USGS Professional Paper 1697 - Alaska Resources Library

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280 Metallogenesis and Tectonics of the Russian Far East, Alaska, and the Canadian Cordillera belts contain granitic-magmatism-related deposits and are interpreted as forming during granitic plutonism associated with subduction of the Pacific Plate. (2) Rifting continues along the Gakkel Ridge (GK; northern extension of mid-Atlantic Ridge) and the extension of the ridge toward the Eurasian plate. The Gakkel Ridge and its extension define the modern boundary between the North American and Eurasian plates. Analysis of sea-floor spreading anomalies in the Eurasia Basin (eb) suggest that the Russian Northeast underwent extension from about 5 to 0.5 Ma (Moma rift episode as discussed by Fujita and others, 1990a,b, 1997; Savostin and Drachev, 1988a,b; Harbert and others, 1990; Fujita and others, 1997). The youngest change, a northward pole shift, occurred at about 0.5 Ma, as indicated by resurgent or continued thrusting (Imaev, 1991). Focal mechanism studies indicate that parts of this region are undergoing compression (Cook and others, 1986; Parfenov and others, 1989; Fujita and others, 1990a,b; Riegel and others, 1993). This compression is relieved by extrusion of the Okhotsk block to the southeast (Riegel and others, 1993) and by uplift and thrusting (Koz’min, 1984; Imaev and others, 1990; Koz’min and others, 1996). Sedimentation continues in the Amerasia Basin (ab). (3) Seismicity defines several new tectonic blocks, including the Amur, Okhotsk, and Bering blocks (Riegel and others, 1993; Fujita and others, 1997; Mackey and others, 1997). Boundaries between blocks are defined by epicenters located by teleseismic and regional networks (Fujita and others, 1997). (4) Marine and continental eruption of sparse, generally small, highly dispersed flows of Bering Strait alkaline basalt (bs) occurred in the Quaternary and Recent. This volcanism may possibly be related to dextral-wrench faulting and tectonic escape in this region. Rotation of the Bering block created extension on the Seward Peninsula and on Chukotka (Mackey and others, 1997), or the Bering block may have formed as the back-arc with respect to the Aleutian-Wrangell arc. (5) Tectonic escape (crustal extrusion) of terranes continues along major dextral-slip faults, including the Denali (DE), Nixon Fork (NF), Kaltag (KA), and companion faults (Scholl and others, 1992, 1994), that may extend into the Bering Sea. Dextral-wrench basins continue to form in association with the dextral-slip faults and are still filling with continental sediments. A thick sedimentary prism continues to form in the Aleutian-Bowers Basin (atb) (Plafker and Berg, 1994). In interior and southern Alaska, displacement continues along major dextral-slip faults, such as the Denali (DE) Fault. (6) The Pacific oceanic plate (PAC) continues to move northwestward relative to the North American Plate. Along the Aleutian megathrust (AL), plate convergence continues to vary from orthogonal in the east to oblique to transform in the west. (7) Intense tectonic disruption continues in the western part of Aleutian-Wrangell arc along the western Aleutian megathrust (AL), as a result of the transform coupling between the Pacific oceanic plate (PAC) and the North American Plate (Geist and others, 1988; Scholl and others, 1992, 1994). A thick sedimentary prism continues to form in the Aleutian- Bowers Basin (atb) that overlies a fragment of accreted Kula oceanic plate (Plafker and Berg, 1994). (8) Along the margin of southern Alaska, the eastern part of the Aleutian-Wrangell arc continues activity. Associated with the arc is mainly oblique subduction of the northern edge of Pacific oceanic plate (PAC) along the Aleutian megathrust (AL), continuing the formation of the younger part of the Prince William terrane (PW). Continuing in the Aleutian- Wrangell arc is the Alaska Peninsula and Aleutian Islands (AP) metallogenic belt, which contains granitic-magmatismrelated deposits and is hosted in the Aleutian volcanic belt. The Yakutat terrane (YA) continues to migrate northwestward and continues to underthrust the Prince William terrane (PW) along the eastern part of the Aleutian megathrust (AL). (9) Sea-floor spreading continues along the Juan de Fuca oceanic ridge (JFR). Northward movement of the Pacific oceanic plate (PAC) continues with transform displacement on the Queen Charlotte transform fault (QC). (10) The Cascade continental-margin arc continues to form. Continuing in the Cascade arc was the Owl Creek (OC) metallogenic belt that is hosted in the Cascade volcanic-plutonic belt. Associated with the Cascade arc is subduction of part of the Juan de Fuca oceanic plate (JF) and formation of a subduction-zone complex along the Cascadia megathrust (CC; Goldfinger and others, 1996, 1997; Fleuh and others, 1997). Metallogenic Belts Formed in Late Tertiary and Quaternary Continental-Margin Arcs, Kamchatka Peninsula, Southern Alaska, and Southern Canadian Cordillera Sakhalin Island Metallogenic Belt of Silica- Carbonate or Volcanic-Hosted Hg Deposits (Belt SH). Sakhalin Island, Southeastern Part of Russian Far East The Sakhalin Island metallogenic belt of silica-carbonate and volcanic-hosted Hg deposits occurs in the central and southern part of Sakhalin Island, in and adjacent to the Aniva, Nabilsky, and West-Sakhalin terranes (fig. 125; tables 3, 4) (Nokleberg and others, 1997b, 1998). The Russian name for the silica-carbonate Hg deposit type is listwandite. The silicacarbonate Hg deposits occur along or adjacent to major faults in faulted fragments of Late Cretaceous sedimentary rocks, serpentinized and altered ultramafic rocks, and in postaccretionary Neogene volcanic rocks. The significant deposits along the In’ River, and at Inskoe, Svetlovskoe, Ostrinskoe, and Yasnoe consist of cinnabar and native Hg in fracture zones along contacts between gabbroic rocks and serpentinite, or in jasper, basalt, and shale. The Hg minerals either replace quartz and carbonate in listwandite or forms pods. Some of the Hg deposits, as along the In’ River, occur in volcanic rocks but display silica-carbonate alteration. Other deposits, as at Inskoe, are hosted in altered quartzite and Neogene volcanic rock.
The origin of the Hg deposits of the Sakhalin island belt is not clear. Silica-carbonate Hg deposits are classically interpreted as related to thrust faults in or near subduction zones (J.J. Rutuba, in Cox and Singer, 1986). However, the nearest late Tertiary subduction zone occurred a few hundred km to the east, east of the Kuril arc, which has been active since the late Tertiary (Nokleberg and others, 1994c, 1997c). The Hg deposits of the Sakhalin island metallogenic belt may have multiple origins. Some of the silica-carbonate Hg deposits may have formed during late Tertiary back-arc rifting and formation of the Sakhalin-Primorye alkali basalts and related igneous rocks. Some or all of the in the belt deposits may have formed in the back arc portions of the late Tertiary through Holocene Kuril arc (Nokleberg and others, 2000). Kuril Metallogenic Belt of Au-Ag Epithermal Vein, Cu-Pb-Zn Polymetallic Vein, Sn Silica- Sulfide Vein, Sn Vein, Sulfur-Sulfide (volcanic S), Kuroko Massive Sulfide, and Porphyry Mo Deposits (Belt KU) Kuril Islands, East-Central Part of Russian Far East The Kuril metallogenic belt of Au-Ag epithermal vein, Cu-Pb-Zn polymetallic vein, Sn silica-sulfide vein, sulfursulfide (volcanic S), kuroko massive sulfide, and porphyry Mo deposits (fig. 125; tables 3, 4) occurs in the Kuril volcanic arc in the east-central part of the Russian Far East. The belt contains a wide variety of volcanic and hypabyssal-related deposits (table 4) (Nokleberg and others 1997a,b, 1998)—(1) sulfur-sulfide (volcanic S) deposits at Ebeko, Golovninskoe, Krishtofovich Volcano, Novoe, Vysokoe, and Zaozernoe, (2) Au-Ag (Zn) epithermal vein deposits at Prasolovskoe, Rifovoe, Sernaya River, and Sofya, (3) Cu- Pb-Zn polymetallic vein deposits at Dushnoe, Koshkina, and Tet’yaevskoe, (4) Sn silica-sulfide vein and Sn vein deposits at Rudnikovskoe and Spiridonovskoe, (5) porphyry Mo deposits at the Carpinsky caldera and Reidovskoe, and (6) a kuroko Cu-Pb-Zn deposit at Valentinovskoe. The principal Au-Ag epithermal vein and polymetallic, Sn, and Sn silicasulfide vein deposits are interpreted as forming during late Neogene during aerial volcanism (Shcheglov and others, 1984). The small occurrences of kuroko-type massive sulfide deposits are interpreted as forming during early Miocene seafloor volcanism. The volcanic S deposits are interpreted as forming during the construction of Quaternary volcanic cones and fields. The Au-Ag epithermal vein and the volcanic S deposits are of potential economic interest. Novoe Sulfur-Sulfide (Volcanic S) Deposit The Novoe sulfur-sulfide (Volcanic S) deposit (Petrachenko, 1967) occurs in a flat-lying sequence, about 500 to 400 m thick, of andesite, andesite-basalt, and related tuff. The sequence crops out in scarps of a 2 km-wide erosional depression. Some ore bodies are controlled by faults. The Middle Tertiary Metallogenic Belts (20 to 10 Ma) (figs. 125, 126) 281 sulfur ore occurs in hydrothermally altered silicified rock, with opalite, alunite, and kaolinite. All altered rocks in the deposit contain some sulfur, but the higher-grade ores contain opalite, silicified rock, and alunite. Secondary minerals are barite, gypsum, marcasite, pyrite (as much as 15 percent), and molybdenite. The age of mineralization is Pliocene and Quaternary. The deposit is large. Average grades are as much as 20 to 80 percent S and as much as 0.5 percent MoS 2. The deposit contains about 5 million tonnes sulfur. Prasolovskoe Au-Ag Epithermal Vein Deposit The Prasolovskoe Au-Ag epithermal vein deposit (Danchenko, 1991) consists of ore veins that are mostly steeply dipping , and range from 2 to 3 m thick, with a few as much as 10 m thick. The veins consist mainly of banded metacolloidal gold, telluride, and quartz veins that contain as much as 1-3 percent ore minerals. The deposit exhibits a vertical succession of assemblages. From bottom to top the assemblages are (1) gold-cassiterite-quartz, (2) polysulfide-quartz, (3) gold-telluride-quartz, and (4) gold-adularia (carbonate)quartz. The dominant ore minerals are pyrite, chalcopyrite, bornite, chalcocite, covellite, and sphalerite. Arsenopyrite, molybdenite, cassiterite, galena, argentite, native silver, gold, hessite, naumannite, and goldfieldite are also abundant. Limonite, covellite, malachite, and azurite occur in an oxidized zone. The ore bodies are explored to a depth of over 200 m. An area 1.5 by 0.5 km is propylitically altered and impregnated with pyrite as well as numerous quartz veinlets with epidote, sericite, adularia, chlorite, calcite, and rare barite. Earlier veinlet and disseminated ore is related to Miocene intrusions. The later Au-Ag ore is related to the Pliocene volcano-plutonic complex. The deposit is associated with Pliocene plagiogranite and quartz diorite that intrude early and middle Miocene pyroclastic green tuff deposits. The deposit is of medium size and was mined before the 1990’s. Koshkina Cu-Pb-Zn Polymetallic Vein Deposit The small Koshkina Cu-Pb-Zn polymetallic vein deposit (Petrachenko, 1978) consists of ore bodies as much as 200 m long that occur hydrothermally altered rock types outside a granodiorite and diorite intrusion. The ore bodies consist of areas of closely spaced sericitized and hydromicatized veins and veinlets with variable composition. Mineral assemblages in veins and veinlets are quartz-tourmaline, quartz-chloritesericite, chlorite-carbonate with zeolites, and quartz-chloriteepidote. The ore minerals are chalcopyrite, cleiophane, galena, stibnite, realgar, orpiment, arsenopyrite, pyrite, marcasite, hematite, and magnetite. Polymetallic and antimony-arsenic ores are spatially separated and various alterations. The mineralogy and metal content of the deposit vary widely. The deposit occurs on the northern part of Shumshu Island and covers an area of approximately 5 km2 . The deposit is hosted in heavily altered early to middle Miocene volcanic rocks that are intruded by numerous extrusive and intrusive rocks, all part of a volcano-plutonic complex. Host rocks are pro-
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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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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
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
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
Page 301 and 302: dolomite. Wall rock alteration incl
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Page 305 and 306: plates that exhibit magnetic anomal
Page 307 and 308: stages (Petrenko, 1999): (1) In the
Page 309 and 310: mon. The deposit is of medium size
Page 311: Metallogenic-Tectonic Model for Lat
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
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
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Struik, L.C., 1986, Imbricated terr
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Valuy, G., and Rostovsky, F., 1988,
Page 369 and 370:
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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Page 425 and 426:
Table 4—Continued Surprise Lake M
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Table 4—Continued Sredinny Metall
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