USGS Professional Paper 1697 - Alaska Resources Library

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272 Metallogenesis and Tectonics of the Russian Far East, Alaska, and the Canadian Cordillera itic to alkalic basalt and associated rocks forming Sakhalin- Primorye volcanic belt (sp). This regional extension is also interpreted as the result of seaward rotation of the Kamchatka Peninsula and formed major units within the Sea of Okhotsk (as discussed by B.A. Natal’in in Nokleberg and others, 1994a). Back-arc spreading may have occurred simultaneously with trench rollback and migration of the Northeast Asia arc into the Pacific oceanic plate. (4) In the Arctic Ocean, rifting continued along the Gakkel Ridge (GK) along with continued sedimentation in the Amerasia Basin (as). Analysis of marine magnetic anomalies in the Eurasia Basin suggests this region underwent compression from about 36 to 5 Ma (Savostin and Drachev, 1988a,b; Harbert and others, 1990; Fujita and others, 1997). Geologic mapping reveals that late Miocene thrust faults and companion folds, which were associated with regional compression, occurred along the Myatisk and companion faults in the Mona and Chersky Ranges as described by Gaiduk and others (1989, 1993). Fault displacements are about 15 to 20 km. (5) A major orthogonal junction formed between the western end of Aleutian-Wrangell arc (al) and Central Kamchatka arc (kc). The western terminus of the Aleutian- Wrangell arc is interpreted as having been obducted onto the Kamchatka Peninsula, thereby forming the Kamchatskiy Mys oceanic terrane (too small to depict on fig. 127), which is interpreted as the oceanic base of the ancestral Aleutian- Wrangell arc, and the Stolbovskoy island-arc terrane (also too small to depict on fig. 127), which is interpreted as the older, western part of the arc (Geist and others, 1988, 1994). (6) In the early to middle Miocene, a short episode (approximately 22 to 10 Ma) of sea-floor spreading along the Komandorsky Ridge (KOM) formed a small pair of oceanic MIDDLE TERTIARY THROUGH PRESENT METALLOGENIC BELTS CK - Central Kamchatka CKY - Central Koryak CS - Central Sakhalin EK - East Kamchatka KV - Kvinumsky NSC OT - Olyutor SH - Sakhalin Island LE SR - Sredinny (unmapped) MO NSS ua ud TD oa uo bu ko ko BD ko UL NSC ud GL UL es oc KN oa wvk SA ma io oa no NSV io KN io io AL KN oa wvk ma RA io MT KH AO RA oa KN AGR ma io AC KN OL oc kk PA om NU rc LS SA io YA KM PA Arctic Ocean om om oc WP kk VE PK 168 76 72 68 om AM es SMA oa CA es TU sj SMA AM KE oa ej AM es sp CS ANV oa ANV SH NAB TR Sea of Okhotsk SR, KV KM kk CK IR ka IR OKA OK SB KRO OT TL CKY MAI kb MT OT EK kk VT AV OKA ar Bering Sea oc kk bs KY km 60 oa KK HI TO kr ku ku EK VT al oa ej NE KU al MT 56 KK KUK al 0 0 800 km 800 mi PAC Pacific Ocean 52 PW 168 120 44 315 60 156 68 168 76 120 132 144 156 168 180 Figure 125. Generalized map of major Tertiary through Present metallogenic belts, overlap assemblages, and tectonically linked subduction-zone or accretionary-wedge terranes for Russian Far East, northern Japan, and adjacent offshore areas. Refer to text for description of metallogenic belts. Adapted from Nokleberg and others (1997b, 1998). Refer to figure 61 for explanation. 180
plates that exhibit magnetic anomalies 5 and 6. The spreading occurred after the marine-arc volcanism in this area that formed the Bowers (bw) and Shirshov (sh) Ridges in the middle Eocene and early Miocene. (7) Intense tectonic disruption occurred in the western part of Aleutian-Wrangell arc, along the western Aleutian megathrust (AL), as a result of the transform coupling between the Pacific and North American Plates (Geist and others, 1988). A complex array of strike-slip, extension, and rotation structures formed in this area (Scholl and others, 1992, 1994; Vallier and others, 1994). In the area of the Bering Sea, a thick sedimentary prism continued to form in the Aleutian-Bowers Basin (atb), which overlies a fragment of accreted Kula oceanic plate (Plafker and Berg, 1994; Scholl and others, 1992, 1994). (8) Tectonic escape (crustal extrusion) of terranes continued to occur along major dextral-slip faults, including the Denali (DE), Iditarod-Nixon Fork (NF), Kaltag (KA), and companion faults (Scholl and others, 1992, 1994). Dextralwrench basins continued to form in association with the dextral-slip faults and were rapidly filled with continental 72 168 oa bs oc bs bs 168 BR km KY NY GD al 156 oa co KY om ia K KO yk km kw DE kw TG AP Arctic Ocean AL CG 144 co yk K km at at wr om kn KA TI om oa om cn DE BR kh CG at oa CO oa CG d PW PW 132 PW 56 AL oa 52 72 Pacific Ocean FO gg YAK NAC om TE cn CG 156 144 Middle Tertiary Metallogenic Belts (20 to 10 Ma) (figs. 125, 126) 273 PAC oa TI gg om sediments. Dextral displacement continued farther east along major dextral-slip faults such as the Denali (DF), Iditarod- Nixon Fork (NF), and Kaltag (KA) Faults. Estimates of total Cenozoic displacements along the Denali and Tintina faults are between 400 and 500 km each (Nokleberg and others, 1985; Plafker and Berg, 1994; Monger and Nokleberg, 1996). These and companion dextral-slip faults probably extended into the area of the Bering Sea. (9) The Pacific oceanic plate (PAC) continued to move northwestward. Along the Aleutian megathrust (AL) plate convergence continued to vary from oblique-orthogonal in the east to oblique to transform in the west. (10) The Aleutian-Wrangell continental-margin arc was associated with mainly oblique subduction of the northern edge of Pacific oceanic plate (PAC) along the Aleutian megathrust (AL) to form the Prince William terrane (PW). During northward migration, the Yakutat terrane (YA) started to underthrust the Prince William terrane along the eastern part of the Aleutian megathrust. Forming in the Aleutian-Wrangell continental-margin arc in southern Alaska was the Alaska cr om 48 cr QC FO sk bo NR PI cn 0 64 tt kl cn oa cr NAC 132 MIDDLE TERTIARY THROUGH PRESENT METALLOGENIC BELTS AP - Alaska Peninsula & Aleutian Islands OC - Owl Creek PC - Pinchi Lake ns FS gg PA OC gg oa cr BR ns sb PR HO OC JFR 56 JF SZ cn WA cr cn ca 800 km om ca oa 0 800 mi Figure 126. Generalized map of major middle Tertiary through Present metallogenic belts, overlap assemblages, and tectonically linked subduction-zone or accretionary-wedge terranes for Alaska, Canadian Cordillera, and adjacent offshore areas. Refer to text for description of metallogenic belts. Adapted from Nokleberg and others (1997b, 1998). Refer to figure 62 for explanation. PC kl CC ns FO 48
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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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Page 255 and 256: Eastern Asia-Arctic Metallogenic Be
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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
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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
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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
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Page 289 and 290: during back-arc extension or transt
Page 291 and 292: stocks and dikes, is associated wit
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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: elt of late Tertiary plutons that a
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
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
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Perello, J.A., Fleming, J.A., O’K
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Far East—Mineralogical criteria f
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Roeske, S.M., Mattinson, J.M., and
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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,
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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
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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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Table 4—Continued Surprise Lake M
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Table 4—Continued Sredinny Metall
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