USGS Professional Paper 1697 - Alaska Resources Library

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48 Metallogenesis and Tectonics of the Russian Far East, Alaska, and the Canadian Cordillera tallic vein, and skarn deposits, occurs in the core of the Brooks Range in northern Alaska (Nokleberg and others, 1995a, 1997b, 1998). The metallogenic belt is hosted in the Coldfoot, Hammond, and North Slope terranes of the Arctic Alaska superterrane (Moore and others, 1992, 1994; Nokleberg and others, 1994c, 1997c). The belt is discontinuous but extends for over 900 km along the length of the Brooks Range. The significant deposits in the belt are: the Mount Igikpak and Arrigetch Peaks polymetallic vein, Au quartz vein, Sn skarn, Cu-Pb-Zn skarn deposits; the Ann (Ernie Lake), Galena Creek, Porcupine Lake, and Romanzof Mountains polymetallic vein deposits; the Jim-Montana Cu-Zn skarn deposit; the Sukakpak Mountain Sb-Zu vein deposit; the Victor, Venus, Evelyn Lee, and Ebo porphyry Cu and Cu skarn deposits; the Geroe Creek porphyry Cu-Mo deposit; the Esotuk Glacier Pb-Zn skarn and fluorite vein deposit; and the Bear Mountain porphyry Mo deposit (table 4) (Nokleberg and others 1997a,b, 1998). These significant deposits occur in two groups described below—a major group in the central Brooks Range, and a minor group in the northeastern Brooks Range. In the northeastern Brooks Range, the belt is sometimes referred to as the Chandalar belt (Newberry and others, 1997a,b). Vein, Skarn, and Porphyry Deposits Central Brooks Range Significant deposits in the central Brooks Range part of the belt are at Mount Igikpak and Arrigetch Peaks, Sukakpak Mountain, Victor, and Geroe Creek. These deposits include polymetallic quartz veins containing base-metal sulfides, Sn skarns containing both disseminated cassiterite and base-metal sulfides, Cu-Pb-Zn skarns containing disseminated Fe and base-metal sulfides, and porphyry Cu and Mo deposits (Nokleberg and others, 1995a). The Victor and associated porphyry Cu and Cu skarn deposits at Venus, Evelyn Lee, and Ebo (DeYoung, 1978; Donald Grybeck, written commun., 1984; Newberry and others, 1997a) consist of veinlet and disseminated chalcopyrite, bornite, molybdenite, and pyrite in schistose Devonian granodiorite porphyry that intrudes either the Silurian and Devonian Skajit Limestone or older marble, calc-schist, and pelitic schist. The skarn minerals are mainly garnet, magnetite, and diopside, and retrograde vein and replacement epidote, amphibole, chlorite, calcite, and quartz. The skarns were subsequently regionally metamorphosed during the Mesozoic. Skarns in marble adjacent to plutonic rocks contain vugs with interstitial bornite, chalcopyrite, bornite, chalcocite, pyrite, magnetite, and some digenite. Zones in granitoid rocks as much as 30 m wide contain as much as 0.4 percent Cu. Grab samples of skarn contain as much as 5.5 percent Cu, 0.41 g/t Au, and 0.29 g/t Ag. The felsic-magmatism-related deposits in the central Brooks Range are hosted in a structurally complex and polymetamorphosed assemblage of Devonian or older carbonate rocks, including Silurian and Devonian polymetamorphosed limestone, calc-schist, quartz-mica schist, and quartzite, which is intruded by mainly Late Devonian gneissic granitoid rocks that together with the metasedimentary rocks constitute the Hammond passive continental margin terrane of the Arctic Alaska superterrane (Moore and others, 1992). Skarn, Vein, and Porphyry Deposits Northeastern Brooks Range Significant deposits in the Brooks Range metallogenic belt in the northeastern Brooks Range are a cluster of Pb- Zn skarn, fluorite vein, polymetallic vein, and porphyry Cu deposits at Esotuk Glacier, Porcupine Lake, Romanzof Mountains, and Galena Creek (Nokleberg and others, 1995a). This part of the belt is sometimes referred to as the Chandalar belt (Newberry and others, 1997a,b). The Romanzof Mountains polymetallic vein and Pb-Zn skarn deposit (Brosge and Reiser, 1968; Grybeck, 1977; Sable, 1977; W.P. Brosge, oral commun., 1984; Newberry and others, 1997a) consists of numerous scattered mineral occurrences of polymetallic sulfides. The most common types of deposits are (1) zones of disseminated galena, sphalerite, chalcopyrite and pyrite, locally with Au and Ag, in Devonian(?) granite, (2) Pb-Zn skarn in marble with disseminated magnetite, pyrite, pyrrhotite, sphalerite, and galena in gangue of carbonate, clinopyroxene, epidote, amphibole, beryl, tourmaline, and fluorite, (3) disseminated galena, sphalerite, chalcopyrite, and (or) molybdenite in quartz veins along sheared contact in in Devonian(?) granite, and (4) local fluorite greisen in in Devonian(?) granite. Grab samples contain as much as 0.15 percent Sn. The skarns and quartz veins occur in Precambrian marble and calc-schist of the Neruokpuk Quartzite at the periphery of the Silurian or Early Devonian Okpilak (granite) batholith. These felsic-magmatism-related deposits are hosted in a variety of Paleozoic and late Proterozoic metasedimentary rock that consist mainly of marble, calc-schist, limestone, quartzite, and greenstone of the North Slope passive continental margin terrane (part of the Arctic Alaska superterrane) that were intruded by Devonian gneissose granite plutons (Newberry and others, 1997a). The paucity of deposits in the northeastern Brooks Range most likely reflects the limited geological exploration of the area. Although not part of this metallogenic belt, a nearby porphyry Mo deposit in this area at Bear Mountain consists of molybdenite- and wolframite-bearing Tertiary(?) granite porphyry stock (Barker and Swainbank, 1986). The stock intrudes the Late Proterozoic(?) Neruokpuk(?) Quartzite, and the Tertiary(?) isotopic age for the stock may be a reset Devonian age. If so, the Bear Mountain deposit would be part of the Brooks Range metallogenic belt. Origin of and Tectonic Controls for Brooks Range Metallogenic Belt Field, chemical, and isotope data indicate the granitic magmatism deposits in the Brooks Range metallogenic belt formed during intrusion of the Devonian gneissic granitoid rocks (Dillon and others, 1987; Nokleberg and others, 1995a). High initial Sr ratios (about 0.715) and Pb and Sm-Nd isotopic studies indicate the presence of an older, inherited crustal component (about 1,000 to 800 Ma) and involvement of Proterozoic or older continental crust in the genesis of the plutons (Dillon and others, 1987; Nelson and others, 1993; Miller, 1994; Moore and others, 1994). U-Pb zircon and Rb-Sr isotopic studies indicate
intrusion from about 402 to 366 Ma (Dillon and other, 1987; Moore and others, 1994). Most of the gneissic granitoid plutons contain a moderately to intensely developed, subhorizontal to gently dipping schistosity that formed during lower greenschist facies metamorphsim. K-Ar, and incremental Ar studies indicate that mid-Cretaceous greenschist metamorphism was superposed on older blueschist facies metamorphism (Dusel-Bacon and others, 1993; Moore and others, 1994). These field, petrologic, chemical, and isotopic data indicate that the Brooks Range metallogenic belt and associated Devonian gneissic granitoid plutons formed along a Devonian continental-margin arc that developed above a subduction zone (Newberry and others, 1997a; Nelson and others, 1993; Miller, 1994; Moore and others, 1994; Nokleberg and others, 1995a, 2000). U-Pb zircon isotopic ages indicate that the Devonian gneissic granitoid rocks intruded about 30 to 40 m.y. after the eruption of the submarine volcanic rocks that host the kuroko massive sulfide deposits to the west in the Arctic metallogenic belt (Newberry and others, 1997a; Nokleberg and others, 1997a) described above. Herein the Brooks Range metallogenic belt is interpreted as the axial arc part of a continental-margin arc in which the Arctic metallogenic belt of kuroko massive sulfide and associated deposits formed in the back arc. Regional tectonic analyses also suggest that the Devonian igneous of the Brooks Range are part of a discontinuous Devonian continentalmargin arc that extended along the margin of the North American Cordillera (Rubin and others, 1991; Nokleberg and others, 1994c, 1997c, 2000; Plafker and Berg, 1994; Goldfarb, 1997). An alternative interpretation by Goldfarb and others (1997, 1998) proposes that some of the deposits in the Arctic metallogenic belt formed during subsequent rifting, as indicated by Pb isotope data reported by Dillon and others (1987). Alaska Range and Yukon-Tanana Upland Metallogenic Belt of Kuroko Massive Sulfide Deposits (Belt AKY) Central and East-Central Alaska The Alaska Range and Yukon-Tanana Upland metallogenic belt of kuroko massive sulfide deposits (fig. 17; tables 3, 4) occurs in the central and eastern Alaska Range in the southern part of the Yukon-Tanana metamorphosed continental margin terrane. The massive sulfide deposits extend for 350 km along strike on the northern flank of the Alaska Range and constitute one of the longer belts of massive sulfide deposits in Alaska. The significant deposits are WTF, Red Mountain, Sheep Creek, Liberty Bell, Anderson Mountain, Miyaoka, Hayes Glacier, McGinnis Glacier, and in several deposits in the Delta district (table 4) (Newberry and others, 1997; Nokleberg and others 1997a,b, 1998). Bonnifield District of Kuroko Massive Sulfide Deposits In the Bonnifield district along the Wood River drainage, the best-studied deposits are at Anderson Mountain, WTF, and Red Mountain. Twenty sulfur isotopic analyses from seven stratiform deposits in the Bonnifield district indicate enrichment by heavier sulfur during deposition, typical of many Middle and Late Devonian Metallogenic Belts (387 to 360 Ma; figures 16, 17) 49 volcanogenic massive sulfide deposits (Gilbert and Bundtzen, 1979; Newberry and others, 1997). One lead isotopic analysis from the Anderson Mountain deposit yielded a single-stage lead age of 370 Ma (Devonian). Anderson Mountain Kuroko Massive Sulfide(?) Deposit The Anderson Mountain kuroko massive sulfide(?) deposit (Gilbert and Bundtzen, 1979; Curtis J. Freeman, written commun., 1984; Newberry and others, 1997a) consists of massive sulfide layers with pyrite, chalcopyrite, galena, sphalerite, enargite, and arsenopyrite in gangue of quartz, sericite, chlorite, calcite, barite and siderite. The deposit is hosted in metamorphosed marine tuffaceous rhyolite and metamorphosed calcareous clastic rocks that are correlated with the Moose Creek Member of the Mississippian(?) Totatlanika Schist. Numerous high-angle faults cut the deposit. The massive sulfide beds lie on an irregular paleosurface in footwall with domal sulfide accumulations. The absence of footwall alteration and stringer mineralization suggests off-vent deposition. Grab samples contain as much as 19 percent Cu, as much as 5 percent Pb, 28 percent Zn, and 171 g/t Ag. High geochemical values of As, Sb, Hg, and W may be derived from underlying schist. WTF and Red Mountain Kuroko Massive Sulfide Deposit The WTF and Red Mountain Kuroko massive sulfide deposits (Gilbert and Bundtzen, 1979; David R. Gaard, written commun., 1984) consist of massive pyrite, sphalerite, galena, and chalcopyrite in a quartz-rich gangue. The sulfides are hosted in in felsic metavolcanic rock derived from crystal and lapilli tuff, minor flows, and metasedimentary rock. The stratiform massive sulfide layers occur on both sides of a large, east-west trending syncline. The massive sulfide layers at Red Mountain occur in a proximal setting on the south limb of the anticline, and occur in a sulfide-silica exhalite that is as much as 130 m thick. An older, southern horizon contains sphalerite and coarse pyrite in black chlorite schist. The WTF deposit occurs on the north limb of the antiform and consists of a thin blanket of fine-grained sulfides that are interpreted as having formed in a distal setting relative to the vent. The WTF deposit contains an estimated 1.10 million tonnes grading 0.15 percent Cu, 2.5 percent Pb, 7.9 percent Zn, 270 g/t Ag, and 1.9 g/t Au. The deposits occur immediately below the Sheep Creek Member and above the Mystic Creek Member of the Mississippian(?) Totatlanika Schist. Delta District of Kuroko Massive Sulfide Deposits The best-known kuroko massive sulfide deposits of the Alaska Range and Yukon-Tanana Upland metallogenic belt are part of the Delta district in the eastern part of the Alaska Range (fig. 23). The district and large massive sulfide deposits have been described by several authors (Nauman and others, 1980; Lange and Nokleberg, 1984; C.R. Nauman and S.R. Newkirk, written commun., 1984; Lange and others, 1990, 1993; Newberry and others, 1997a). The district comprises an area of about 1,000 km 2 . The district contains about 26
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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
Page 29 and 30: xxviii 36. Wellgreen gabbroic Ni-Cu
Page 31 and 32: xxx 87. Partizanskoe Pb-Zn skarn de
Page 33 and 34: Metallogenesis and Tectonics of the
Page 35 and 36: format (Nokleberg and others, 1996)
Page 37 and 38: logenesis of the region (1) subduct
Page 39 and 40: Subterrane—A fault-bounded unit w
Page 41 and 42: dilemma consists of two conflicting
Page 43 and 44: 2 to 20 m thick. A related dolomite
Page 45 and 46: Lantarsky-Dzhugdzhur Metallogenic B
Page 47 and 48: Origin of and Tectonic Controls for
Page 49 and 50: Metallogenic Belts Formed During Pr
Page 51 and 52: as at Oz, Monster, and Tart, may al
Page 53 and 54: Monashee Metallogenic Belt of Sedim
Page 55 and 56: Clark Range Metallogenic Belt of Se
Page 57 and 58: in addition to the Fe deposits. Min
Page 59 and 60: study) consists of lenses, from 100
Page 61 and 62: Omulev Austrian Alps W Deposit The
Page 63 and 64: ock, including coarse clastic rock,
Page 65 and 66: lative metalliferous brines in a re
Page 67 and 68: Prince of Wales Island Metallogenic
Page 69 and 70: suite of deposits and host rocks ar
Page 71 and 72: margin of the North American Craton
Page 73 and 74: newly created terranes migrated int
Page 75 and 76: (Ryazantzeva and Shurko, 1992). The
Page 77 and 78: tonnes Au and an average grade of a
Page 79: mafic and felsic metavolcanic rocks
Page 85 and 86: mentary rocks of the Cambrian to De
Page 87 and 88: (Preto and Schiarizza, 1985; Schiar
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 99 and 100: Finlayson Lake Metallogenic Belt of
Page 101 and 102: and barite in siliceous black turbi
Page 103 and 104: Windermere Creek (Western Gypsum) C
Page 105 and 106: (NX, DL, MY), Viliga (VL), and Zolo
Page 107 and 108: South of the main east-west-trendin
Page 109 and 110: ated subduction zone in the Wrangel
Page 111 and 112: icite-biotite-quartz bodies in frac
Page 113 and 114: Canada Cordillera. The granitoid ro
Page 115 and 116: Viliga (VL) passive continental-mar
Page 117 and 118: 32; tables 3, 4) occurs along the n
Page 119 and 120: superterrane, consists mainly of ma
Page 121 and 122: ers, 1994c, 1997c). In southern Bri
Page 123 and 124: mental volcanic rocks of intermedia
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
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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
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
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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
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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 and 244:
Democrat (Mitchell Lode) Granitoid-
Page 245 and 246:
with high-temperature and high-pres
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
Page 299 and 300:
sists of a mineralized fracture zon
Page 301 and 302:
dolomite. Wall rock alteration incl
Page 303 and 304:
elt of late Tertiary plutons that a
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 and 312:
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
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
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:
Page 387 and 388:
Page 389 and 390:
Page 391 and 392:
Page 393 and 394:
Page 395 and 396:
Page 397 and 398:
Page 399 and 400:
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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