USGS Professional Paper 1697 - Alaska Resources Library

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218 Metallogenesis and Tectonics of the Russian Far East, Alaska, and the Canadian Cordillera tion of part of the Pacific oceanic plate (PAC) to form the West Kamchatka (WK) and Ekonay (EK) terranes. Local plutons in the Okhotsk-Chukotka volcanic-plutonic belt intruded under extension, probably as the result of rollback of the subduction slab during the Late Cretaceous (Amato and Wright, 1997). Also in the same region, the Okhotsk-Chukotka and East Sikhote-Alin continental-margin arcs were offset in a sinistral sense along the Mongol-Okhotsk fault system (MO). Continuing in the Okhotsk- Chukotka arc was the Eastern Asia metallogenic belt of graniticmagmatism-related deposits, which contained a complex array of zones. Continuing or new zones were the Anuyi-Beringovsky (AB), Chaun (CN), Chukotka (CH), Korkodon-Nayakhan (KN), Okhotsk (OH), Omsukchan (OM), Verkhoyansk-Indigirka (VY), Verkhne–Kolyma (VK), Verkhne-Yudomsky (VY) zones. Also continuing to form in the Okhotsk-Chukotka volcanic-plutonic belt and peripherally related to the Eastern Asia metallogenic belt in the Russian Far East were the Adycha-Taryn (AT), and Vostochno-Verkhoyansk (VV) metallogenic belts. Forming in the Okhotsk-Chukotka volcanic-plutonic belt in western Alaska, and peripherally related to the Eastern Asia metallogenic belt, were the Northwestern Koyukuk Basin metallogenic belt (NWK), which contains felsic plutonic U deposits, the Seward Peninsula metallogenic belt (SP) that contains Sn skarn and related deposits, and the West-Central Alaska metallogenic belt (WCA), which contains porphyry Cu deposits. NSC COLL EAST SIKHOTE- ALIN ARC LA es SY WSA SG, TK, KM, LZ o At 50-60 latitude NE, SH, TR KRO IR MO CS HI, ANV, NAB VT OLYUTORKA ARC (ASC, IOC) OH OKA, IR KH, VT NSC VV VI VY oc 60 o ? ? ? 80 o am ? ? KO KA NF (4) Between the areas of the Russian Far East and Alaska, continental-margin arcs and companion subduction zones in each region were connected by a major transform fault. In the area of western Alaska, tectonic escape (crustal extrusion) of terranes occurred along major dextral-slip faults, including the Denali (DE), Iditarod-Nixon Fork (NF), Kaltag (KA), and companion faults (Scholl and others, 1992, 1994). In association with movement on these major dextral-slip faults, dextral-wrench sedimentary basins formed, including the Kuskokwim Basin (kw; Plafker and Berg, 1994; Bundtzen and Miller, 1997). The crustal extension and wrench faulting were associated with a major period of extension in Interior Alaska according to the interpretation of Miller and Hudson (1991). The middle and Late Cretaceous extension is interpreted as forming warm, thin continental crust that was favorable for crustal extrusion and dextral-wrench faulting (Scholl and others, 1992, 1994). (5) By the early Tertiary, in the region of the Amerasia (ab), Canada (cb) and Eurasia (eb) Basins, sea-floor spreading and associated rifting was completed (Grantz and others, 1990, 1991, 1998), and sedimentation continued in the large Amerasia (ab), Canada (cb) and Eurasia (eb) Basins. The formation of the Alpha and Mendeleev Ridges (am), which are interpreted as large piles of hot-spot basalt and associated deposits, was completed (Grantz and others, 1990, 1991, 1998). (TA, KT) eb NAC COLLAGE OF ab RIFTED cb TERRANES: NSV NR, CK, CS, AT AP COLL cb NAM VK CN, OKHOTSK- CH (CH) CHUKOTKA ARC COLL NAM SP oc (AA) ECA NAC KLUANE km ARC oc pn SL BK, NAC COLL oc SK COAST cn ARC KN, at WK EK ka OM AB kw COLL km KLUANE cn at ARC CG WRA sab COLL PAC CG KMT sab KULA WRA PR FAR cn 0 800 km 84 to 52 Ma 0 800 km WCA, METALLOGENIC BELTS LA - Lower Amur LZ - Luzhkinsky AB - Anuyi-Beringovsky MC - Maclaren AT - Adycha-Taryn NW - KNorthwest Koyukuk BK - Bulkley Basin BN - Baranov NS - Nelson CF - Catface OH - Okhotsk CM - Chugach Mounains OM - Omsukchan CN - Chaun PW - Prince William Sound CH - Chukotka SA - Southern Alaska CS - Central Sakhalin SG - Sergeevka CSE - Central-Southeastern SK - Skeena Alaska SL - Surprise Lake ECA - Eastern-Southern SP - Seward Peninsula Alaska TK - Taukha FLB - Fish Lake-Bralorne TM - Talkeetna Mountains GA - Gambier TY - Tyaughton-Yalakom IR - Iruneiskiy VI - Verkhoyansk-Indigirka JU - Juneau VK - Verkhne-Kolyma KH - Khingan VV - Vostochno-Verkhoyansk KM - Kema VY - Verkhne-Yudomsky KMT - Kuskokwim Mountains WCA - West-Central Alaska KN - Korkodon-Nayakhan YK - Yakobi NWK FLB, TY NS TM MC, JU CM SA BN, YK CSE PW GA, CF DE TI ? ? Figure 104. Late Cretaceous and early Tertiary (Campanian through early Eocene—84 to 52 Ma) stage of metallogenic-tectonic model for the Russian Far East, Alaska, and the Canadian Cordillera and adjacent offshore areas. Refer to text for explanation of metallogenic-tectonic events, to tables 3 and 4 for descriptions metallogenic belts and significant deposits, and to figure 18 for explanation of abbreviations, symbols, and patterns. Adapted from Nokleberg and others (1997b, 1998, 2000). 60 o HA RL
(6) In the Paleocene (about 56 to 60 Ma), in the area of the Bering Sea, major counter-clockwise rotation of the Pacific oceanic plate (PAC) occurred (at about 30º to 50º paleolatitude; Lonsdale, 1988). The rotation resulted from compression between Eurasia and North America (Plafker and Berg, 1994). At the same time, the extension of dextral-slip faults from the area of western Alaska into the Bering Sea resulted in accretion and capture of a fragment of the Kula oceanic plate (KULA; Scholl and others, 1992, 1994). (7) In response to oblique subduction of the Kula oceanic plate (KULA), the major Kluane continental-margin arc formed (Plafker, 1994; Nokleberg and others, 2000). Parts of the arc are preserved as the Kuskokwim Mountains volcanic-plutonic belt (km) and Alaska Range-Talkeetna Mountains igneous belt (at). The coeval Coast arc formed along the margin of the North American Cordillera. Parts of this arc are preserved in the Coast-North Cascade plutonic belt (cn) and the Kamloops magmatic belt (kl). These continental-margin arcs overlapped the previously accreted Wrangellia superterrane and adjacent inboard terranes and extended for a distance of more than 3,200 km along the active continental margin of the North American Cordillera. Associated with the Kluane continental-margin arc was the subduction of the laterally extensive Chugach terrane (CG) and the Pacific Rim terrane (PAR). Forming in the Kluane arc in southern Alaska were the East-Central Alaska (younger part; ECA), Southern Alaska (SA), and Kuskokwim Mountains (KMT) belts, which are hosted in the Kuskokwim Mountains sedimentary and volcanic belt or the Alaska Range-Talkeetna Mountains igneous belt. Forming in the Coast arc in southeastern Alaska and the Canadian Cordillera were a large array of metallogenic belts, which contain granitic-magmatism-related deposits, which are hosted in or near the Coast-North Cascade plutonic belt. The belts include the Catface (CF), central-southeastern Alaska (CSE), Bulkley (BK), Fish Lake-Bralorne (FLB), Gambier (GA), Nelson (NS), Skeena (SK), and Surprise Lake (SL) belts. All these belts are interpreted as forming during subduction-related granitic plutonism. (8) Along the active margin of the North American Cordillera, the rapid northward migration of the Kula oceanic plate (KULA), which started to form at about 85 Ma (Englebretson and others, 1985), resulted in formation of major dextral-slip faults, including the Denali (DE), Tintina (TI), Ross Lake (RL), and companion faults (Plafker and Berg, 1994). Oblique subduction of the Kula-Farallon oceanic ridge occurred at about 50 to 60 Ma along the margin of southern Alaska (Bradley and others, 1993). The subduction of the oceanic ridge, locally partly preserved in ophiolites in the Prince William Terrane (Lytwyn and others, 1997; Kusky and Young, 1999), in the early Tertiary is interpreted as causing (1) a regional metamorphic welt and formation of anatectic granites (Plafker and others, 1989b; 1994), (2) rapid changes in components strike-slip movements along the subduction zone bordering the early Tertiary continental margin (Bradley and others, 1993), and (3) formation of belts of early Tertiary granitic and mafic-ultramafic plutonic rocks of the Sanak-Baranof plutonic belt (unit sab (Hudson, 1979; Moll- Late Cretaceous and Early Tertiary Metallogenic Belts (84 to 52 Ma) (figs. 102, 103) 219 Stalcup and others, 1994) in Southern and southeastern Alaska, which are interpreted as forming in a near-trench environment during subduction of the Kula-Farallon oceanic ridge (Bradley and others, 1993; Kusky and others, 1997). In Southern and southeastern Alaska, several metallogenic belts are interpreted as forming during oblique subduction of the Kula-Farallon oceanic ridge under margin of Southern and southeastern Alaska. These metallogenic belts include the Baranof (BN), Chugach Mountains (CM), Juneau (JU), Maclaren (MC), and Talkeetna Mountains (TM) metallogenic belts, which contain Au quartz vein deposits, and the Yakobi (YK) metallogenic belt, which contains gabbroic Ni- Cu deposits. (9) Also in the same region, the Prince William Sound (PW) metallogenic belt, which contains massive sulfide deposits related to marine mafic volcanic rocks, is interpreted as forming during sea-floor spreading along the Kula-Farallon oceanic ridge before subduction of the ridge beneath the margin of southern Alaska. (9) Regional extension occurred in the southern Canadian Cordillera and northeastern Washington. The extension is interpreted as (1) the result of a change from transpression to transtension at about 55 Ma (Parrish and others, 1988), (2) caused by a change of obliquity of convergence of the oceanic plate, and (or) (3) alternatively, but likely, collapse of overthickened thrust units. (10) The eastward thrusting of the North American Craton Margin (NAM) over the North American Craton (NAC) ended at about 60 Ma in the Canadian Cordillera. Metallogenic Belt Formed in Late Mesozoic and Early Cenozoic Olyutorka Island Arc, Russian Northeast Iruneiskiy Metallogenic Belt of Porphyry Cu Deposits (Map Unit IR), Southern Kamchatka Peninsula The small Iruneiskiy metallogenic belt (IR) of porphyry Mo deposits (Vlasov, 1977) occurs in the southern part of the Kamchatka Peninsula in the Iruneiskiy island-arc terrane (fig. 102; tables 3, 4) (Nokleberg and others, 1994c, 1997b, c, 1998). The one economic porphyry Cu deposit in the belt at Kirganik (Vlasov, 1977; A.V. Ignatyev, written commun., 1980) consists of steeply dipping , metasomatically altered zones of biotite and K-feldspar that occur in Late Cretaceous siliceous volcanic rocks. The altered zones contain veinlets and disseminations of pyrite, chalcopyrite, bornite, chalcocite, hematite, and gold; the zone contain as much as 0.8 g/t Au. The Late Cretaceous calc-alkalic volcanic rocks hosting the zones grade upward into Maastrichtian shoshonite that is intruded by dunite-clinopyroxenite-gabbro monzonite. The porphyry Cu deposits are interpreted as being related to the monzonite intrusions. The deposit has a K-Ar isotopic age of 75 to 65 Ma that is similar to that for the intrusion. The deposit is of medium size, and average grades are 0.1 to 1 percent Cu
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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;
Page 199 and 200: as interpreted for the Rock Creek d
Page 201 and 202: source (Yeo, 1992). The Blow River
Page 203 and 204: 2000). The spatial location of the
Page 205 and 206: to the east in the central Yukon Te
Page 207 and 208: occur in a 30-km-long belt along ir
Page 209 and 210: The Emerald deposit has produced ap
Page 211 and 212: Metallogenic-Tectonic Model for Ear
Page 213 and 214: cham oceans were closed, and the Ch
Page 215 and 216: greisenized Mesozoic granite that i
Page 217 and 218: composition magmatic bodies (with a
Page 219 and 220: Origin of and Tectonic Controls for
Page 221 and 222: 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: cum-North Pacific, (2) completion o
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 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
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dolomite. Wall rock alteration incl
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elt of late Tertiary plutons that a
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plates that exhibit magnetic anomal
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stages (Petrenko, 1999): (1) In the
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mon. The deposit is of medium size
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Metallogenic-Tectonic Model for Lat
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The origin of the Hg deposits of th
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margin or island-arc tectonic envir
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Columbia: Implicatons for the Middl
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Bazard, D.R., Butler, R.F., Gehrels
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Bradley, D.C., Haeussler, P.J., and
Page 323 and 324:
Bundtzen, T.K., Laird, G.M., Caluti
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Cecile, M.P., 1982, The lower Paleo
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Debari, S.M., and Coleman, R.G., 19
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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.,
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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
Page 373 and 374:
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
Page 379 and 380:
Table 3—Continued Metallogenic Be
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Table 4. Significant lode deposits,
Page 401 and 402:
Table 4—Continued Appendix 369 De
Page 403 and 404:
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
Page 409 and 410:
Table 4—Continued Mainits Metallo
Page 411 and 412:
Page 413 and 414:
Page 415 and 416:
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
Page 427 and 428:
Table 4—Continued Sredinny Metall
Page 429:
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