USGS Professional Paper 1697 - Alaska Resources Library

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276 Metallogenesis and Tectonics of the Russian Far East, Alaska, and the Canadian Cordillera conglomerate, and widespread large ignimbrite fields. Shallowmarine deposits predominate in the lower part and nonmarine deposits predominate in the upper part. The formation of the belt culminated with eruptions of Pliocene to Quaternary plateau basalts, which are associated with large composite cone volcanoes. The volcanic belt is interpreted as a major postaccretionary continental-margin arc, which is tectonically linked to the Kuril-Kamchatka accretionary-wedge and subductionzone complex (fig. 125) (Nokleberg and others, 1994c, 1997c). Central Kamchatka Metallogenic Belt of Au-Ag Epithermal and Porphyry Cu-Mo Deposits (Belt CK), Kamchatka Peninsula The Central Kamchatka metallogenic belt of Au-Ag epithermal vein and porphyry Cu-Mo deposits (fig. 125; tables 3, 4) occurs along the length of the Kamchatka Peninsula. The deposits are hosted in the Central Kamchatka Volcanic and Sedimentary Basin of Oligocene to Holocene age (Nokleberg and others, 1994c, 1997c). The significant deposits in the belt are (table 4) (Nokleberg and others 1997a,b, 1998) (1) Au-Ag epithermal vein deposits at Aginskoe (Aga), Baran’evskoe, Oganchinskoe, Ozernovskoe, Sukharikovskie Grebni, Tutkhlivayam, and Zolotoi, (2) a porphyry Cu-Mo deposit at Krasnogorskoe, and (3) a volcanic-hosted Hg deposit at Chempura. The Au-Ag epithermal vein deposits are interpreted as forming mainly during two stages in the Miocene: (1) In the early Miocene (22 to 14 Ma), during eruption of mainly felsic volcanic rocks, low sulfide, Au-Ag deposits, as at Ozernovskoe and Tutkhlivayam, with high Te contents, formed during construction of composite cone volcanoes and associated hypabyssal intrusions. At the same time, sulfide Au deposits, as at Olgakanskoe, with high Cu, Pb, and Zn contents, formed in association with intermediate intrusions. However, some of these deposits may have formed during the Late Eocene to Oligocene. (2) In the late Miocene (12 to 5 Ma), in the final stages of Miocene volcanism, andesitic and basaltic alterations. Au (+ Ag) epithermal vein deposits formed in association with small hypabyssal bodies and dikes, as at Aginskoe, Sukharikovskie Grebni, and Baran’evskoe deposits and some ore bodies of Tutkhlivayam deposit. These deposits consist mainly of gold and minor sulfide minerals in quartz-adularia veins. In the middle and northern parts of the belt, Hg deposits, as at Chempura, and Au and Au-Ag epithermal vein deposits occur in late Miocene hypabyssal bodies and dikes. Porphyry Mo, Cu, and Cu-Mo deposits in the southern part of the belt occur in Miocene subalkaline granite porphyry and porphyritic diorite. These granitoid plutons intrude areas underlain by the eastern part of the Sredinny-Kamchatka metamorphic terrane. These deposits, as at Kirganik, Krasnogorskoe, and Malakhitovoe, are small to medium-size and occur mainly in stockworks and in long fracture zones in both intrusions and adjacent metamorphic rocks. The major ore minerals are pyrite, chalcopyrite, and molybdenite. Molybdenite contains amounts of rhenium as much as 600 g/t. Ozernovskoe Au-Ag Epithermal Vein Deposit The large Ozernovskoe Au-Ag epithermal vein deposit (Shchepot’ev, 1989) consists of Au-bearing quartz-adularia veins along with Cu-Mo, realgar-orpiment, and Au-Ag deposits. The Au-Ag deposits occurs in veinlets and disseminations and is superimposed on various facies of hydrothermally altered rocks. Ore formed in fracture-filling veins and veinlets, and as metasomatic replacement of earlier aggregates. At least four stages of mineralization are recognized—(1) gold-goldfieldite-quartz (fineness of 933-938), (2) tellurium-silvanite-goldfieldite-kaolinite-quartz gold 945 fine, (3) gold-hessite-hydromica-quartz (gold 894 fine), and (4) gold-adularia-hydromica-quartz (gold 643 to 679 fine). Host rocks exhibit several types of alteration, mainly propylitization and silicification. Argillite displaying quartz-sericite, quartz-kaolinite, and quartz-montmorillonite-hydromica facies alteration occurs in the central part of the ore field near the main volcanic vent. Altered rocks consist of quartz and pyritealunite-kaolinite-quartz assemblages that form linear bodies as much as 100 m thick along the fault zones. The largest ore bodies occur in these tabular, altered silicified rocks. The deposit occurs in a weakly eroded volcano composed of basaltic andesite, andesite, and dacitic pyroclastic rocks and lava. The deposit is large and contain 0.01 to 0.1 percent Te and Au in rare high-grade zones, with as much as 700 g/t Au. Most of the ore is low-grade, ranging from 2 to 20 g/t Au. Aginskoe Au-Ag Epithermal Vein Deposit The Aginskoe Au-Ag epithermal vein deposit (Shchepot’ev,1989) consists dominantly of fine-grained, chalcedony-like quartz, adularia, and hydromica with colloform banding. The ore minerals are 0.3 to 1.0 percent of veins. The major ore minerals are tellurides, including hessite, altaite, calaverite, silvanite, and petzite. A total of 55 ore minerals are identified. Gold fineness ranges from 740 to 990, and the Au/Ag ratio varies from 2:1 to 7:1. Six stages of ore deposition are recognized—(1) quartz-pyrite, (2) gold-adularia-corrensite-quartz with a gold fineness of 924 to 968, (3) gold-adularia-quartz with a gold fineness of 936 to 952 at upper levels, and a gold fineness of 740 to 854 at deeper levels, (4) gold-calaverite-quartz with a gold fineness 940 to 960, (5) gold-hessite-corrensitequartz with a gold fineness 816 to 880, and (6) quartz-zeolitecalcite. Endogenous zoning is marked by a vertical change of ore composition, texture, and structure. The concentration of tellurides and sulfides increases with depth. The deposit occurs in a volcanic caldera composed of Miocene basaltic andesite and basaltic andesite tuff. Ore occurs in fracture zones and zones of intense jointing. Ore-bearing structures consist of shear and breccia tectonic zones, which include numerous andesitic dikes and veins, lenses, and veinlets of adularia-quartz and quartz-carbonate composition. The main ore-bearing zones are the Aginskaya and Surpriz. In the main ore-bearing zones, short ore bodies merge at depth forming a gently dipping mineralized band, complicated in the upper part by steeply dipping ore shoots. Hydrothermal alteration, commonly propylitic, is com-
mon. The deposit is of medium size and contains an estimated resource of 30 to 50 tonnes Au and 70 to 100 tonnes Ag. The average grade of the Aginskoe deposit is 20 g/t Au. The deposit is currently under development. Kirganik Porphyry Cu Deposit The Kirganik porphyry Cu deposit (Vlasov, 1977; A.V. Ignatyev, written commun., 1980) consists of steeply dipping zones of rocks with biotite-K-feldspar metasomatic alteration. The deposit is 10 to 15 m thick, as much as 1,200 m long, and occurs in Late Cretaceous siliceous volcanic rocks. The deposit consists of zones of disseminated and veinlet copper and Au minerals. The ore bodies are generally conformable with the host rocks. The oxidized zone extends deepest in heavily fractured rocks, to a depth of 100 to 120 m, and contains as much as 0.8 g/t Au. The richest ore is in biotite-K-feldspar-metasomatically altered rocks. Altered rocks containing both pyroxene and K-feldspar are practically devoid of ore. The ore minerals are pyrite, chalcopyrite, magnetite, bornite, chalcocite, hematite, and gold. The richest Au values occur in rich chalcosite-chalcopyrite-bornite ore with more than 1 percent Cu. The K-Ar isotopic age of the biotite-K-feldspar-altered rocks that host the ore is 65 to 75 Ma. The deposit is of medium size. Average grades are 0.1 to 1 percent Cu and 0.2 to 0.4 g/t Au in disseminated and veinlet ore, and as much as 0.8 g/t Au in oxidized ore. Origin of and Tectonic Controls for Central Kamchatka Metallogenic Belt The Central Kamchatka Volcanic and Sedimentary Basin (Nokleberg and others, 1994c, 1997c), which hosts the Central Kamchatka metallogenic belt, consists chiefly of late Oligocene to Holecene volcanic and sedimentary rocks in sequences as much as 5 km thick. The belt ranges from 20 to 70 km wide and is about 350 km long. The volcanic and sedimentary basin also contains mainly shallow-marine sedimentary rocks as much as 6,000 m thick and widespread tuff, basalt, and basaltic andesite. The basinal units overly deformed Late Cretaceous to early Tertiary sedimentary rocks. The basin is interpreted as a fore-arc unit of the Central Kamchatka volcanic belt; both are interpreted as parts of the major, postaccretionary, Northeast Asia continental-margin arc in the Russian Far East (Nokleberg and others, 1994c, 1997c). Alaska Peninsula and Aleutian Islands Metallogenic Belt of Igneous Arc Deposits (Belt AP), Western-Southern Alaska The major Alaska Peninsula and the Aleutian Islands metallogenic belt of igneous arc deposits (fig. 126; tables 3, 4) occurs in western-southern Alaska (Nokleberg and others, 1995a). The metallogenic belt is hosted in the area underlain or adjacent to the middle and late Tertiary granitic and volcanic rock of the Aleutian arc in the eastern Aleutian Islands and the southwestern Alaska Peninsula (Nokleberg and others, 1994c, Middle Tertiary Metallogenic Belts (20 to 10 Ma) (figs. 125, 126) 277 1997c). The arc is composed mainly of middle Tertiary to Holocene andesite to dacite flows and tuff, shallow intrusive rocks, small silicic stocks and sills, and associated sedimentary rocks (Burk, 1965; Wilson, 1985). Underlying parts of the southwestern Alaska Peninsula, almost as far west as Cold Bay, is the mainly Mesozoic bedrock of the Peninsular island-arc terrane. Numerous epithermal vein, polymetallic vein, and porphyry Cu and Cu-Mo deposits occur in the metallogenic belt. The significant deposits are (table 4) (Nokleberg and others 1997a,b, 1998) (1) epithermal vein deposits at Apollo-Sitka, Aquila, Canoe Bay, Fog Lake (Pond), Kuy, Shumagin, and San Diego Bay, (2) polymetallic vein deposits at Braided Creek, Sedanka (Biorka), Cathedral Creek, and Kilokak Creek, and (3) porphyry Cu and Mo deposits at Bee Creek, Mallard Duck Bay, Mike, Pyramid, Rex, and Sedanka (Biorka). The epithermal and polymetallic vein and porphyry deposits of the Alaska Peninsula and Aleutian Islands belt occur over a distance of more than 800 km. This belt is related to the epithermal and hydrothermal activity associated with the late-magmatic stages of Tertiary and Quaternary hypabyssal plutonic and associated volcanic centers. These centers are along part of the Aleutian arc, one of the classic continentalmargin arcs along the rim of the Circum-Pacific rim. Pyramid Porphyry Cu Deposit The Pyramid porphyry Cu deposit (Armstong and others, 1976; Hollister, 1978; Wilson and Cox, 1983; G.L. Anderson, written commun., 1984; R.L. Detterman, oral commun., 1986) occurs in the southwestern Alaska Peninsula and consists of disseminated molybdenite and chalcopyrite(?) in a Fe-stained dacite porphyry stock of late Tertiary age. A zonal alteration pattern is defined by a core of secondary biotite, containing about 3 to 10 percent magnetite, which grades outward into an envelope of quartz-sericite alteration. Fractures adjacent to the stock are filled with sericite. Local extensive oxidation and supergene enrichment by chalcocite and covellite occur in a blanket as much as 100 m thick. The deposit is centered on a 3 km2 area within the stock and contains a resource of 110 million tonnes grading 0.4 percent Cu, 0.03 percent Mo and trace Au (G.L. Anderson, written commun., 1984). The host stocks and dikes, and several smaller stocks that occur nearby all intrude the fine-grained clastic rocks of the Late Cretaceous Hoodoo Formation and the Paleocene or Eocene to Oligocene Stepovak(?) or Tolstoi(?) Formation. The sedimentary rocks are contact metamorphosed adjacent to the stocks. Bee Creek Porphyry Cu Deposit The Bee Creek porphyry Cu deposit consists of chalcopyrite, pyrite, and traces of molybdenite in contact-metamorphosed Jurassic and Cretaceous sedimentary rocks that are intruded by a small tonalite porphyry stock of Tertiary age (Cox and others, 1981). The deposit, located on the Alaska Peninsula 25 km northeast of Chignik Lagoon, was discovered by Bear Creek Mining Company in cooperation with Bristol Bay Native Corporation in the late 1970’s (E.D. Fields, written commun., 1977).The contact-metamorphosed sedimentary
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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
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quartz-arsenopyrite-pyrrhotite, pol
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thermally altered to siliceous and
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These ore bodies are as much as 1 m
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Eastern Asia-Arctic Metallogenic Be
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Demin, and Krasilnikov, 1974; Nekra
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10 percent Cu, as much as 0.92 perc
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pyrite, pyrite, galena, sphalerite,
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content decreases with depth, as do
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azdelnoye, (2) porphyry Sn deposits
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Karalveem Au Quartz Vein Deposit Th
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Democrat (Mitchell Lode) Granitoid-
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with high-temperature and high-pres
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chalcocite and covellite and also h
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cum-North Pacific, (2) completion o
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(6) In the Paleocene (about 56 to 6
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sists of cinnabar and metacinnabari
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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 and 274: Cretaceous and early Tertiary conti
Page 275 and 276: deposits, at Chichagoff and Hirst-C
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: stages (Petrenko, 1999): (1) In the
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
Page 329 and 330: U.S. Bureau of Land Management Open
Page 331 and 332: Cordilleran Orogen in Canada: Geolo
Page 333 and 334: Goldfarb, R., Hart, C., Miller, M.,
Page 335 and 336: Grove, E.W., 1986, Geology and mine
Page 337 and 338: 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.
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formation occurrences: Materialy po
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Struik, L.C., 1986, Imbricated terr
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Valuy, G., and Rostovsky, F., 1988,
Page 369 and 370:
Wolfe, W.J., 1995, Exploration and
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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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Table 4. Significant lode deposits,
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Table 4—Continued Appendix 369 De
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Table 4—Continued Tracy Metalloge
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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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Page 413 and 414:
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Table 4—Continued Whitehorse Meta
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Table 4—Continued Appendix 389 LA
Page 423 and 424:
Page 425 and 426:
Table 4—Continued Surprise Lake M
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Table 4—Continued Sredinny Metall
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