Metallogenesis and Tectonics of the Russian Far East, Alaska, and ...

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occur in these tabular, altered silicified rocks. The deposit occurs in a weakly-eroded volcano composed ofbasaltic andesite, andesite, and dacitic pyroclastic rocks and lava. The deposit is large and contain 0.01-0.1% Te and Au in rare high-gde zones, up to 700 g/t Au. Most of the ore is low-grade, ranging from 2-20 g/t Ail. Aginskoe Au-Ag Epithermal Vein Deposit The Aginskoe Au-Ag epithed vein deposit (Shchepo1'ev,l989f consists dominantly of fine-grained, chalcedony-like quartz, adularia, and hydromica with colloform banding. The ore minerals comprise 0.3 to 1.0% of veins. The major ore minds are tellurides, including hessite, altaite, calaverire, silvanite, and pewe. A total of 55 ore minerals are identified. Ooldfineness ranges from 740 to 990, and the AdAg ratio varies from 2: 1 b 7:i. Six stages of me deposition we rewgnk&: (1) quartz-pyrite; (2) gold-adularia-corrensite-quartz with a gold fineness of 924 to 968; (3) gold-adulariaquam with a gold fineaesa, of 936 to 952 at upper levels, and a gold fineness of 740 to 854 at deeper IcveL; (4) gold-calaverite-quartz with a gold fkxms 940 to P60; (5) gold-hessite-corrensite-quartz with a gdd frneness 8 16 to 880 ~d (6) quartz-~eolite-calcite. End~gen~ zg&g is mared by a vertical change of ore compositian, texture, and structure. The concentrarioa of tellurides and dfidw increwses with depth. The deposit occurs in a volcanic caldera composed of Miocene basaltic andesile and basaltic andtsite luff:. Ore occurs in kchire zones and zones of intense jointing. Ore-beanng stnrctlves COW& of ~ hbnd r breccia tectonic zones, which include nutmrmu a~degitk dikes and veins, lenses, and veimlets of &laria-quartz and qlum-tzcdnate composition. Tbe main ore-b$&fing mcs tire the Aginskaya and Surpriz. In the main ore-bearing me short we bodies merge at deptb formiag a gently-dipping rnhedkd band; complicated in the upper p t by steeply-wig ore shook Hydrothermal alteration, c o d y propylitic, is oammon. The deposit is of medium size andconlains an estimated rcsourca of 30-50 toms Au and 70-100 tonnes Ag. The average grade Of the Aginskoe deposit is 20 g/t Au. The deposit is currently under development. Kirganik Porphyry Cu Deposi? The Kirganik porpbyry Cu dspasir (Vhov, 1977; AV. Iptyev, written commun., 1980) e o n of ~ ekeplydipping zones of rocks with biotite-K-feldspar sonret re tic alteration. The deposit is 10-15 m thick, up to 1200 rnlofig? rradoccm in Late Cretaceous siliceous volcanic rocks. The deposit consirhs of zones of disoeminatted and veinlet capper aod Au minds. The ore bodies are generally conformablt with Ihe host FQC~. The oxidizad zone extends deepest in heavily h%md rocks, to a depth of 100 to 120 m, and contains up b 0.8 g/t Au. Tbe richest ore is in biotite-K-feldspar--matically altered rocks. Altered rocks containing both pyroxene aod K-feldspar are pctieally devoid of ore. Tbe ore minerds are pyrite, chalcopyrite, magnetite, bomite, chalcocite, hematite, and gold The richest Au values occur in ri& chalcosite-chalcopyrite-bomk ore with more than 1% Cu. The K-Ar isotopic age ofthe biotitebl-f 1dJpar-altered rocks which hoet the ore is 65-75 Ma. The deposit is of d u m size. Average grades are 0.1 - 1% Cu and 0.2 to 0.4 gh Au in disseminatd and veinlet ore, and up to 0.8 g/t Au m oxictiztd ore. Origin of and Tectonic Controls for Central Kamchatka Metallogenlc 664 The Central Kamchatka volcanic and sedimentafy basin (Nokleberg and others, 1994c, 1997~) which hosts the Central Kamchatka metallogenic belt consists chiefly of late Otigocene to Holecene volcanic and sedimenm rocks in saqt&ace~ up to 5 krn thick. The belt ranges from 20 to 70 km wide and is about 350 km long. The volcanic and s-rttary basin a b contak mainly shallow-marine sedimentary rocks up to 6,000 m thick, and widespread tuff, basalt, and basaltic mhite. Thre basid units overly deformed Late Crekeou to early Tertiary sedimentary rocks. The bssin is intqreted as a fmarc unit of the Ceutral Karnchatka volcanic belt; both we interpreted as parts of the major, post-accretionary, Northeast Asia mtinmtal-rnar@ arc ira the Russian Far East (Noklebetg and othm, 1994c, 1997~). Alaska Peninsula and Aleutian Islands Metallogenic Belt of Igneous Arc Depeab (Belt AP) Western-Souttmn Alaska The major Alaska Peninsula and the Aleutian lslands metallogenic belt of igneous arc dqxxits (fig. 126; table8 3,4) occurs in western-southern Alaska (Nokleberg and others, 1995a). The metallogenic belt is b d in the arc41 uderhh fx adjacent to the middle and late Tertiary granitic and volcanic rock of the Aleutian arc in the t~tetn Ahtim L W and the southwestern Alaska Peninsula (Nokleberg and others, 1994c, 1997~). The arc is composed mainly of middle Tcrtisry to Ho1andesite to dacite flows and tuff, sshiallow intrusive rocks, small silicic stocks and sills, and associated setiimerrtary rocks (Buik, 1965; Wilson, 1985). Underlying parts of the southwestern Alaska Peninsula, almost as far west as Cold by, is the mainly Mesozoic bedrock of the Peninsular island-arc terrae. Numerous epithed vein, polyrnetallic vein, add porphyry Cu and Cu-Mo deposits occur in the metdogenic kit. The significant deposlts are (tahle 4) (Nokleberg and others 1997a, b, 19%): epithed vein deposits at ApoH8-SiUra, Aquila, Canoe Bay, Fog Lake (Pond), Kuy, Shumagin, and San Diego Bay; po1ymetallic vein deposits at Braided CR&, M a (Biorka), Cathedral Creek, and Kilokak Creek; and porphyry Cu and MO deposits at Bee Creek, Mallard Duck Bay, Mike, m d , Rex, and Sedanka (Biorka). The eplthermal and polymetallic vein and porphyry deposits of the Alaska Peninsula trad AIP;uh lsladds
elt occur over a distance of over 800 km. This belt is related to the epithermal and hydrothermal activity associated with the late- magmatic stages of Tertiary and Quaternary hypabyssal plutonic and associated volcanic centers. These centers are along part of the Aleutian arc, one of the classic continental-margin arcs along the rim of the Circum-Pacific rim. Pyramid Porphyry Cu Deposit The Pyramid porphyry Cu deposit (Armstong and others, 1976; Hollister, 1978; Wilson and Cox, 1983; G.L. Anderson, written commun., 1984; R.L. Detterman, oral cornrnun., 1986) occurs in the southwestern Alaska Peninsula and consists of disseminated molybdenite and chalcopyrite(?) in a Fe-stained dacite porphyry stock of late Tertiary age. A zonal alteration pattern is defined by a core of secondary biotite, containing about 3 to 10% magnetite, which grades outward into an envelope of quartz- sericite alteration. Fractures adjacent to the stock are filled with sericite. Local extensive oxidation and supergene enrichment by chalcocite and covellite occur in a blanket as much as 100 m thick. The deposit is centered on a 3 km2 area within the stock, and contains a resource of 110 million tonnes grading 0.4% Cu, 0.03% Mo, and trace of Au (G.L. Anderson, written commun., 1984). The host stocks and dikes, and several smaller stocks which occur nearby all intrude the fine-grained clastic rocks of the Late Cretaceous Hoodoo Formation, and the Paleocene or Eocene to Oligocene Stepovak(?) or Tolstoi(?) Formation. The sedimentary rocks are contact metamorphosed adjacent to the stocks. Bee Creek Porphyry Cu Deposit The Bee Creek porphyry Cu deposit consists of chalcopyrite, pyrite, and traces of molybdenite in contact-metamorphosed Jurassic and Cretaceous sedimentary rocks which are intruded by a small tonalite porphyry stock of Tertiary age (Cox and others, 198 1). The deposit, located on the Alaska Peninsula 25 km northeast of Chignik Lagoon, was discovered by Bear Creek Mining Company in cooperation with Bristol Bay Native Corporation in the late 1970's (E.D. Fields, written cornrnun., 1977).The contact-metamorphosed sedimentary rocks and the porphyry stock exhibit strong potassic (biotite) alteration, and quartz grains in the porphyry contain abundant, high-salinity fluid-filled inclusions. The deposit is unexplored on the southwest and northeast sides and probably contains a resource of between 5 and 30 million tonnes with average grade between 0.1 to 0.4 percent Cu. Five drill holes totaling 2,359 m explore the deposit; one hole intercepted 150 m averaging 0.25% Cu. Aleutian Arc The Aleutian arc, which hosts the Alaska Peninsula and Aleutian lslands metallogenic belt, is composed of Oligocene (post-30 Ma) to Holocene andesite to dacite flows, tuff, and intrusive and extrusive breccia; hypabyssal diode and quartz diorite and small silicic stocks, dikes, and sills; and volcanic graywacke, shale, and lahars (Burk, 1965; Wilson and Cox, 1983; Wilson, 1985; Wilson and others, 1993; Vallier and others, 1994). To the northeast on the Alaska Peninsula, magmatism apparently started in the late Miocene (about 15 Ma). An older Eocene and Oligocene succession of igneous rock that yields K-Ar ages ranging h m 40 to 30 Ma, is located in the northeastern Aleutian Islands and is defined as the Meshik arc by Wilson (1985). Petrologic, chemical, and isotopic characteristics of the Aleutian arc (Miller and Richter, 1994) are as follow^. (1) The arc consists predominantly of andesite and low-silica dacite; rhyolite occurs only in a few volcanic centers. (2) The axial part of the central and northeastern parts of the arc is mostly calc-alkalic; SiOz contents typically range between 50 to 78 percent. (3) Volcanic centers to the southwest are either tholeiitic or transitional to calc-alkalic. (4) The back arc contains alkalic volcanic rocks which occur in widely separated centers. And (5) initial Sr ratios are relatively low, in the range of 0.70305 to 0.7046. The lode deposits of Alaska Peninsula and Aleutian Islands metallogenic belt reflect the bedrock underlying tbe arc. The northeastern part of the arc on the southwestern part of the Alaska Peninsula is underlain by Mesozoic bedrock of the Peninsular terrane, part of the Wrangellia superterrane (Wilson and Cox, 1983; Nokleberg and others, 1994d). On the Alaska Peninsula, the Peninsular terrane consists of a Late Triassic(?) and Early Jurassic sequence of volcaniclastic and volcanic rocks (Talkeetna Formation), the Middle Jurassic part of the Alaska-Aleutian Range batholith (Reed and Lanphere, 1969, 1973), and younger Cretaceous sedimentary rocks. In contrast, to the southwest, the Aleutian arc is interpreted to be underlain by oceanic crust (Wilson and Cox, 1983; Vallier and others, 1994). The Pyramid Bee, Creek, Rex, and Warner Bay porphyry Cu deposits in the central part of the metallogenic belt occupy a transitional zone between the parts of the magmatic arc underlain by oceanic crust to the southwest and by continental crust to the northeast. Some of the deposits to the northeast are Mo-rich and contain anomalous concentrations of Bi, Sn, and W which may be characteristic of continental-margin deposits (Wilson and Cox, 1983). K-Ar isotopic studies indicate a variable time span of up to two million years between igneous activity and mineralization. Isotopic studies also indicate sporadic occurrences of mineralization during a long period of igneous activity (Wilson and Cox, 1983). Tectonic Setting for Alaska Peninsula and Aleutian lslands Metallogenic Belt The Aleutian arc, one of the classic igneous continental-margin arcs along the Circum-Pacific rim, occurs structurally above the Aleutian megathrust, an active subduction zone which dips to the northwest and along which the Pacific Plerte is being thrust under the southern margin of Alaska (fig. 126). The tectonic setting, and the field, petrologic, chemical, and isotopic data is'- -=_"
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I EUSGS science Ior a changing wwld
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CONTENTS Abstract .................
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5 : 3 . Kedon metall lo genic Belt
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Parson and Brisco Barite Vein and G
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Overview ..........................
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Chepak Granitoid-Related Au Deposit
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Origin of and Tectonic Controls for
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Au-Ag Epithermal Vein Deposits Asso
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Metallogenesis and Tectonics of the
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and Byalobzhesky (1996). A volume c
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1,079 significant mineral deposits
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Acknowledgements We thank the many
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0 --mmm=oRuwrrrur ommmmarUaAll NEr-
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Figure 3. Generalized map of mtljor
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Archean granulite facies metamorphi
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Figure 5. Oroek sediment-h section
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1 a a - --rich sandstone ~b-Qmg@ner
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Origin of and Tectonic Setting for
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occur in clastic and impure carbona
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Figure 7. Sullivan sedimentary-exha
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I 1997a, b, 1998). The massive sulf
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Ma which locally form extensive plu
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Figure 10. Gerbikanskoe vdcanogenic
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from crystalline basement of craton
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Figure 13. Howards Pass sedknenWy e
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McLean Arm Porphyry Cu-Mo District
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[..'......I Surfia'al deposits (Hol
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Figwe 16. GeneraCied map of major M
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.- *.-* *. . - - ---- -A - EARLY MI
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Metallogenic Belt Formed During Col
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several tens of meters to 1,300 m l
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Goldfarb (197) who interprets that
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WTF and Red Mountain Kuroko Massive
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interpreted by and as part of a ext
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Mount Sicker Metallogenic Belt of K
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interpreted as vents. The deposit c
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hosted in the Yarkhodon subterrane
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origin of the younger Triassic(?) B
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Mississippian age of mineralizalioi
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Monger and Nokleberg, 1996; Noklebe
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1997a, b). Most of the magnesite an
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FL - Finlayson Lakm FR-FmLake LI -
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disseminations in chert, disseminat
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U F~gure 32 GemMzed m p of mejw -ni
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terrane, and by the Stikine Assembl
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Metallogenic-Tectonic Model for Lat
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. I . r ; 4 ~ (9) During subduction
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Eastern Alaska Range Metallogenic B
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individual flows range from 5 cm to
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occurrence of turbiditic clastic ro
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along the with tectonically-related
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: m- 3- w43 k M- u m u~u) mtl 'M~!A
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island-arc volcanic rocks of the Ni
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-- - //// EpldoW Figure 41. Nickel
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(TC), and Toodoggone (TO) belts whi
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(4) The Angayucham Ocean (Kobuck Se
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lueschist units and the McHugh Comp
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Figure 46. Lawyers Au-Ag epitiefmel
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(5) The Angayucham Ocean (Kobuck Se
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Figure 49 Generaltzed map Of mbjm L
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continental-margin terranes which w
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Pokrovskoe Au-Ag Epithermal Vein De
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Granite-porphm and wanits W e ~~ hl
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subordinate adularia, dolomite, cel
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shale, basalt, plagiorhyolite, silt
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ocks and serpentinite which occur a
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interpreted as forming in the Juras
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Fault / Figure 57. Bond Creek and O
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Klukwan-Duke Metallogenic Bett of M
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tonnes of ore mined between 1967 an
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Cariboo Metallogenic Belt of Au Qua
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Sheep Creek Au-Ag Polymetallic Vein
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---. .% of the North American Conti
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- OwiapaasembC Cmhmmmand Cemmcl. an
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in the west-central part of the Rus
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for about 850 krn (ZalishshaL ad oh
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Stanovoy Metallogenic Belt of Grani
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Goryachev, 1995, 1998, 2003) consis
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Altinskoe, Aragochan, Dalnee, Dokhs
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comprises up to 70-80% in some ore
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The Au quartz vein deposits are int
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leucogranite plutons form large, ho
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+ , . Diorite phyry dike (Early ~ta
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- . --- Origin of and Tectonic Cont
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Britannia Metallogenic Belt of Kuro
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Specific Events for Late Early Cret
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Figure 73. Solnechnae Sin qu- ~d~ n
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- Origin of and Tectonic Controls f
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Nome Metallogenic Belt of Au Quartz
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quartz vein deposits of the Souther
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Selwyn Plutonjc Suite. The host roc
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along the western end in the Eagle
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101 Ma (K.M. Dawson, unpublished da
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I Bayonne Metallogenic Belt of Porp
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., (VV) belts. These zones and beb
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I (2) The East Sikhote-Alin (es) co
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Metallogenic Belt Formed in Late Me
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The Pb-Zn polyrnetallu: vein depb a
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olistolith. The deposit is currentl
Page 222 and 223:
the core of the veins, chlorite, Mn
Page 224 and 225:
Tayozhnoe Ag Epithermal Vein Deposi
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Figure 90. lskra deposit Sn polyrne
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- El (Late ~re&ceous) I+ we cmm=s)
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Figure 93. Mnogovershinnoe AMq @pWw
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immed by wehrlite, olivine-magnetit
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Eastern Asia-Arctic Metallogenic Be
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which would be hosted in the early
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Etandzha Porphyry Cu-Mo and Muromet
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0- / Fadt . . Au veins and pods Fig
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Sentachan Clastic-Sediment-Hosted A
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I I I Undifferentiated vdcanic and
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.r . : . -d ' . . ,, $44 . assembla
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closure, the Chukotka supertca&c wa
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- Mgh anglefau#or prsminant Fitwar
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intrude and crosscut both the relat
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Figure 101 8. Ke~ecolt &4W d KemwaI
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Figure 103. Generalized map of majo
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metallogenic belt (SP) which contai
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Eastern Asia-Arctic Metallogenic Be
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Valunistoe Au-Ag Epithermal Vein De
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Lost River Sn-W Skarn and Sn Greise
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Wheeler Creek, Clear Creek, and Zan
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Au veln,and hots spring deposits at
Page 270 and 271: Chicken Mountain Cu-Au Deposit The
Page 272 and 273: Chip sample location - Fault / Cont
Page 274 and 275: A proximate laatbm c#f C h # d ~nar
Page 276 and 277: 0.03 1% Mo; and (3) for a hypogene
Page 278 and 279: others, 1994c. 1997~). The granitoi
Page 280 and 281: Cross section - - South greisen zon
Page 282 and 283: Origin of and Tectonic Controls for
Page 284 and 285: 198 1). The mine at the deposit pro
Page 286 and 287: Beatson (Latouche) and Ellamar Bess
Page 290 and 291: CRETACEOUS Mount Leonard St& gueYtr
Page 292 and 293: n pJ pRanens. Pd-dc i3 Meeomic .---
Page 294 and 295: Figure 120. Huckleberry porphyry Cu
Page 296 and 297: 0.15% Cu (ox), 0.127 g/t Au, and 0.
Page 298 and 299: Zone are 188 million tonnes grading
Page 300 and 301: Kitsault (B.C. Moly) Porphyry Mo De
Page 302 and 303: million tonnes grading 0.42% Cu, 0.
Page 304 and 305: extension. The Coryell Suite is int
Page 306 and 307: elated deposits. Forming in the bac
Page 308 and 309: Metallogenic Belts Formed in Tertia
Page 310 and 311: Hg Deposits Hg deposits occur throu
Page 312 and 313: Maletoivayam Sulfur-Sulfide Deposit
Page 316 and 317: (5) A major orthogonal junction for
Page 318 and 319: Metallogenic Belts Formed in Tertia
Page 322 and 323: summarlzed above are used by analog
Page 324 and 325: the Aleutian volcanic belt. The Yak
Page 326 and 327: metamorphism, anatectic granites, a
Page 328 and 329: References Cited Abbott, G., 1981,
Page 330 and 331: Society of America Abstracts with P
Page 332 and 333: Sciences, North-Eastern lnterdiscip
Page 334 and 335: Burgoyne, A.A., 1986, geology and e
Page 336 and 337: Canadian Cordillera, Yukon-northeas
Page 338 and 339: the Koryak Highlands: Transactions
Page 340 and 341: during 1984: U.S. Geological Survey
Page 342 and 343: Northeast Scientific Intergrated Re
Page 344 and 345: House, G.D., and Ainsworth, B., 199
Page 346 and 347: International Field Conference in V
Page 348 and 349: lithosphere in flood basalt genesis
Page 350 and 351: MacKevett, E.M., Jr., 1978, Geologi
Page 352 and 353: Miller, M.L., Bundtzen, T.K., and K
Page 354 and 355: Nekrasov, I.Ya., 1995, Genetic type
Page 357 and 358: Pakhomova, V.. Silyanik, V., Popov,
Page 359 and 360: Pollack, John, 1997, Summary report
Page 361 and 362: 1993: British Columbia Geological S
Page 363 and 364: Schroeter, T.G., 1987, Golden Bear
Page 365 and 366: Geology of the Liese zone, Pogo pro
Page 367 and 368: Colorado, Geological Society of Ame
Page 369 and 370: lnstitute of Mining and Metallurgy
Page 371 and 372:
Anorthosite apatite-Ti-Fe Gabbroic
Page 373 and 374:
TABLE 2. Summary of correlations an
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TABLE 2. Summary of correlations an
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9! TABLE ectonic environment of Pro
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(Abbreviation) Rassokha (RA) Dzhard
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Metallogenic Belt (Abbreviation) Be
Page 383 and 384:
Major Mineral Deposits Types. Envir
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(Abbreviation) Guichon (GU) I Belt
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Major Mineral Deposits Types. Envir
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(Abbreviation) (Significant Mineral
Page 391 and 392:
(Abbreviation) Adycha-Taryn (EAAT)
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~etallo~enic Belt Major Mineral Dep
Page 395 and 396:
Metallogenic Belt (Abbreviation) Ca
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TABLE 4. Significant lode deposits,
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Mineral Deposit Model Major Metals
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Deposit Name Mineral Deposit Model
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Deposit Nmme Mineral Deposit Model
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p;. ;A'..* Deposit Name Mineral Dep
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De~osit Name Mineral Deposit Model
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