USGS Professional Paper 1697 - Alaska Resources Library

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212 Metallogenesis and Tectonics of the Russian Far East, Alaska, and the Canadian Cordillera Richardson lineament. Free gold occurs as interlocking alloys of native silver and gold that average 67 percent Au and 33 percent Ag. Silver sulfosalts are abundant locally and exhibit very high grades of as much as 66,000 g/t Ag. In 1989, a pilot mill produced 88,000 tonnes grading 2.2 g/t Au and 5.0 g/t Ag. The deposit is interpreted as forming during high-level emplacement of a Late Cretaceous granite porphyry along the Richardson lineament. Pogo Granitoid-Related Au Quartz Vein Deposit The Pogo deposit (Liese Zone) consists of at least two, subparallel, gently dipping tabular quartz bodies that are hosted by Proterozoic to early Paleozoic paragneiss and minor orthogneiss of the Yukon-Tanana Terrane (Lefebure and Cathro, 1999; Smith, 1999; Smith and others, 1999, 2000). The deposit contains both vein and replacements quartz bodies and consists mainly of three or more large, tabular, gently dipping quartz bodies at L1, L2, and L3. The quartz bodies, none of the bodies crop out at the surface, vary from 1 to 21 m thick, and the largest at L1 extends at least 1,300 meters along strike. The L2 quartz body underlies the eastern half of the L1 body. The quartz bodies lie from 1 to 215 m apart, range from 1 to 20 m thick (average 7 m thick), are roughly parallel, and dip from 25° to 30°. The bodies cut the foliation in the host rocks and are offset by high angle faults. The quartz bodies contain three percent sulfide minerals. The ore minerals are pyrrhotite, pyrite, loellingite, arsenopyrite, chalcopyrite, bismuthinite, various Ag-Pb-Bi±S minerals, maldonite, native bismuth, galena, and tetradymite. Native gold typically ranges from 5 to -25 microns in diameter and locally as much as 100 microns. Gold is often rimmed by native bismuth. The deposit grade ranges as much as more than 75 g/t Au over widths of several meters. High Au values are associated with high values of Bi, Te, W, As, and possibly Sn. Both white and gray quartz occur; the former is associated pyrrhotite and loellingite and is interpreted as early stage, whereas the latter is associated with arsenopyrite and pyrite and is interpreted as late stage. As of 1999, the L1 and L2 zone contained an estimated 9.05 millions tonnes grading 17.8 g/t for a total of 147,386,400 gm Au at a 3.42 g/t cutoff. Median grade for Ag in the mineralized zones is 2 g/t (Smith and others, 1999, 2000). One drill hole along steep shears and quartz-veins averaged 8.6 g/t Au for over 75 m. This area may be a possible feeder zone. The quartz is saccharoidal to polygonal. Biotite alteration envelopes as much as 0.5 m wide occur adjacent to veins and are overprinted by younger, widespread quartz-sericite stockwork and sericitedolomite alteration. The host rocks consist of highly deformed, amphibolite grade, mainly metasedimentary rocks that are intruded by diorite, granodiorite, pegmatite, and aplite dikes sills, and a granodiorite intrusion. The deposit is younger than a granite dike that exhibits a preliminary U-Pb monazite isotopic age of 107 Ma, and is older than a crosscutting diorite that has a preliminary U-Pb zircon isotopic age of 94 Ma. The Pogo deposit shares a number of characteristics with plutonic-related quartz veins in the Fairbanks district and Yukon, including a similar geological setting, a close association with Cretaceous granitoid rocks, low sulfide content, and similar geochemistry. The Pogo deposit may represent a deeper, higher-temperature part of a plutonicrelated Au system (D. McCoy, personal commun., 1999). Kantishna District At least 70 polymetallic and Sb-Au vein deposits occur in the Kantishna district in the western part of the southern Yukon-Tanana terrane in the northern Alaska Range (Bundtzen, 1981; McCoy and others (1997). The significant deposits are Sb-Au vein deposits at Caribou, Eagles Den, Slate Creek, and Stampede, and polymetallic vein deposits at Banjo, Quigley Ridge, and Spruce Creek (table 4) (Nokleberg and others 1997a,b, 1998). The polymetallic vein deposits occur in middle Paleozoic or older, polymetamorphosed and polydeformed submarine metavolcanic and metasedimentary rocks of the Yukon-Tanana terrane, which also hosts an extensive belt of middle Paleozoic kuroko massive sulfide deposits described previously (Aleinikoff and Nokleberg, 1985; Nokleberg and Aleinikoff, 1985). Most of the polymetallic vein deposits occur as crosscutting quartz-carbonate-sulfide veins and are confined to a 60-km-long, northeast-trending fault zone, which extends from Slate Creek to Stampede (Bundtzen, 1981). Mineralization occurred before, during, and after fault-zone movement as illustrated by both crushed and undeformed ore shoots in the same vein system. 39Ar-40Ar isotopic ages indicate vein formation was from 91 to 88 Ma (McCoy and others, 1997). Origin of and Tectonic Controls for East-Central Alaska Metallogenic Belt (mid-Cretaceous part) The mid-Cretaceous granitoid rocks of the older part of the Yukon-Tanana igneous belt (Moll-Stalcup, 1994), which host the older part of the East-Central Alaska metallogenic belt, occurs in large batholiths and small, isolated granitoid plutons (Foster and others, 1987; Miller, 1994). The plutons range in area from smaller than 1 km2 to larger than 300 km2 . The irregular-shaped plutons were intruded after a period of intense metamorphism and deformation in the mid-Cretaceous. The plutonic rocks exhibit K-Ar mineral, Rb-Sr whole rock, and U-Pb zircon ages that range from about 100 to 90 Ma (Wilson and others, 1994; Smith and others, 1999, 2000). The polymetallic, Sb-Au vein, and granitoid-related Au deposits of the mid-Cretaceous part of the East-Central Alaska metallogenic belt, and similar deposits in the Tombstone metallogenic belt to the east, are generally hosted in or near mid-Cretaceous granitoid plutons (Nokleberg and others, 1995a; McCoy and others, 1997; Smith, 1999, 2000) and are herein interpreted as forming during the waning stages of a major mid-Cretaceous collision of the Wrangellia superterrane with the previously accreted Yukon-Tanana terrane (Stanley and others, 1990; Dusel Bacon and others, 1993; Pavlis and others, 1993; Nokleberg and others, 2000). The collision and associated metamorphism and deformation is interpreted as forming in three phases—(1) a relatively older period of collision and thrusting, associated
with high-temperature and high-pressure metamorphism, (2) a slightly younger period of extension associated with lower greenschist facies metamorphism, and (3) intrusion of anatectic granitoid plutons and relatively younger Au quartz veins. The mid-Cretaceous granitoid rocks and relatively younger quartz veins intrude and crosscut both the relatively older, highergrade, and relatively younger, lower grade metamorphic fabrics in the region (Dusel Bacon and others, 1993; Pavlis and others, 1993). These relations suggest that the granitoid-related Au deposits of the older part of the East-Central Alaska metallogenic belt, and the Tombstone belt to the east, formed in the waning stages of this complex deformational event (Nokleberg, 1997e, 2000). Alternatively, McCoy and others (1997) interpret the mid-Cretaceous granitoid-related Au deposits as forming in a continental-margin arc related to subduction. Misused Name: Tintina Gold Belt In recent years, the name Tintina Gold Belt (as described and interpreted in a series of papers by by Goldfarb and others (2000), Flanigan and others (2000), Hart and others (2000), Mortensen and others (2000), Newberry (2000), O’Dea and others (2000), and Smith (2000) in the volume edited by Tucker and Smith (2000) has been used for granitoid-related Au deposits and occurrences in the East-Central Alaska metallogenic belt of Nokleberg and others (1995a, 1996, 1997a) and in the correlative Tombstone metallogenic belt (described below) of Nokleberg and others (1995a, 1996, 1997a) that occurs to the east in the central Yukon Territory. Because the Tintina Gold Belt actually includes a number of belts of differing ages and tectonic origins, the term is not used in this study. Bundtzen and others (2000) have introduced the term Tintia Gold Province to denote Cretaceous and early Tertiary intrusive-hosted gold deposits in East-Central Alaska and the Yukon Territory. This province includes the following metallogenic belts, which are described and interpreted in this study: East-Central Alaska (older part; ECA), Kuskokwim Mountains (KM), Tombstone (TS), and metallogenic belts (table 3). These distinct belts are separately described and interpreted herein because they (1) formed over a relatively long time span, (2) are hosted in a diverse array of host rocks, and (3) formed at different times in strongly contrasting tectonic environments, either collisional or subduction-related environments. Yukon-Tanana Upland Metallogenic Belt of Au- Quartz Vein Deposits (Belt WT), East-Central Alaska The Yukon-Tanana Upland metallogenic belt of Au-quartz vein deposits occurs in east-central Alaska (fig. 80; tables 3, 4) (Nokleberg and others, 1997b, 1998). The metallogenic belt is hosted in the Devonian and Mississippian metasedimentary and lesser metavolcanic rocks of the southern Yukon-Tanana displaced-continental-margin terrane, and in the Stikinia(?) islandarc terrane (Nokleberg and others, 1994c, 1997c). The known deposits occur in parts of these terranes that display greenschist Early Late Cretaceous Metallogenic Belts (100 to 84 Ma; figs. 79, 80) 213 facies and associated major metamorphism that ended in the mid-Cretaceous. The significant deposit is at Purdy. Purdy Au Quartz Vein Deposit The small Purdy Au quartz vein deposit (H.L. Foster, written commun., 1984; W.D. Menzie, written commun., 1985) contains a large quartz-calcite fissure vein and smaller veinlets that contain spectacular lace gold. The deposit consists mainly of this one large vein , which extends for about 2 m and is terminated by a fault. The large vein and smaller veinlets intrude mid-Paleozoic or older metasedimentary schist of the Stikinia(?) terrane. The large vein was mined out by 1960. Small veins and veinlets were mined in 1969 and early 1970’s. Origin of and Tectonic Controls for Yukon-Tanana Upland Metallogenic Belt The Yukon-Tanana Upland metallogenic belt is associated with a major, low-grade regional metamorphism and intense deformation of the Stikinia(?) and structurally subjacent Yukon-Tanana terranes in east-central Alaska (Dusel- Bacon and others, 1993; Pavlis and others, 1993; Nokleberg and others, 1994c, 1997c). As with the East-Central Alaska metallogenic belt describe and interpreted above, the Yukon- Tanana belt is interpreted as forming during the third stage of a mid- to Late Cretaceous complex deformational event that ended with intrusion of anatectic granitoid plutons and relatively younger Au quartz veins. The quartz veins crosscut a subhorizontal, schistose fabric that exhibits the younger stage of greenschist facies metamorphism. This complex event occurred during final accretion of the Wrangellia superterrane to the active margin of the North American continental margin (Plafker and others, 1989; Stanley and others, 1990; Pavlis and others, 1993; Nokleberg and others, 2000). Wrangell Mountains Metallogenic Belt of Cu-Ag Quartz Vein and Kennecott Cu Deposits (Belt WR), Eastern-South Alaska The Wrangell Mountains metallogenic belt of Cu-Ag quartz vein and Kennecott Cu deposits (fig. 80; tables 3, 4) occurs in the eastern Alaska Range, Nutzotin Mountains, and Wrangell Mountains in eastern-southern Alaska. The metallogenic belt is hosted in the part of the Wrangellia island-arc terrane underlain by Late Cretaceous and older stratified rocks, particularly the Late Triassic Nikolai Greenstone, and older late Paleozoic sedimentary and volcanic rocks (Nokleberg and others, 1994c, 1997c; MacKevett and others, 1997). The extensive suite of minor Cu-Ag quartz vein deposits occurs mainly along the northern margin of the Wrangellia sequence of Wrangellia superterrane. The major Cu-Ag quartz vein deposits are at Kathleen-Margaret, Nugget Creek, and Nikolai; the major Kennecott Cu deposits are in the Kennecott district at Kennecott and Westover; and a basaltic Cu deposit is at Erickson (table 4) (Nokleberg and others 1997a,b, 1998).
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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
Page 49 and 50:
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
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
Page 205 and 206: to the east in the central Yukon Te
Page 207 and 208: occur in a 30-km-long belt along ir
Page 209 and 210: The Emerald deposit has produced ap
Page 211 and 212: Metallogenic-Tectonic Model for Ear
Page 213 and 214: cham oceans were closed, and the Ch
Page 215 and 216: greisenized Mesozoic granite that i
Page 217 and 218: composition magmatic bodies (with a
Page 219 and 220: Origin of and Tectonic Controls for
Page 221 and 222: to Albian pelecypods (Nokleberg and
Page 223 and 224: quartz-arsenopyrite-pyrrhotite, pol
Page 225 and 226: thermally altered to siliceous and
Page 227 and 228: These ore bodies are as much as 1 m
Page 229 and 230: Eastern Asia-Arctic Metallogenic Be
Page 231 and 232: Demin, and Krasilnikov, 1974; Nekra
Page 233 and 234: 10 percent Cu, as much as 0.92 perc
Page 235 and 236: pyrite, pyrite, galena, sphalerite,
Page 237 and 238: content decreases with depth, as do
Page 239 and 240: azdelnoye, (2) porphyry Sn deposits
Page 241 and 242: Karalveem Au Quartz Vein Deposit Th
Page 243: Democrat (Mitchell Lode) Granitoid-
Page 247 and 248: chalcocite and covellite and also h
Page 249 and 250: cum-North Pacific, (2) completion o
Page 251 and 252: (6) In the Paleocene (about 56 to 6
Page 253 and 254: sists of cinnabar and metacinnabari
Page 255 and 256: Eastern Asia-Arctic Metallogenic Be
Page 257 and 258: groups of deposits are interpreted
Page 259 and 260: 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
Page 267 and 268: wim Group and altered mafic dikes.
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
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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
Page 305 and 306:
plates that exhibit magnetic anomal
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stages (Petrenko, 1999): (1) In the
Page 309 and 310:
mon. The deposit is of medium size
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Metallogenic-Tectonic Model for Lat
Page 313 and 314:
The origin of the Hg deposits of th
Page 315 and 316:
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
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
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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
Page 373 and 374:
Table 2 Summary of correlations and
Page 375 and 376:
Table 2—Continued Unit(s) and Cor
Page 377 and 378:
Table 2—Continued Unit(s) and Cor
Page 379 and 380:
Table 3—Continued Metallogenic Be
Page 381 and 382:
Page 383 and 384:
Page 385 and 386:
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Table 4. Significant lode deposits,
Page 401 and 402:
Table 4—Continued Appendix 369 De
Page 403 and 404:
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
Page 409 and 410:
Table 4—Continued Mainits Metallo
Page 411 and 412:
Page 413 and 414:
Page 415 and 416:
Table 4—Continued Whitehorse Meta
Page 417 and 418:
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Page 421 and 422:
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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