USGS Professional Paper 1697 - Alaska Resources Library

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122 Metallogenesis and Tectonics of the Russian Far East, <strong>Alaska</strong>, and the Canadian Cordillera Mainits Metallogenic Belt of Kuroko Massive Sulfide Deposits (Belt MA), Eastern Part of Russian Northeast The Mainits metallogenic belt of Kuroko massive sulfide deposits (fig. 48; tables 3, 4) occurs in the eastern part of the Russian Northeast. The east-west-trending belt is 170 km long, as much as 40 km wide, and is hosted in the Late Jurassic and Early Cretaceous Mainitskiy island-arc terrane (Nokleberg and others, 1994c, 1997c). The significant deposit in the belt is at Ugryumoe (table 4) (Nokleberg and others 1997a,b, 1998). Ugryumoe Massive Sulfide Deposit The Ugryumoe deposit consists of massive sulfides that contain high concentrations of Cu, Zn, Pb, and Au that occur along a silicified zone as much as 3 km long (Oparin and Sushentsov, 1988). The sulfide horizons consists of massive pyrite, and chalcopyrite, pyrite, and quartz. The sulfides occur in a Mesozoic sequence of interbedded basalt, plagiorhyolite, tuff, and siliceous tuffaceous siltstone. The deposit is interpreted as a possible kuroko massive sulfide deposit and occurs in the Hettangian and Sinemurian Lazov sequences. The sequences contain interbedded basalt, plagiorhyolite, tuffs, and tuffaceous siltstone. Intrusive rocks include granite, plagiogranite, and gabbro. Abundant 0 1 km geological data suggest significant potential for additional massive sulfide deposits in this belt. Origin of and Tectonic Controls for Mainits Metallogenic Belt The Mainitskiy island-arc terrane that hosts the Mainits metallogenic belt consists of an older and a younger sequence (Nokleberg and others, 1994c, 1997c). The older sequence consists of (1) a lower unit of serpentinite and serpentinite mélange that contains fragments of late Paleozoic and early Mesozoic ophiolites, and limestone with spilite and bedded jasper that contains Middle and Late Jurassic radiolarians, and (2) an upper unit of graywacke, siltstone, tuff, and bedded chert that contain rare Berriasian and Valanginian Buchia. Local olistoliths are common and are composed of ophiolite, limestone, plagiogranite, andesite, and rhyolite that are all metamorphosed to pumpellyite facies. The younger sequence consists of a thick assemblage of Late Jurassic and Early Cretaceous island arc volcanic and sedimentary rocks composed of tholeiitic basalt, andesitic basalt, rhyolite, tuff, breccia, chert, siltstone, and sandstone. The younger sequence is interpreted as primitive island-arc sequence and contains the Lazov sequence, which hosts the massive sulfide deposits of the Mainits metallogenic belt. The Late Jurassic and Early Cretaceous part of the Mainitskiy terrane is interpreted as forming Dioritic porphyry and andesite intrusions (Late Cretaceous- Paleogene) Tuff-sandstone, siltstone, chert (Late Jurassic-Early Cretaceous(?)) Dunite with orthopyroxenite veins Harzburgite Late Jurassic and Early Cretaceous(?) Pyroxenite, dunite, and harzburgite Serpentinite melange Contact Fault Facies transition PGE-chromite occurrence Strike and dip of compositional layering Figure 54. Krasnaya Gora podiform Cr deposit, Tamvatney-Mainits metallogenic belt, Russian Northeast. Schematic geologic map. Adapted from Dmitrenko and others (1987). See figure 48 and table 4 for location.
in a island arc that was tectonically linked to the Alkatvaam accretionary-wedge terrane (Nokleberg and others, 2000). Svyatoy-Nos Metallogenic Belt of Au-Ag Epithermal Vein Deposits (Belt SVN), Northern Part of Russian Northeast The Svyatoy-Nos metallogenic belt of Au-Ag epithermal vein deposits (fig. 48; tables 3, 4) occurs in the northern part of the Russian Northeast. The deposits are closely related to intermediate and felsic dikes with K-Ar isotopic ages of 149 Ma that are part of Late Jurassic Svyatoy Nos volcanic belt (Bakharev and others, 1998). The epithermal Au-Ag deposits in the metallogenic belt, as at Polevaya, are associated with dikes and small bodies of Early Cretaceous subvolcanic rhyolite, monzonite, and quartz syenite-porphyry (Nokleberg and others 1997a,b, 1998). The Svyatoy-Nos metallogenic belt is partly overlain by Cenozoic sedimentary rocks of the Primorskaya lowland. The sole significant deposit is at Polevaya (table 4). Polevaya Au-Ag Polymetallic Vein Deposit The Polevaya Au-Ag polymetallic vein deposit (Nekrasov, 1962; Bakharev and others, 1988) consists of two thin, subparallel zones of intensely silicified and sericitized granodiorite and quartz diorite. The zones range from 1 to 2 m thick and to as much as 500 m long. The zones occur along and near the contact of an Early Cretaceous pluton that forms the core of a complex, Late Jurassic to Late Cretaceous volcanicplutonic structure. The major minerals are chalcedony-like cryptocrystalline quartz, calcite, pyrite, galena, sphalerite, chalcopyrite, and gold. The sulfide content is about 2-3 percent. The deposit contains as much as 10 g/t Au, 10 g/t Ag, 0.020-1 percent Pb, 0.050-1 percent Zn, 0.005-0.3 percent Cu, and 0.5 percent Sn. Origin of and Tectonic Controls for Svyatoy-Nos Metallogenic Belt The Svyatoy-Nos metallogenic belt is hosted in the younger (Neocomian) part of Late Jurassic and Early Cretaceous Oloy-Svyatoy Nos volcanic belt (Nokleberg and others, 1994c, 1997c). This igneous belt occurs along the northeastern margin of the Kolyma-Omolon superterrane and is part of the Indigirka-Oloy sedimentary-volcanic-plutonic assemblage. The belt contains mainly andesite, rhyolite, and tuff with interlayered shallow-marine sandstone, conglomerate, and siltstone (Parfenov, 1995a,b). The Oloy-Svyatoy Nos volcanic belt occurs adjacent to and southwest of the South Anyui terrane (fig. 48) and consists of mainly shallow-marine, rarely nonmarine basalt, andesite, rhyolite, and tuff with interlayered sandstone, conglomerate, siltstone, and shale. The volcanic belt also contains small bodies of granite, granodiorite, and monzogranite. The belt is interpreted as possibly related to a short-lived period of Late Jurassic Early Cretaceous subduction of the part of the South Anyui oceanic terrane beneath the northeastern Late Jurassic Metallogenic Belts (163 to 144 Ma; figs. 48, 49) 123 margin of the Kolyma-Omolon superterrane, after accretion of the Kolyma-Omolon superterrane to the North Asian Craton Margin (Nokleberg and others, 1994c, 1997c, 2000). Kuyul Metallogenic Belt of Podiform Cr, PGE and Associated Deposits (Belt KUY), East-Central Part of Russian Northeast The Kuyul metallogenic belt of podiform Cr and associated PGE deposits (fig. 48; tables 3, 4) occurs in the southern part of the major nappe and thrust belt of the Koryak Highlands in the east-central part of the Russian Northeast. The belt extends for more than 900 km from the Taigonoss Peninsula to the northern spurs of the Pekulney Range. The metallogenic belt is hosted in the Kuyul ophiolite, part of the Gankuvayam and Elistratov units of the Kuyul subterrane (unit TLK) of the Talovskiy subduction-zone and oceanic terrane (Nokleberg and others, 1994c, 1997c). The Kuyul ophiolite contains about 20 poorly-prospected Cr deposits in serpentinized peridotites that occur in about 50 mainly small, discontinuously exposed ultramafic bodies. The significant deposits in the belt are at Talov and Tikhorechen (table 4) (Nokleberg and others 1997a,b, 1998). These deposits consist of chromite and accessory chromium spinel that occur with PGE minerals in dunite and associated ultramafic rocks. PGE minerals, in association with gold, are hosted in serpentinite and rodingite adjacent to peridotite and dunite. Local Cu-Zn-Co-Ag sulfide minerals occur in carbonate breccias (Gorelova, 1990). Origin of and Tectonic Controls for Kuyul Metallogenic Belt The Kuyul subterrane of the Talovskiy terrane consists chiefly of tectonic sheets composed of (Nokleberg and others, 1994c, 1997c) (1) serpentinite mélange with blocks of: (a) ultramafic rock, gabbro, plagiogranite, dike suites of oceanic and subduction zone origin, and amphibolite,, (b) island arc volcanic and sedimentary deposits composed mainly of andesite, dacite, tuff; and glaucophane schist, and (c) fore-arc tuff and sedimentary rocks, (2) Kuyul ophiolite composed of harzburgite, gabbro, troctolite, wehrlite, plagiogranite, sheeted dikes, and pillow lava of Bathonian and Tithonian age (Chekov, 1982; Markov and others, 1982), (3) Kingiveem complex composed of oceanic volcanic, siliceous, and carbonate rocks of Permian, Middle and Late Triassic, and Middle Jurassic age, and (4) the Kuyul subduction-zone mélange composed of Late Jurassic and Early Cretaceous turbidite deposits, which contain Buchia and Middle Jurassic radiolarian chert. The Kulul ophiolite assemblage that hosts the Kuyul metallogenic belt is interpreted as forming either (1) during spreading of a marginal-sea basin during the early stages of island-arc formation; or (2) adjacent to a transform fault along the margin of an ocean basin (Palandzhyan and Dmitrenko, 1990). The Talovskiy subduction-zone terrane is tectonically linked to the mainly Late Jurassic and Early Cretaceous Koni- Murgal island-arc terrane (Nokleberg and others, 2000).
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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
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
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Page 125 and 126: a resource of 34.3 million tonnes o
Page 127 and 128: potassic zone. Combined estimated p
Page 129 and 130: and quartz monzodiorite stock and s
Page 131 and 132: and Omolon (OM) cratonal terranes,
Page 133 and 134: in volcanic and volcaniclastic rock
Page 135 and 136: minor calcite, and sporadic pyrite
Page 137 and 138: supergene blanket are interpreted a
Page 139 and 140: deposits and occurrences consist of
Page 141 and 142: onto the Omulevka terrane to form t
Page 143 and 144: superterrane. This belt is interpre
Page 145 and 146: to form along the leading edge of t
Page 147 and 148: quartz, and is virtually not associ
Page 149 and 150: deposits are at Terrassnoe and Kuna
Page 151 and 152: Peschanka Porphyry Cu-Mo Deposit Th
Page 153: The belt is hosted in the Late Jura
Page 157 and 158: and Early Cretaceous Koyukuk island
Page 159 and 160: The deposit consists of disseminate
Page 161 and 162: The Orange Hill deposit contains an
Page 163 and 164: 49; tables 3, 4) (Foley and others,
Page 165 and 166: locally Late Triassic marine volcan
Page 167 and 168: gold in a gangue of quartz, calcite
Page 169 and 170: Verkhoyansk granite belt, which int
Page 171 and 172: metallogenic belts are interpreted
Page 173 and 174: assemblages, which may have been mo
Page 175 and 176: during hypogene and supergene alter
Page 177 and 178: collision and regional thrusting, t
Page 179 and 180: Yur Au Quartz Vein Deposit The smal
Page 181 and 182: phase has a Rb-Sr isotopic age of 1
Page 183 and 184: sian Northeast. The belt is hosted
Page 185 and 186: Host Granitoid Rocks and Associated
Page 187 and 188: that are up to 600-1,500 m long, av
Page 189 and 190: Metallogenic Belts Formed During La
Page 191 and 192: y partly coeval plutons that range
Page 193 and 194: tion is interpreted as occuring by
Page 195 and 196: the Badzhal-Ezop and Khingan parts
Page 197 and 198: 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
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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
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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
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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
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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
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Debari, S.M., and Coleman, R.G., 19
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U.S. Bureau of Land Management Open
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Cordilleran Orogen in Canada: Geolo
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Goldfarb, R., Hart, C., Miller, M.,
Page 335 and 336:
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
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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
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Canada Annual Meeting, Saskatoon, S
Page 355 and 356:
Perello, J.A., Fleming, J.A., O’K
Page 357 and 358:
Far East—Mineralogical criteria f
Page 359 and 360:
Roeske, S.M., Mattinson, J.M., and
Page 361 and 362:
Schmidt, J.M., and Zierenberg, R.A.
Page 363 and 364:
formation occurrences: Materialy po
Page 365 and 366:
Struik, L.C., 1986, Imbricated terr
Page 367 and 368:
Valuy, G., and Rostovsky, F., 1988,
Page 369 and 370:
Wolfe, W.J., 1995, Exploration and
Page 371 and 372:
Appendix Table 1. Mineral deposit m
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Table 2 Summary of correlations and
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Table 2—Continued Unit(s) and Cor
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Table 2—Continued Unit(s) and Cor
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Table 3—Continued Metallogenic Be
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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
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Table 4—Continued Surprise Lake M
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Table 4—Continued Sredinny Metall
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