USGS Professional Paper 1697 - Alaska Resources Library

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108 Metallogenesis and Tectonics of the Russian Far East, Alaska, and the Canadian Cordillera Okhotsk oceanic plate to form the Turkuringra-Dzhagdinski (TD), Ulban (UL), and Galam (GL) terranes. Subduction and sinistral transpression occurred along the Mongol-Okhotsk suture (MO). (3) The extensive Kony-Murgal island arc (Kony-Murgal terrane (KM)) continued to form as an offshore extension of the Uda arc. Associated with the arc was subduction of part of the Ancestral Pacific oceanic plate to form the Talovskiy (TL) and Penzhina-Anadyr (PA) terranes. Inboard of the Kony-Murgal island arc (KM) were the Okhotsk (OK), Avekova (AK), and Omolon (OM) cratonal terranes that were previously rifted from the North Asian Craton (NSC), and the Viliga (VL) passive continental-margin terranes, which was previously rifted from the North Asian Craton Margin (NSV). Behind the arc were fragments of prior Devonian to Pennsylvanian island-arc COLL MONAKIN ARC - mo (BU) UMLEKAN ARC - uo SMA, KB, BD TALKEETNA ARC ? MO CG NSS uz ? WRA (PE) UL WRA (AX) UDA ARC ud TD MONGOL- OKHOTSK TL OCEAN GL KONY-MURGAL ARC KM 0 800 km 0 800 mi o o At about 25 or 45 latitude? TM, AP BONANZA ARC 80 o AK PA NSC OK ? ? NSV, KN VL BA PR OM o 25 RA MT CD BR IP CACHE CREEK WRA OCEAN CG (WR) OV BE ANCESTRAL PACIFIC OCEAN OIMYAKON OCEAN COLL MU AC YA OL (TA, KT) SOUTH ANYUI OCEAN ARG ALAZEYA ARC AL, KH o 60 terranes, including the Beryozovka turbidite-basin (BE), and Oloy (OL), and Yarakvaam (YA) island-arc terranes. (4) During the Bathonian, the Alazeya island arc, consisting of the Alazeya (AL) and Khetachan (KH) island-arc terranes, as a result of flip of the associated subduction zone, migrated towards the terranes forming the Kolyma-Omolon superterrane. The southern part of the Kolyma structural loop was formed during the convergence of the Alazeya arc toward the terranes forming the Kolyma-Omolon superterrane. The major terranes in the superterrane are the Alazeya (AL), Aluchin (AC), Argatas (ARG), Beryozovka (BE), Khetachan (KH), Munilkan (MU), Oloy (OL), Omolon (OM), Omulevka (OV), Prikolyma (PL), Rassokha (RA), Uyandina (UY), and Yarakvaam (YM) terranes. During this collision, fragments of the older part of the Angayucham oceanic plate were obducted ZL ANGAYU- CHAM OCEAN NAM KI GOOD- NEWS OCEAN NX, DL, MY 193 to 163 Ma NAC SV YT TALLY HO SINISTRAL SHEAR ZONE NAM KL METALLOGENIC BELTS AP - Alaska Peninsula CM - Coast Mountains CMN - Copper Mountain North CMS - Copper Mountain South GL - Galore GU - Guichon IP - Island Porphyry KL - Klotassin TC - Texas Creek TM - Talkeetna Mountains TO - Toodoggone QUESNELLIA ARC SM SV QN Takla Group NAC SM o 40 NAM KO UNK STIKINIA TC, CC ST ARC Hazelton GL Group TO, CMN, CM CMS, GU CACHE CREEK OCEAN Figure 47. Middle Jurassic (Toarcian through Callovian—193 to 163 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). ?
onto the Omulevka terrane to form the Munilkan (MU) ophiolite terrane, and the Uyandina, Kybytygas, and Indigirka ophiolite terranes of Oxman and others (1995). (5) The Angayucham Ocean (Kobuck Sea of Plafker and Berg, 1994), along with the South Anyui Ocean, continued to receive sparse continental-derived detritus. Previously rifted terranes, including the Kilbuck-Idono cratonal (KI) and the combined Nixon Fork-Dillinger-Mystic passive continentalmargin (NX, DL, MY) terranes, were near the North American Craton Margin. (6) The dextral-slip imbrication of the Stikinia-Quesnellia arc and associated subduction-zone terranes was completed along the Tally Ho shear zone (Hansen and others, 1990; Hart, 1995). Alternatively, the oroclinal warping of the Stikinia- Quesnellia island-arc and associated subduction-zone terranes was completed (not depicted in fig. 47; Mihalynuk and others, 1994). For either interpretation, migration of the Stikinia- Quesnellia arc and associated terranes toward North America was accomplished by subduction and (or) obduction of the Seventymile oceanic plate along the continental margin. (8) The subduction-related volcanic and plutonic arc rocks of the Quesnellia part of the arc, consisting of the Takla Group and the coeval igneous belts formed in response to continued subduction of part of the Cache Creek oceanic plate (CC; Mihalynuk and others, 1994). The Stikinia part of the arc consisted of the extensive suite of the subduction-related volcanic and plutonic arc rocks of the Hazelton Group that also formed in response to subduction of part of the Cache Creek oceanic plate. Remnants of this oceanic plate may be preserved in the terrane of ultramafic and related rocks that occurs discontinuously along the Denali strike-slip fault (DE, fig. 47) for several hundred kilometers (Nokleberg and others, 1994b). (9) Forming in the Stikinia-Quesnellia arc and continuing on from the Early Jurassic were the Coast Mountains (CM), Copper Mountain (North; CMN), Copper Mountain (South; CMS), Galore (GL), Guichon (GU), Klotassin (KL), Texas Creek (TC), and Toodoggone (TO) belts that contain either granitic magmatism-related deposits or deposits related to felsic to mafic marine volcanism. (10) Also completed was obduction of parts of the Seventymile and Slide Mountain oceanic plates onto the North American Craton Margin (NAM; Mihalynuk and others, 1994). Migration of the Stikinia-Quesnellia arc and associated terranes toward the North American Craton Margin was accomplished by subduction of the Seventymile oceanic plate along the continental-margin and by obduction. (11) Outboard and perhaps at a lower paleolatitude (either 25° or 45°), the Talkeetna and Bonanza arcs continued activity in the Wrangellia superterrane (WRA). This extensive arc formed along most of the length of the Wrangellia superterrane with coeval equivalents in the Cadwallader (CD) island arc and Methow (MT) turbidite-basin terranes. Forming in the arc and continuing on from the Early Jurassic were the Talkeetna Mountains-Alaska Range metallogenic belt, which contains kuroko massive sulfide deposits, the Alaska Peninsula (AP) Late Jurassic Metallogenic Belts (163 to 144 Ma; figs. 48, 49) 109 metallogenic belt, which contains Cu- and Fe-skarn deposits, and the Island Porphyry (IP) metallogenic belt, which contains granitic-magmatism-related deposits. Associated with the Talkeetna and Bonanza arcs was subduction of part of the Cache Creek oceanic plate to form the Chugach (CG), Bridge River (BR), and possibly Baker (BA) terranes. Late Jurassic Metallogenic Belts (163 to 144 Ma; figs. 48, 49) Overview The major Late Jurassic metallogenic belts in the Russian Far East, Alaska, and the Canadian Cordillera are summarized in table 3 and portrayed on figures 48 and 49. The major belts are as follows: (1) In the Russian Southeast, the Ariadny (AR) belt, which contains zoned mafic-ultramafic Ti deposits, is hosted in zoned mafic-ultramafic plutons intruding the Samarka subduction-zone terrane. The belt is interpreted as forming along a transform continental margin. (2) Also in the Russian Southeast is the North Bureya (NB) belt of graniticmagmatism-related deposits, which is interpreted as forming in the Umlekan continental-margin arc. (3) In the central part of the Russian Far East is the Stanovoy (ST) belt, which contains anatectic, granitic-magmatism-related deposits and is interpreted as forming during accretion of the Bureya superterrane to North Asian Craton. (4) In the Russian northeast is the Chersky-Argatass Ranges (CAR) belt of kuroko massive sulfide deposits and the Yasachnaya River (YS) belt of granitic-magmatism-related deposits. Both metallogenic belts are hosted in the Indigirka-Oloy volcanic-plutonic assemblage and are interpreted as forming in the Uyandina island arc. (5) In the Russian northeast, the Oloy (OL) belt contains graniticmagmatism-related deposits and is hosted in the Oloy island arc. (6) In the same region, the Pekulney (PK) belt, which contains basaltic Cu deposits, is hosted in Late Jurassic oceanic crustal rocks that were subsequently tectonically incorporated into the Pekul’ney subduction-zone terrane. (7) In the same region, the Tamvatney-Mainits (TAM) belt, which contains podiform Cr deposits, is hosted in zoned mafic-ultramafic plutons, and the Mainits (MA) belt, which contains kuroko massive sulfide deposits, are both interpreted as forming in the Mainitskiy island arc. (8) Also in the same region, the Svyatoy-Nos (SVN) belt, which contains Au-Ag epithermal vein deposits, is hosted in the Svyatoy-Nos volcanic belt, which is interpreted as forming in the conamed island arc. (9) In the Russian Northeast, Alaska, and the northern Canadian Cordillera, the Eastern Seward Peninsula and Marshall (ESM), Kobuk (KB), Kuyul (KUY), southwestern Alaska (SWA), and Yukon-River (YR) belts, which contain podiform Cr and related deposits and also zoned mafic-ultramafic PGE deposits, are hosted in mafic-ultramafic plutons that intruded into the basal parts of various island arcs. These arcs include the
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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
Page 89 and 90: Origin of and Tectonic Controls for
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 97 and 98: Origin of and Tectonic Controls for
Page 99 and 100: Finlayson Lake Metallogenic Belt of
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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: deposits and occurrences consist of
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 and 154: The belt is hosted in the Late Jura
Page 155 and 156: in a island arc that was tectonical
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
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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
Page 253 and 254:
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
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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
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
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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
Page 405 and 406:
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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