of the region (1) subduct
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Subterrane—A fault-bounded unit w
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dilemma consists of two conflicting
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2 to 20 m thick. A related dolomite
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Lantarsky-Dzhugdzhur Metallogenic B
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Origin of and Tectonic Controls for
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Metallogenic Belts Formed During Pr
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as at Oz, Monster, and Tart, may al
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Monashee Metallogenic Belt of Sedim
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Clark Range Metallogenic Belt of Se
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in addition to the Fe deposits. Min
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study) consists of lenses, from 100
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Omulev Austrian Alps W Deposit The
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ock, including coarse clastic rock,
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lative metalliferous brines in a re
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Prince of Wales Island Metallogenic
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suite of deposits and host rocks ar
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margin of the North American Craton
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newly created terranes migrated int
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(Ryazantzeva and Shurko, 1992). The
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tonnes Au and an average grade of a
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mafic and felsic metavolcanic rocks
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intrusion from about 402 to 366 Ma
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mentary rocks of the Cambrian to De
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(Preto and Schiarizza, 1985; Schiar
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ate and clastic rocks and volcanicl
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(Nokleberg and others, 1994c, 1997c
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Berezovka River Metallogenic Belt o
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Finlayson Lake Metallogenic Belt of
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and barite in siliceous black turbi
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Windermere Creek (Western Gypsum) C
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(NX, DL, MY), Viliga (VL), and Zolo
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South of the main east-west-trendin
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ated subduction zone in the Wrangel
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icite-biotite-quartz bodies in frac
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Canada Cordillera. The granitoid ro
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Viliga (VL) passive continental-mar
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32; tables 3, 4) occurs along the n
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superterrane, consists mainly of ma
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ers, 1994c, 1997c). In southern Bri
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mental volcanic rocks of intermedia
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a resource of 34.3 million tonnes o
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potassic zone. Combined estimated p
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and quartz monzodiorite stock and s
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and Omolon (OM) cratonal terranes,
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in volcanic and volcaniclastic rock
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minor calcite, and sporadic pyrite
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supergene blanket are interpreted a
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deposits and occurrences consist of
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onto the Omulevka terrane to form t
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superterrane. This belt is interpre
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to form along the leading edge of t
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quartz, and is virtually not associ
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deposits are at Terrassnoe and Kuna
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Peschanka Porphyry Cu-Mo Deposit Th
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The belt is hosted in the Late Jura
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in a island arc that was tectonical
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and Early Cretaceous Koyukuk island
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The deposit consists of disseminate
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The Orange Hill deposit contains an
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49; tables 3, 4) (Foley and others,
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locally Late Triassic marine volcan
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gold in a gangue of quartz, calcite
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Verkhoyansk granite belt, which int
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metallogenic belts are interpreted
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assemblages, which may have been mo
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during hypogene and supergene alter
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collision and regional thrusting, t
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Yur Au Quartz Vein Deposit The smal
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phase has a Rb-Sr isotopic age of 1
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sian Northeast. The belt is hosted
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Host Granitoid Rocks and Associated
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that are up to 600-1,500 m long, av
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Metallogenic Belts Formed During La
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y partly coeval plutons that range
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tion is interpreted as occuring by
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the Badzhal-Ezop and Khingan parts
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and comagmatic with volcanic rocks;
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as interpreted for the Rock Creek d
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source (Yeo, 1992). The Blow River
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2000). The spatial location of the
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to the east in the central Yukon Te
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occur in a 30-km-long belt along ir
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The Emerald deposit has produced ap
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Metallogenic-Tectonic Model for Ear
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cham oceans were closed, and the Ch
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greisenized Mesozoic granite that i
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composition magmatic bodies (with a
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to Albian pelecypods (Nokleberg and
Page 223 and 224: quartz-arsenopyrite-pyrrhotite, pol
Page 225 and 226: thermally altered to siliceous and
Page 227 and 228: These ore bodies are as much as 1 m
Page 229 and 230: Eastern Asia-Arctic Metallogenic Be
Page 231 and 232: Demin, and Krasilnikov, 1974; Nekra
Page 233 and 234: 10 percent Cu, as much as 0.92 perc
Page 235 and 236: pyrite, pyrite, galena, sphalerite,
Page 237 and 238: content decreases with depth, as do
Page 239 and 240: azdelnoye, (2) porphyry Sn deposits
Page 241 and 242: Karalveem Au Quartz Vein Deposit Th
Page 243 and 244: Democrat (Mitchell Lode) Granitoid-
Page 245 and 246: with high-temperature and high-pres
Page 247 and 248: chalcocite and covellite and also h
Page 249 and 250: cum-North Pacific, (2) completion o
Page 251 and 252: (6) In the Paleocene (about 56 to 6
Page 253 and 254: sists of cinnabar and metacinnabari
Page 255 and 256: Eastern Asia-Arctic Metallogenic Be
Page 257 and 258: groups of deposits are interpreted
Page 259 and 260: Indian Mountain and Purcell Mountai
Page 261 and 262: and southeastern Alaska (Moll and P
Page 263 and 264: Nokleberg and others, 1995a; Bundtz
Page 265 and 266: g/t Au or 368.2 Au gold. The deposi
Page 267 and 268: wim Group and altered mafic dikes.
Page 269 and 270: Mount Nansen porphyry Cu-Mo deposit
Page 271 and 272: A Map 450 500 550 Cross section Dik
Page 273: Cretaceous and early Tertiary conti
Page 277 and 278: others, 1994c, 1997c). The signific
Page 279 and 280: tonnes grading 0.53 percent Ni, 0.3
Page 281 and 282: with a 0.25 percent cut-off. The de
Page 283 and 284: Bulkley Metallogenic Belt of Porphy
Page 285 and 286: Red Rose W-Au-Cu-Ag Polymetallic Ve
Page 287 and 288: ish Columbia and consists of severa
Page 289 and 290: during back-arc extension or transt
Page 291 and 292: stocks and dikes, is associated wit
Page 293 and 294: etrograde minnesotaite (Fe talc), F
Page 295 and 296: Specific Events for Early to Middle
Page 297 and 298: of fractured and faulted Permian-Tr
Page 299 and 300: sists of a mineralized fracture zon
Page 301 and 302: dolomite. Wall rock alteration incl
Page 303 and 304: elt of late Tertiary plutons that a
Page 305 and 306: plates that exhibit magnetic anomal
Page 307 and 308: stages (Petrenko, 1999): (1) In the
Page 309 and 310: mon. The deposit is of medium size
Page 311 and 312: Metallogenic-Tectonic Model for Lat
Page 313 and 314: The origin of the Hg deposits of th
Page 315 and 316: margin or island-arc tectonic envir
Page 317 and 318: Columbia: Implicatons for the Middl
Page 319 and 320: Bazard, D.R., Butler, R.F., Gehrels
Page 321 and 322: Bradley, D.C., Haeussler, P.J., and
Page 323 and 324: Bundtzen, T.K., Laird, G.M., Caluti
Page 325 and 326:
Cecile, M.P., 1982, The lower Paleo
Page 327 and 328:
Debari, S.M., and Coleman, R.G., 19
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U.S. Bureau of Land Management Open
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Cordilleran Orogen in Canada: Geolo
Page 333 and 334:
Goldfarb, R., Hart, C., Miller, M.,
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Grove, E.W., 1986, Geology and mine
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Høy, T., 1982a, Stratigraphic and
Page 339 and 340:
Jones, D.L., Silberling, N.J., Cone
Page 341 and 342:
Kutyev, F. Sh., Baikov, A.I., Sidor
Page 343 and 344:
Shield—Ultramafic magma and its m
Page 345 and 346:
Manns, F.T., 1981, Stratigraphic as
Page 347 and 348:
Miller, M.L., and Bundtzen, T.K., 1
Page 349 and 350:
Mortimer, N., 1987, The Nicola Grou
Page 351 and 352:
Noble, S.R., Spooner, E.T.C., and H
Page 353 and 354:
Canada Annual Meeting, Saskatoon, S
Page 355 and 356:
Perello, J.A., Fleming, J.A., O’K
Page 357 and 358:
Far East—Mineralogical criteria f
Page 359 and 360:
Roeske, S.M., Mattinson, J.M., and
Page 361 and 362:
Schmidt, J.M., and Zierenberg, R.A.
Page 363 and 364:
formation occurrences: Materialy po
Page 365 and 366:
Struik, L.C., 1986, Imbricated terr
Page 367 and 368:
Valuy, G., and Rostovsky, F., 1988,
Page 369 and 370:
Wolfe, W.J., 1995, Exploration and
Page 371 and 372:
Appendix Table 1. Mineral deposit m
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Table 2 Summary of correlations and
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Table 2—Continued Unit(s) and Cor
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Table 2—Continued Unit(s) and Cor
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Table 3—Continued Metallogenic Be
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Page 383 and 384:
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Table 4. Significant lode deposits,
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Table 4—Continued Appendix 369 De
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Table 4—Continued Tracy Metalloge
Page 405 and 406:
Table 4—Continued Appendix 373 In
Page 407 and 408:
Table 4—Continued Deposit Name Mi
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Table 4—Continued Mainits Metallo
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Table 4—Continued Whitehorse Meta
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Table 4—Continued Appendix 389 LA
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Page 425 and 426:
Table 4—Continued Surprise Lake M
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Table 4—Continued Sredinny Metall
Page 429:
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