USGS Professional Paper 1697 - Alaska Resources Library

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42 Metallogenesis and Tectonics of the Russian Far East, <strong>Alaska</strong>, and the Canadian Cordillera was an unknown subduction zone (UNK). In the southern Canadian Cordillera today, the Sicker arc is defined by the Sicker Group, which consists of Late Devonian arc-related volcanic and sedimentary strata, having a U-Pb zircon age of 367 Ma, and coeval intrusions (Muller, 1980; Parish and McNicoll, 1992). Occurring in the Alexander sequence (AX) was the Mount Sicker metallogenic belt of kuroko massive sulfide deposits, which formed in the subduction-related, short-lived Sicker arc. Insufficient data exist to ascertain the relative positions of the Wrangellia superterrane (WRA) and associated subduction zone. On the basis of paleomagnetic, geologic, geochronologic, and faunal data, the Wrangellia superterrane (Alexander sequence, AX) may have been derived from the Russian platform (Baltica) in the Barents Sea region (Bazard and others, 1993, 1994) or possibly from Australia (Gehrels and Saleeby, 1987). Metallogenic Belt Formed During Collision Yaroslavka Metallogenic Belt of Fluorite and Sn Greisen Deposits (Belt YA), Southern Part of Russian Southeast The Yaroslavka metallogenic belt of fluorite and Sn greisen deposits (fig. 16; tables 3, 4) occurs in the southwestern part of the Primorye Province of the Russian southeast (Ryazantseva, 1998). The deposits occur in numerous early W ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ E Paleozoic granitoid plutons that intrude Cambrian clastic and limestone units in the Vosensenka continental-margin arc terrane of the Khanka superterrane. The major fluorite greisen deposit is at Voznesenka-II; the major Sn greisen deposit is at Yaroslavka (table 4) (Nokleberg and others 1997a,b, 1998). Voznesenka-II Fluorite Greisen Deposit The major Voznesenka-II fluorite greisen deposit (fig. 19) (Androsov and Ratkin, 1990; Ryazantzeva, 1998) consists of fluorite that occurs above the apex of a 1.5 km-wide Late Cambrian intrusion of lithium-fluorine alaskite granite with Rb-Sr isotopic ages of about 512-475 Ma. The fluorite is interpreted as forming from metasomatic replacement and alteration of Early Cambrian, black organic limestone to greisen along a north-south-trending fault into which the alaskite granite intruded. An aggregate of muscovite and fluorite occurs at the periphery of the ore zone, whereas the greisen occurs in the middle of the zone. The greisen is often brecciated into fragments of mica and fluorite, fluoritized limestone, greisen, and greisenized granite, which are cemented by an aggregate of quartz, topaz, and micaceous-fluorite. The deposit is very large and contains an estimated 450 million tons fluorite ore averaging 30 to 35 percent CaF2. The Voznesenka-II deposit has been mined since 1960’s, is the sole producer of Russian fluorspar, and is currently one of the largest fluorine producers in the world. The formation of the greisen fluorspar deposits is interpreted as related to intrusion of Late Cambrian leucogranite 0 m 200 m 400 m v v v v v + ~ ~ Quaternary deposits Basic and intermediate dikes Greisenized granite Fluoritized limestone Fluorite ore Slate Limestone Tectonic fault and zone Contact 0 120 m Figure 19. Voznesenka II F greisen deposit, Yaroslavka metallogenic belt, Russian Southeast. Schematic cross section through Glavnoe deposit. Adapted from Androsov and Ratkin (1990) and Ryazantzeva (1998). See figure 16 and table 4 for location. Elevations below sea level.
(Ryazantzeva and Shurko, 1992). The high fluorine content of the granitic intrusions is related to the presence of Precambrian accumulations of boron, fluorine, and sufur, and other metals in the zone in the host sedimentary rocks. Isotopic analyses of boron in tourmaline from leucogranite suggests that evaporites were the source for the boron and that florine may be derived from associated dolomite. Yaroslavka Sn Greisen Deposit The major Yaroslavka Sn greisen deposit (fig. 20) (Govorov, 1977; Ryazantzeva, 1998) occurs mainly in greisen that mainly replaces skarn, limestone, and schist and to lesser extent in granite and granite porphyry with a Rb-Sr isotopic age of S S S S S S S S S S S S S S S S S S S S S S S S S S S Middle and Late Devonian Metallogenic Belts (387 to 360 Ma; figures 16, 17) 43 S S S S S S S S S 408 Ma and an initial Sr ratio of 0.7136 (Rayazantseva and others, 1994). Tin-bearing quartz and quartz-tourmaline veins, related to replacement of skarn by greisen, are classified into (1) mineralized fracture zones, (2) ore veins, (3) veinlets and ore pods, and (4) saddle-shaped and sheeted ore. The Sn ores are classified into three types based on mineral association—(1) tourmaline-quartz, (2) tourmaline-fluorite, and (3) sulfide-tourmaline-quartz with subordinate cassiterite-polymetallic and chlorite-sulfides. The sulfide minerals are dominantly pyrite, arsenopyrite, galena, and sphalerite. The deposit occurs along the contact of an early Paleozoic biotite granite (approximately 400 Ma) that intrudes Early Cambrian shale, siltstone, sandstone, and limestone. The pre-ore pyroxene-scapolite, vesuvianite-garnet, and epidote-amphibole skarn occurs in limestone and S + + Granite (Devonian) Limestone (Cambrian) Slate (Cambrian) Skarn Cassiterite-sulfide and cassiteritesulfide-quartz-tourmaline vein Sulfide-quartz-fluorite vein Cassiterite-tourmaline-fluorite vein Fault Contact Shear zone 0 300 m Figure 20. Yaroslavka Sn greisen deposit, Yaroslavka metallogenic belt, Russian Southeast. Schematic geologic map. Adapted from Govorov (1977) and Ryazantzeva (1998). See figure 16 and table 4 for location.
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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
Page 23 and 24: xxii Plutonic Rocks Hosting East-Ce
Page 25 and 26: xxiv Skeena Metallogenic Belt of Po
Page 27 and 28: xxvi Bee Creek Porphyry Cu Deposit
Page 29 and 30: xxviii 36. Wellgreen gabbroic Ni-Cu
Page 31 and 32: xxx 87. Partizanskoe Pb-Zn skarn de
Page 33 and 34: Metallogenesis and Tectonics of the
Page 35 and 36: format (Nokleberg and others, 1996)
Page 37 and 38: logenesis of the region (1) subduct
Page 39 and 40: Subterrane—A fault-bounded unit w
Page 41 and 42: dilemma consists of two conflicting
Page 43 and 44: 2 to 20 m thick. A related dolomite
Page 45 and 46: Lantarsky-Dzhugdzhur Metallogenic B
Page 47 and 48: Origin of and Tectonic Controls for
Page 49 and 50: Metallogenic Belts Formed During Pr
Page 51 and 52: as at Oz, Monster, and Tart, may al
Page 53 and 54: Monashee Metallogenic Belt of Sedim
Page 55 and 56: Clark Range Metallogenic Belt of Se
Page 57 and 58: in addition to the Fe deposits. Min
Page 59 and 60: study) consists of lenses, from 100
Page 61 and 62: Omulev Austrian Alps W Deposit The
Page 63 and 64: ock, including coarse clastic rock,
Page 65 and 66: lative metalliferous brines in a re
Page 67 and 68: Prince of Wales Island Metallogenic
Page 69 and 70: suite of deposits and host rocks ar
Page 71 and 72: margin of the North American Craton
Page 73: newly created terranes migrated int
Page 77 and 78: tonnes Au and an average grade of a
Page 79 and 80: mafic and felsic metavolcanic rocks
Page 81 and 82: intrusion from about 402 to 366 Ma
Page 85 and 86: mentary rocks of the Cambrian to De
Page 87 and 88: (Preto and Schiarizza, 1985; Schiar
Page 91 and 92: ate and clastic rocks and volcanicl
Page 93 and 94: (Nokleberg and others, 1994c, 1997c
Page 95 and 96: Berezovka River Metallogenic Belt o
Page 99 and 100: Finlayson Lake Metallogenic Belt of
Page 101 and 102: and barite in siliceous black turbi
Page 103 and 104: Windermere Creek (Western Gypsum) C
Page 105 and 106: (NX, DL, MY), Viliga (VL), and Zolo
Page 107 and 108: South of the main east-west-trendin
Page 109 and 110: ated subduction zone in the Wrangel
Page 111 and 112: icite-biotite-quartz bodies in frac
Page 113 and 114: Canada Cordillera. The granitoid ro
Page 115 and 116: Viliga (VL) passive continental-mar
Page 117 and 118: 32; tables 3, 4) occurs along the n
Page 119 and 120: superterrane, consists mainly of ma
Page 121 and 122: ers, 1994c, 1997c). In southern Bri
Page 123 and 124: 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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Origin of and Tectonic Controls for
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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
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groups of deposits are interpreted
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Indian Mountain and Purcell Mountai
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and southeastern Alaska (Moll and P
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Nokleberg and others, 1995a; Bundtz
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g/t Au or 368.2 Au gold. The deposi
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wim Group and altered mafic dikes.
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Mount Nansen porphyry Cu-Mo deposit
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A Map 450 500 550 Cross section Dik
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Cretaceous and early Tertiary conti
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deposits, at Chichagoff and Hirst-C
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others, 1994c, 1997c). The signific
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tonnes grading 0.53 percent Ni, 0.3
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with a 0.25 percent cut-off. The de
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Bulkley Metallogenic Belt of Porphy
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Red Rose W-Au-Cu-Ag Polymetallic Ve
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ish Columbia and consists of severa
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during back-arc extension or transt
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stocks and dikes, is associated wit
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etrograde minnesotaite (Fe talc), F
Page 295 and 296:
Specific Events for Early to Middle
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of fractured and faulted Permian-Tr
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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
Page 309 and 310:
mon. The deposit is of medium size
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Metallogenic-Tectonic Model for Lat
Page 313 and 314:
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
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Bundtzen, T.K., Laird, G.M., Caluti
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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
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.
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
Page 375 and 376:
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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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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