Northeast Asia Geology: Terranes, Metallogenic Belts, Formations, Exercises of Geology

Download Northeast Asia Geology: Terranes, Metallogenic Belts, Formations and more Exercises Geology in PDF only on Docsity! Chapter 5 Introduction This article presents an overview of the regional geol- ogy, tectonics, and metallogenesis of Northeast Asia for the Neoproterozoic through Silurian. The major purposes are to provide a detailed summary of these features for readers who are unfamiliar with Northeast Asia. Several parts of this book on Northeast Asia provide background information. An overview of the regional geology, metallogenesis, tectonics, of the region, and other materials, such as employed geologic time scale and standard geologic definitions, are provided in chapter 1. The methodology for the metallogenic and tectonic analysis of this region is provided in Chapter 2. Descriptions of mineral deposit models are provided in Chapter 3. Addi- tional information on project publications, descriptions of major geologic units, and summaries of metallogenic belts are provided in appendixes A-C. Compilations Employed for Synthesis, Project Area, and Previous Study The compilation of regional geology and metallogen- esis in this introduction is based on publications of the major international collaborative studies of the metallogenesis and tectonics of Northeast Asia that were led by the U.S. Geologi- cal Survey (USGS). These studies have produced two broad types of publications. One type is a series of regional geologic, Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia By Nikolai A. Berzin1, Elimir G. Distanov1, Onongyn Tomurtogoo2, Andrei V. Prokopiev3, Vladimir F. Timofeev3, and Warren J. Nokleberg4 1 Russian Academy of Sciences, Novosibirsk. 2 Mongolian Academy of Sciences, Ulaanbaatar. 3 Russian Academy of Sciences, Yakutsk. 4 U.S. Geological Survey, Menlo Park, Calif. mineral-deposit, and metallogenic-belt maps and companion descriptions for the regions. Examples of major publications of this type are Obolenskiy and others (2003, 2004), Parfenov and others (2003, 2004a,b), Nokleberg and others (2004, 2005), Rodionov and others (2004), and Naumova and others (2006). The other type is a suite of metallogenic and tectonic analyses of these same regions. Examples of major publica- tions of this type are Rodionov and others (2004), Nokleberg and others (2000, 2004), and Naumova and others (2006). Detailed descriptions of lode deposits are available in Ariun- bileg and others (2003). For more detail than presented in this chapter, refer to the detailed descriptions of geologic units and metallogenic belts in the above publications. The Northeast Asia project area consists of eastern Russia (most of Siberia and most of the Russian Far East), Mongolia, Northern China, South Korea, Japan, and adjacent offshore areas (fig. 1). This area is approximately bounded by 30 to 82° N. latitude and 75 to 144° E. longitude. The major participat- ing agencies are the Russian Academy of Sciences; Academy of Sciences of the Sakha Republic (Yakutia); VNIIOkean- geologia and Ministry of Natural Resources of the Russian Federation; Mongolian Academy of Sciences; Mongolian University of Science and Technology; Mongolian National University; Jilin University; Changchun; China; the China Geological Survey; the Korea Institute of Geosciences and Mineral Resources; the Geological Survey of Japan/AIST; University of Texas Arlington; and the USGS. The Northeast Asia project extends and is built on data and interpretations from a previous project on the Major Mineral Deposits, Metallogenesis, and Tectonics of the Russian Far East, Alaska, and the Canadian Cordillera that was conducted by the U S G S, the Russian Academy of Sciences, the Alaska Division of Geological and Geophysical Surveys, and the Geological Sur- vey of Canada. A summary of the major products of this project is contained online at: http://pubs.usgs.gov/of/2006/1150/ PROJMAT/RFE-Ak-Can_Cord_Proj_Pamph.pdf and in appendix A. Metallogenesis and Tectonics of Northeast Asia Edited by Warren J. Nokleberg U.S. Geological Survey Professional Paper 1765 5-2 Metallogenesis and Tectonics of Northeast Asia Lake Baikal VLADIVOSTOK KHABAROVSK CHANGCHUN TOKYO SEOUL BEIJING IRKUTSK ULAANBAATAR YAKUTSK NOVOSIBIRSK 68 76 82 44 52 96 108 120 132 144 36 75 84 60 International boundaries for onshore area are approximate and do not indicate endorsement by participating countries. 0 500 1,000 km M O N G O L I A C H I N A R U S S I A NORTH-CENTRAL CHINA NORTHWEST CHINA NORTHEAST CHINA KOREAN PENINSULA J A P A N Pac ific O ce an Laptev SeaKara Sea Y a k u t i a S i b e r i a S o u t h e a s t e r n S i b e r i a a n d T r a n s b a i k a l i a R u s s i a n F a r E a s t Figure 1.  Regional summary geographic map for Northeast Asia showing major regions and countries. Major Geologic Units The major Neoproterozoic (Late Riphean through Vendian) through Silurian geologic and tectonic units of Northeast Asia are cratonal margin units, sedimentary basins formed on craton and cratonal margins and accreted terranes and superterranes (fig. 2, table 1). Short descriptions of map units are given in appendix B. Summary descriptions of the major units are provided in descriptions of metallogenic belts (below), and detailed descriptions of geologic units are provided by Nokleberg and others (2000, 2004), and Parfenov and others (2004b). Major Craton Margins and Craton-Margin Terranes The Archean through Proterozoic backstop or core units for the region of Northeast Asia are the North Asian craton and overlying Phanerozoic units, various cratonal margin units [Baikal-Patom, East Angara, South Taimyr, and Verkhoyansk terranes (fold- and thrust-belts)],and the Sino-Korean craton (fig. 2, appendix C). The Baikal-Patom cratonal margin (BP) consists of a fault-bounded basin containing Riphean carbonate and terrig- enous sedimentary rock, and younger Vendian and Cambrian 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-5 EXPLANATION Cratons and Cratonal Margins Cratons: NAC - North Asian (Archean and Proterozoic); SKC - Sino-Korean (Archean and Proterozoic) Cratonal Margin: BP - Baikal-Patom (Riphean through Cambrian and older basement; EA - East Angara (Riphean and older basement; ST - South Taimyr (Ordovician through Jurassic); VR - Verkhoyansk (Devonian through Jurassic). Tectonic Collages Between the North Asian and Sino-Korean Cratons Tectonic Collages Along the Northern and Eastern Margins of North Asian and Sino-Korean Cratons Active Subduction Zones CS - Circum-Siberia (Proterozoic) YT - Yenisey-Transbaikal (Vendian through Early Ordovician) AL - Altay (Vendian to Ordovician) WD - Wundurmiao (Riphean through Ordovician) AB - Atasbogd ( ; SM - South Mongolia-Khingan (Ordovician through Carboniferous); WS - West Siberian (Ordovician through Carboniferous) Ordovician through Permian) MO - Mongol-Okhotsk (Devonian through Late Jurassic); SL - Solon (Carboniferous and Permian) CH - Chukotka (Paleozoic and Triassic) BD - Badzhal (Triassic through Early Cretaceous); PA - Penzhina-Anadyr (Late Jurassic and Cretaceous); HS - Honshu-Sikhote-Alin (Jurassic and Early Cretaceous); SA - South Anyui (Permian through Jurassic); VK - Verkhoyansk-Kolyma Paleozoic through Early Jurassic) KOR - Koryak (Late Jurassic through Paleocene; SH - Sakhalin-Hokkaido (Cretaceous); WK - West Kamchatka (Mid-Cretaceous through Early Tertiary) ES - East Sakhalin (Late Cretaceous and Early Tertiary); OK - Olyutorka-Kamchatka (Late Cretaceous to Paleocene) Cratonal terranes (Archean and Proterozoic): GY - Gyeonggi-Yeongnam; JA - Jiaonan; OH - Okhotsk Late Proterozoic and Cambrian superterranes: AR - Argun-Idermeg; TM - Tuva-Mongolia Archean through Permian superterranes: BJ - Bureya-Jiamusi; KR - Kara Jurassic Superterrane: KOM - Kolyma-Omolon (Archean through Jurassic) Oceanic crust Surficial deposits Pelagic and Oceanic Rocks Cratonal Terranes and Superterranes Overlap Continental-Margin Arcs and Igneous Belts Plume-Related Igneous Province Active Arcs - Altay arc (Devonian and early Carboniferous, 381 to 290 Ma) East Sikhote-Alin arc (Late Cretaceous through early Tertiary, 96-65 Ma) - arc - Hangay arc ( arc arc - Lugyngol arc (Permian and Triassic, 295 to 250 Ma) - Norovlin arc (Devonian and Early Carboniferous, 410 to 255 Ma) - Okhotsk-Chukotka arc (Late Cretaceous and early Tertiary, 96 to 53 Ma) - arc - Selenga arc ( - South Mongolian arc (Carboniferous through Triassic, 320 to 203 Ma) - South Siberian arc (Devonian) - South Verkhoyansk granite belt (Late Jurassic through mid-Cretaceous, 157 to 93 Ma) - Transverse granite belt (Early Cretaceous, 134 to 124 Ma) - arc - Uda-Murgal and Stanovoy arc ( arc (Late Jurassic and Early Cretaceous, 154 to 120 Ma) - Tungus Plateau igneous province - (Late Permian and Early Triassic, 245 Ma) - Izu-Bonin (late Cenozoic, 20 to 0 Ma) - Japan (late Cenozoic, 23 to 0 Ma) - Kuril-Kamchatka (late Cenozoic, 11 to 0 Ma) at ea - gh ha lg nr oc ol se sm ss sv tr uo us ib ja kk Gobi-Khankaisk-Daxing'anling (Permian, 295 to 250 Ma) Late Carboniferous and Early Permian, 320 to 272 Ma) - Jihei (Permian, 295 to 250 Ma) - Khingan (Early and mid-Cretaceous) Main granite belt (Late Jurassic, 144 to 134 Ma) - Northern granite belt (Early Cretaceous, 138 to 120 Ma) North Margin (Late Carboniferous and Permian, 320 to 272 Ma) Oloy (Late Jurassic, 154 to135 Ma) Permian through Jurassic, 295 to135 Ma) Umlekan-Ogodzhin (Cretaceous, 135 to 65 Ma) Jurassic and Early Cretaceous, 203 to 96 Ma) - Uyandina-Yasachnaya ji ko ma - nb nm - uy Transpressional Arcs - Kema (Mid-Cretaceous) - Mongol-Transbaikal ( - South Siberian - ke mt ss tb Late Triassic through Early Cretaceous, 230 to 96 Ma) (Early Devonian, 415 to 400 Ma) Transbaikalian-Daxinganling (Middle Jurassic through Early Cretaceous,175 to 96 Ma) EP - East Kamchatka Peninsular (Mainly Paleocene) JT- Japan Trench (including Kuril-Kamchatka trench) (Miocene through Holocene; NN - Nankai (Miocene through Holocene) Devonian aulacogen Riphean aulacogen Modern rift system (Gakkel Ridge) Metallogenic belt Thrust Strike-slip fault Fault Contact Symbols, Faults, and Contacts Overlap-continental-margin arc Transform-continental-margin arc Active subduction zone OS tp Figure 2.—Continued. 5-6 M etallogenesis and Tectonics of N ortheast Asia Name of unit. Map Symbol Type of Unit (Craton, Terrane, Overlap Asseblage) Age range Tectonic Environment Tectonic Linkage NORTH ASIAN AND SINO-KOREAN CRATONS AND OVERLYING PROTEROZOIC AND PHANEROZOIC UNITS North Asian. NAC Sino Korean. SKC Craton Archean through Me- sozoic Cratonal and passive continental margin NORTH ASIAN CRATON MARGIN UNITS Baikal-Patom. BP East Angara. EA South Taimyr. ST Verkhoyansk. VR Overlap assemblages Neoproterozoic through Mesozoic Passive continental mar- gin with pericratonal subsidences Original overlap assemblages on North Asian Craton that were subsequently transformed into fold- and thrust-belts and terranes. SUPERTERRANES Argun-Idermeg. AR Bureya-Jiamusi. BJ Superterrane Superterrane Paleoproterozoic through late Paleo- zoic Proterozoic through Permian Passive continental- margin Composite May be either exotic with respect to the North Asian Craton or may be a rifted fragment of the craton. Accreted in Ordovi- cian through Silurian. Consists of early Paleozoic metamorphic , continental-margin arc, subduction-zone, passive continental-margin and island-arc terranes. Interpreted as a fragment of Gondwana. Accreted to the Sino-Korean Craton in the Late Permian and accreted to the North Asian Craton in the Late Jurassic. Kara. KR Superterrane Proterozoic through Ordovician Passive continental- margin Consists of Late Neoproterozoic through Ordovician Kara continental-margin turbidite terrane. Interpreted as a rift fragment of the North Asian Craton that was reaccreted in the Jurassic. Kolyma-Omolon. KOM Superterrane Archean through Juras- sic Composite Consists of of cratonal, passive continental-margin, island-arc, ophiolite terranes. The cratonal and passive continental core of the superterrane was rifted from the North Asian Craton and Margin in Late Devonian or Early Carboniferous. Reaccreted to the North Asian cratonal margin in the Late Jurassic. Tuva-Mongolia. TM Superterrane Late Riphean and older Composite Consists of Gargan and Baydrag cratonal terranes, Sangilen passive continental-margin terrane. Accreted in the Late Neoproterozoic. Table 1.  Summary of major Neoproterozoic through Silurian geologic units and characteristics for Northeast Asia (Russian Far East, Yakutia, Siberia, Transbaikalia,  Northeastern China, Mongolia, South Korea, and Japan). [Major units are listed from west to east, progressing from north to south. Units arranged in alphabetical order of map symbol in each major section on figure 2] 5. N eoproterozoic through Silurian M etallogenesis and Tectonics of N ortheast Asia 5-7 Name of unit. Map Symbol Type of Unit (Craton, Terrane, Overlap Asseblage) Age range Tectonic Environment Tectonic Linkage TECTONIC COLLAGES Altai. AL Collage Vendian through Ordovician Mainly Island arc and subduction zone Consists of the Vendian through Early Ordovician Salair island-arc and various fragments of arc-related turbidite terranes, subduction-zone terranes, metamorphic terranes derived from arc-related units, thick Cambrian and Ordovi- cian overlap turbidite units that formed on a continental slope and rise, and fragments of originally adjacent oceanic terranes. Collage interpreted as an island-arc system that was active near the southwest margin (present-day coordi- nates) of the North Asian Craton and Margin and previ- ously accreted terranes. Accreted in Late Silurian. Atasbogd. AB Collage Ordovician through Permian Composite Consists of: the Ordovician through Permian Waizunger- Baaran terrane, Devonian through Carboniferous Beitian- shan-Atasbogd terrane, and (3) Paleoproterozoic through Permian Tsagaan Uul-Guoershan continental-margin arc terrane. Collage is interpreted as a southwest continuation (present-day coordinates) of the South Mongolia-Khingan island arc that formed southwest and west (present-day coordinates) of the North Asian Craton and Margin and previously accreted terrane. Accreted in Late Carboniferous or Early Permian. Circum-Siberia. CS Collage Neoproterozoic Composite Consists of Baikal-Muya island arc, the Near Yenisey Ridge island arc, and the Zavhan continental-margin arc, all of Neoproterozoic age, and small fragments of cratonal and metamorphic terranes of Archean and Proterozoic age. The three separate Neoproterozoic island-arc systems formed south (present-day coordinates) of the North Asian Craton and Margin. Accreted in Neoproterozoic South Mongolia-Kh- ingan. SM Collage Ordovician through Carboniferous Island arc and sub- duction zone Consists of the South Mongolia-Khingan arc and tectonically linked subduction-zone terranes. The collage is interpreted as a major island-arc system that formed southwest and west (present-day coordinates) of the North Asian Craton and Margin and previously accreted terranes. Collage was separated from the North Asian Craton by a large back-arc basin. accreted in Late Carboniferous or Early Permian. Table 1.  Summary of major Neoproterozoic through Silurian geologic units and characteristics for Northeast Asia (Russian Far East, Yakutia, Siberia, Transbaikalia,  Northeastern China, Mongolia, South Korea, and Japan).—Continued [Major units are listed from west to east, progressing from north to south. Units arranged in alphabetical order of map symbol in each major section on figure 2] 5-10 Metallogenesis and Tectonics of Northeast Asia North Asian craton or the Yenisey-Transbaikal and Circum- Siberia collages. These favorable geologic environments consisted of regional metamorphism and hydrothermal alter- ation that were associated with accretion of terranes to the North Asian cratonal margin. The Bokson-Kitoiskiy metal- logenic belt also contains serpentine-hosted asbestos deposits that are interpreted as having formed in the same tectonic environment. The Prisayanskiy belt is hosted in terranes derived from the North Asian craton and contains REE car- bonatite, and mafic-ultramafic related Ti-Fe deposits that are interpreted as having formed in Neoproterozoic magmatic events. The Jixi metallogenic belt contains minor Homestake Au deposits for which the tectonic origin is unclear. Major Neoproterozoic (1,000 to 540 Ma) Metallogenic Belts and Host Units The major Neoproterozoic metallogenic belts are the Angara-Pit, Baikalo-Muiskiy, Bodaibinskiy, Bokson-Kitoiskiy, Central-Yenisei, Hovsgol, Jixi, Kyllakh, Lake, Pribaikalskiy, Prisayanskiy, and Vorogovsko-Angarsk belts (fig. 3, appendix C). Angara-Pit Metallogenic Belt of Sedimentary Hematite and Volcanogenic-Sedimentary Fe Deposits (Belt AP) (Yenisei Ridge, North-Asian Craton Margin, Russia) This Upper Riphean metallogenic belt is hosted in the North Asian cratonal margin (East Angara fold- and thrust- belt) and occurs in the southeastern part of the Yenisei Ridge. The belt forms a band along the east wing of the Central anticlinorium from the Angara River to the north to the Gorbilok River to the south, and is up to 100 km long. The belt contains three large chlorite-hematite deposits at Nizhne-Angarskoye, Ishimbinskoye, and Udorongovskoye, and numerous smaller occurrences. The deposits occur in clastic sedimentary rock of the late Riphean Nizhneangarsk. Each deposit consists of several (about 7 to 36) ore layers that vary from 2 to 16 m thick (ranging up to 30 m), have a total thickness of as much as 50 m, and are 0.3 to 14 km long. All deposits exhibit similar geological structure, min- eral composition, and quality of ore minerals. Ore layers and lenses are hosted in clastic and clastic-chemogenous sedi- mentary rocks, mainly hematite gritstone and conglomerate, hematite sandstone, and sandy hematite-chlorite siltstone. Host rocks and deposits are metamorphosed to phyllite (Matrosov and Shaposhnikov, 1988). The major deposit is at Nizhne-Angarskoye. The main references on the geology and metallogenesis of the belt are Yudin (1968), Brovkov and others (1985), and Matrosov and Shaposhnikov (1988). Nizhne-Angarskoye Sedimentary Hematite Fe  Deposit This deposit (Yudin, 1968; Brovkov and others, 1985) consists of layered hematite hosted in late Riphean argil- lite, siltsone, and sandstone. The Fe horizon is 45 to 180 m thick and occurs in 36 separate deposits that range up to 29 m thick, extend up to 15 km along strike, and range to 650 m depth. Fe layers are intercalated with sedimentary rocks that range from to 2 to 15 m thick. Ore layers consist of hema- tite, sandy-hematite, argillaceous chlorite hematite gritstone, hematite-siderite. Main ore minerals are hydrogoethite, hema- tite, and goethite with lesser siderite, magnetite, and pyrite. Gangue minerals are quartz, leptochlorite, clays, and sericite. The deposit contains 0.03 percent S and 0.08 percent P. The deposit is large with reserves of 1,200 million tonnes grading 40.4 percent Fe. Origin and Tectonic Controls for Angara-Pit  Metallogenic Belt The belt is interpreted as having formed during a preoro- genic stage of the Yenisei pericratonal subsidence in a back- arc (interland) sedimentary basin. Lithological-facial control of distribution of sedimentary hematite ores occurred. The paleodelta setting of formation of Fe ores is indicated by struc- tural, mineralogical, and geochemical features of host rocks (Yudin, 1968). A possible source of clastic ore minerals was residual Fe-rich weathering crust (Brovkov and others, 1985). Baikalo-Muiskiy Metallogenic Belt of Volcanogenic-Hydrothermal-Sedimentary Massive Sulfide Pb-Zn (±Cu), Polymetallic (Pb, Zn, Ag) Carbonate-Hosted Metasomatite, and Serpentine-Hosted Asbestos Deposits (Belt BM) (Russia, Northern Transbaikalia) This Neoproterozoic metallogenic belt occurs in the Baikal-Muya island-arc terrane, the Muya metamorphic ter- rane, and part of the Olokit-Delunur craton-margin rift terrane. The major deposits are at Kholodninskoye, Lugovoye, and Molodezhnoye. The belt occurs along the northern periphery of the Vitim highland (northeastern coast of Lake Baikal) and extends from Lake Baikal to Vitim River. The belt is 500 km long and 120 km wide. The lower part of the Baikal-Muya island-arc terrane consist of tectonic slabs of ophiolite of various ages with hemipelagic sedimentary rock (Lower Kelyansky suite); and a middle Riphean island-arc complex basalt, andesite, and plagiorhyolite (Verkhne Kelyansky suite), and gabbro and pla- giogranite intrusions. The island-arc rocks are metamorphosed to greenschist facies (Bulgatov and Gordienko, 1999; Bozhko and others, 1999). 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-11 Figure 3.  Generalized map of major Neoproterozoic metallogenic belts and major geologic units for Northeast Asia. Refer to text  and appendix C for summary descriptions of belts. Refer to figure 2 and table 1 for explanation of geologic units. Metallogenic  belt outlines adapted from Obolenskiy and others (2003, 2004) and Parfenov and others (2003, 2004). Metallogenic belts for area  east of 144º E (eastern boundary of Northeast Asia project area) are described and interpreted by Nokleberg and others (2003). The Muya terrane consists of the metamorphic Kindikan- sky, Ileirsky, and Lunkutsky suites. The Olokit-Delunuran craton-margin rift terrane con- sists of Riphean volcaniclastic and sedimentary rocks of the Olokit series with abundant interbedded tholeiitic basalt and rhyolite, volcanogenic siliceous sedimentary rock and tuff, and late Riphean carbonaceous, clastic, carbonate sedimentary rock of the Dovyren series. All units are metamorphosed to amphibolite facies and folded. The top displays subhorizon- tally lying postaccretionary sedimentary rock of intermontane basins (basalt, rhyodacite and molasse of the Padrinsky series late Riphean). The suture complexes are collisional late Paleozoic gran- itoids of the Barguzin-Vitim belt. The belt contains a group of depos- its and large ore occurrences: Kholodninskoe GY GY GY NAC SKC HS HS BJ HS KR ST Bering Sea Pacific Ocean Laptev Sea CS VK VK KOM SA CH oc nb, ol uy, ma oc, us oc, us oc, us oc ol KOR VR OH PA WK OK OK PA WK OK EP WS CS tp EA BP AL AL AL YT YT YT YT YT AR AR TM SM SMAB AB SL SL SL JA WD BJ BJ BJ BJ BD HS HS ea ji sm sm at at ko nm gh lg nr se se ha, mt se ss ss ss tb tb ke us uo sv tr MO CS SH JT JT NN ES SH ja ja ib Sea of Okhotsk Lake Baikal East-Siberian Sea kk MO MO P A C I F I C P L A T E ES ES MO 156 168 188 2,000 km1,0000 BM BK AP CY VA KY PR PB LA HO JX 5-12 Metallogenesis and Tectonics of Northeast Asia (volcanogenic-hydrothermal-sedimentary massive Pb-Zn sulfide (±Cu) (fig. 4), Lugovoye-polymetallic (Pb-Zn-Cu, Ba, Ag, Au) carbonate-hosted metasomatic. These deposits occur along the northern margin of the Baikal-Muya island arc in sedimentary rocks of the Olokit-Delunuran accretionary-wedge terrane. There are deposits of Ni (Chaisky, Baikalsky), Mo and Fe (Tyisky, Abchadsky-ferruginous quartzite), Ti, Mn and REE. In the Baikal-Muya belt some basins (Distanov and others, 1982) contain local synclines filled with volcanogenic and siliceous- clastic rocks. As a result of metamorphism of amphibolite facies they turned to be garnet-quartz-plagioclase-micaceous schist, quartzite and marble. They host stratified pyrite-pyrrhotite- sphalerite-galena-chalcopyrite ores of banded texture (Kholod- ninsky deposit, occurrences Kholoysky and Kosmonavtov). The deposits are enclosed in horizons of rhythmically alternat- ing carbonaceous aleuropelitic rock of diverse composition (Distanov and Kovalev, 1995). The deposits are multistaged, and associated younger shear zones exhibit streaky-stockwork aggregates of quartz, carbonate, sphalerite, pyrite, and galena. The central part of the basin hosts the band of foliated Ni- bearing intrusions of olivinite-peridotite-troctolite composition of the Dovyren complex (Chaisky, Ioko-Dovyren, Baikalsky, Nurundukan plutons). The ultramafic varieties of the complex contain streaky-stockwork deposits of pyrrhotite, pentlandite, chalcopyrite and magnetite (Chaisky deposit of mafic-ultra- mafic related Cu-Ni-PGE). Ores often show increased content of cobalt, chromium, and platinoids. The late Riphean and Cambrian overlap complex of the Upper Angara sedimentary basin hosts deposits of polymetal- lic (Pb-Zn-Ag) metasomatic-hosted model type (Lugovoye deposit) occurring in silicified horizons of limestone. The deposits consist of lensoid-shaped aggregates of sphalerite, galena, pyrite, and fluorite. Bedded bodies of metasomatically altered dunite and har- zburgite include commercial chrysotile-asbestos deposits with top quality commodity (Molodezhnoye, Ust-Kelyansky) that belongs to serpentine-hosted asbestos model type. The neph- rite deposits (Paramskoye, Buronskoye) occur in the margins of ultramafic bodies and zones of apocarbonate metasomatism. Enclosing rocks have small occurrences of graphite (Muys- koye). The volcanic complexes of paleoophiolite composition encompass minor Au-sulfide-pyrite deposits confined to large zones of mylonitization of interblock origination (Kamennoye, Samokutskoye, Ust-Karalonskoye). Bedded lensoid sulfide ores contain pyrite, pyrrhotite, chalcopyrite, galena, sphalerite, and sulfosalts of Ag with Pt and Pd. The main references on the geology and metallogenesis of the belt are Distanov and others (1982), Bulgatov (1983), Distanov and Kovalev (1995), Bozhko and others (1999), and Bulgatov and Gordienko (1999). Origin and Tectonic Controls for Baikalo-Muyskiy  Metallogenic Belt Various deposits in the belt are interpreted as having formed in Baikal-Muya island arc or during Riphean accretion of terrane with Muya metamorphic terrane and Olokit- Delunuran craton-margin rift terrane. Bodaibinskiy Metallogenic Belt of Au in Black Shale Deposits (Belt Bod) (Russia, Northern Transbaikalia) This Neoproterozoic through Early Carboniferous metallogenic belt occurs in the Patom fold- and thrust-belt in the North Asian cratonal margin. The major deposits are at Sukhoy Log, Vysochaishi, and Dogaldynskoye. The belt extends for 150 km east-west and 160 km north-south. The belt occurs in the Mesoproterozoic through early Paleozoic overlap complex of the Patom sedimentary basin that formed in a deep-water shelf along the southeastern passive continen- tal margin of the North Asian craton. The basin is filled with thick (8 to 10 km) carbonate and clastic sedimentary rock of the Teptorginsky, Balaganakh, Dalnetaiginsky and Bodaibo series (Ivanov and others, 1995). The black shale sequences comprise an important part of the basin. The rocks are metamorphosed to kyanite-sillimanite grade and collisional granitoids of the late Riphean Yazovsky complex are coeval with metamorphism. The deposit-controlling structure is the Bodaibo synclinorium that contains the Bodaibo and Kropot- kino basins (Sher, 1961). Narrow axial parts of anticlines with shear zones, intense foliation and hydrothermal-metasomatic deposits control some districts, as at Alexander-Dogaldynsky, Sukhoy Log, Verninsky, and Kamensky. Loci of warping of major fold folds and crosscutting, diagonal ruptures are favor- able for Au-quartz-vein and Au-sulfide-quartz veinlet deposits (Buryak, 1982), herein termed Au in black shale. Major depos- its occur at Sukhoy Log, Vysochaishy, Verninsky, and Nevsky. The largest district at Sukhoy Log extends more than 2.5 km and has deposits as much as 200 m thick. The main references on the geology and metallogenesis of the belt are Buryak (1982), Konovalov (1985), Neumark and others (1990), Rundquist and others (1992) and Ivanov and others (1995). Sukhoy Log Au in Black Shale Deposit This deposit (Konovalov, 1985) (fig. 5) consists of two types (1) quartz and sulfide veinlets and disseminations of (75 percent reserves); and (2) low-sulfide quartz veins (25 percent reserves). The first type consists of layered linear stockwork consisting of veinlets and disseminations with pyrite and quartz. Sulfides range from 2 to 5 percent, pyrite is abundant (95 percent). Rare minerals are galena, sphalerite, arsenopyrite, pyrrhotite, chalcopyrite, pentlandite, millerite, and cubanite. Au is very fine-grained (0.1-0.14 mm) and fine- ness is 780 to 820. Gold occurs in cracks in pyrite and rarely in arsenopyrite. The second type consists of 22 quartz veins with complicated morphology and occurs on the western edge of the deposit. This type consists of coarse-crystalline quartz (90 to 95 percent), pyrite (1 to 3 percent), carbonates (siderite, 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-15 metamorphic terrane, Hug accretionary wedge, and Tunka tonalite-trondhjemite-gneiss terranes, the Tannuola plutonic belt, and the Huvsgol-Bokson sedimentary overlap assem- blage. The belt occurs in the central part of East Sayan Mountains in the upper parts of Irkut, Urik, and Kitoy Rivers, extends along a nearly sublatitudinal trend for 315 km, and is 150 km wide. The metallogenic belt is a composite that includes several mineral deposit types. The Gargansky terrane consists of Archean plagio- granite-gneiss overlapped by a Riphean carbonates. The Ilchir terrane consists of a Riphean ophiolite, the Dibinsky suite of rhythmically bedded sedimentary volcanic rock, the Sarkhoy suite of calc-alkaline and tholeiitic volcanic rock, and the middle Riphean Khugeinsky suite of clastic and volcanic rock metamorphosed at high-pressure. The Huvsgol-Bokson over- lap assemblage consists of carbonate and clastic sedimentary rocks of the Vendian and Cambrian Bokson series. Igneous suture complexes are the subduction-related tonalite Sumsunur complex with U-Pb and Rb-Sr ages of 790 Ma, and Devonian and Carboniferous granitoids of the Khol- binsky, Ognitsky, and Botogol complexes. The major deposits are the Boksonskoye sedimentary bauxite, Botogolskoye magmatic nepheline, Ilchirskoye serpentinite-hosted asbestos, Bourun-Kholba Au in shear-zone and quartz-vein, Zun-Kholba Au in shear-zone and quartz-vein, and the Pionerskoye Au in shear-zone and quartz-vein deposits. The main references on the geology and metallogenesis of the belt are Krutsko (1962, 1964), Levitsky and others (1984), Dobretsov and Ignatovich (1989), Feofilaktov (1992), and Mironov and others (1995). Zun-Kholba Au in Shear-Zone and Quartz-Vein  Deposit This deposit (Dobretsov and Ignatovich, 1989, Feofilaktov, 1992; Zhmodik and others, 1994) (fig. 6) consists of a steeply dipping zone (8000 by 200 to 600 m) that strikes northwest and contains more than 30 bodies of which 12 are economic. The bodies are divided into (1) steeply dipping quartz-polysulfide; (2) banded chalcopyrite-pyrite bodies; and (3) quartz veins. The first type, which is economically important and is hosted in talc- chlorite and carbonaceous-siliceous shales, consists of a com- bination of veins and disseminations with 20 to 50 percent sul- fides. Major ore minerals are pyrite (as much as 30-45 percent), pyrrhotite (as much as 5 to 30 percent), chalcopyrite (as much as 10 percent), galena (as much as 5 to 8 percent), sphalerite (up to 5 percent), rare bornite, chalcocite, bismuthine, native silver, and Au and Ag tellurides. Gangue minerals are quartz, calcite, and talc, and rare albite, chlorite, muscovite, sericite, and graph- ite. The wall rocks contain zones of beresite, talc, graphitie, and listvinite alterations. Sulfide-body dimensions are 150 to300 by 0.2 by 0.4 m and occur in limestone. Sulfide grade ranges up to 50-80 percent and sulfides are mainly pyrite, sphalerite, galena, chalcopyrite, and pyrrhotite. Small quartz-sulfide veins contain 1-2 percent and rarely 5 percent sulfides, and has an average grade of 9.8 ppm Au and 13 ppm Ag. The deposit occurs in the central part of the Samarta-Kholba shear zone along the north- ern boundary of the Gargansky terrane. The deposit is medium size and has an average grade of 26 ppm Au, 24 to 37 ppm Ag, and 1.7 ppm Pt. Boksonskoye Sedimentary Bauxite Deposit This deposit (Il’ina, 1958; Orlova, 1958) consists of bauxite layers that occur over different dolomites (spotty, reef-generating, algae, banded, pink and red) in part of the thick Bokson suite in Archean and Proterozoic metamor- phic and mafic igneous rock. Thickness of the bauxite beds average 5 m, locally up to 30 m. Bauxite occurs in masses, layers, breccia, and locally in sandstone. The deposit contains 35 minerals and the primary minerals are bemite, kaolinite, dickite, leptochlorite, and gallauzite, and rare montmorillonite, pyrophyllite, Fe oxides, and hydroxide. Secondary minerals are sericite, muscovite, talc, serpentine, zeolite, hydrargillite, diaspore, chlorite, crysotile, quartz, calcite, and gypsum. The ore minerals are hematite, goethite, pyrite, and magnetite. Terrigenous minerals are tourmaline, olivine, feldspar, quartz, rutile, leucoxene, and alunite. Varieties of mineral assemblages are red-brown diaspore-hematite, gray-green diaspore chlo- rite, and intermediate diaspore-chlorite-hematite. The bauxite formed from coastal marine and lagoon sediments. The age of the deposit is 600 to 540 Ma. This is the oldest bauxite deposit in Russia. The deposit is large and has an average grade of 40 percent Al203. Botogolskoye Magmatic Nepheline Deposit This deposit (Solonenko, 1950) occurs in the Botogol alka- line nepheline syenite massif that forms an elongated oval that is 6 by 2 km and intrudes Proterozoic schist and carbonate rock. The massif formed in three stages (1) normal pyroxene and quartz syenite; (2) alkaline pyroxene and nepheline syenite; and (3) leucocratic nepheline syenite. Two deposit bodies occur, the 0.6 km2 Severny body and the 0.2 km2Yuzhny body. The bodies are separated by a kilometer-wide zone of a low-grade deposit. The Severny body is mainly leucocratic nepheline syenite with local biotite and pyroxene. The Yuzhny body is mainly pyrox- ene nepheline syenite. The deposit is interpreted as having formed in a back-arc rift. The deposit is medium size and has an average grade of 21 percent Al203. Ilchirskoye Serpentinite-Hosted Asbestos Deposit This deposit (Shamansky, 1945; Krutsko, 1964) occurs in the Ilchir lens-shaped massif (2.5 by 1 km) composed of Ven- dian peridotite and serpentinite. The deposit is an irregular lens with dimensions of 1700 by 100-380 by 150-550 m. The deposit has a concentric structure: a central part of asbestos-bearing serpentinite with a core of unaltered harzburgite; outward, serpentinite devoid of asbestos; and serpentinite-talc-carbonate 5-16 Metallogenesis and Tectonics of Northeast Asia ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ X X + + __ __ __ __ __ __ __ __ ____ __ ____ __ __ - - - - - - - - -- - -- - - ~ ~ ~ X X X X X X X X X X + + + + + + + X X X X X X X X X X X X X X X X X X X X X X X X X - - - - - - - - - - - - - - - - - - 1,740 2,036 2,140 2,267 m~ ~ ~~ ~ ~ ~ ~ ~ ~ ~ _ _ _ _ _ _ __ _ _ a b Ilchir Suite - Green and black shale, tuffaceous shale, and tuffaceous sandstone (Neoproterozoic), with local limestone and serpentinite olistolith Irkutnaya (Mongoshinskaya) Suite - Marble and limestone with interlayered black shale and quartzite (Neoproterozoic) Gargansky Metamorphic Complex (Archean and Paleoproterozoic) Sumsunursky Complex - Plagiogranite and granodiorite (Paleoproterozoic) Diorite and granodiorite (Devonian and Carboniferous) Granitized volcanic and sedimentary rock (Archean) Cataclastic zones a,Mylonite b,Shear Ore body Major shear Contact Figure 6.  Schematic cross section of Zun-Kholba Au in shear-zone and quartz-vein deposit,  Bokson-Kitoiskiy metallogenic belt. Adapted from Mironov and others (1995).6. Schematic cross  section of Zun-Kholba Au in shear-zone and quartz-vein deposit, Bokson-Kitoiskiy metallogenic  belt. Adapted from Mironov and others (1995). 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-17 rock. High-grade asbestos occurs in two tectonic zones that cut the massif and vary from 100 to 400 m thick. Asbestos is a large network type with veinlets ranging from 20-30 mm thick (locally up to 70 mm), cutting in various directions, and occur- ring about 1 to 2 m apart. The ore minerals are chrysotile-asbes- tos, bastite, serpentine, ophite, magnetite, talc, chromite, brucite, antigorite, carbonates, pyroxene, and olivine. Asbestos is silky, durable, and is useful for technological purposes. The deposit is small and has an average grade of 2.5 percent asbestos fibre and 0.08 to 0.25 percent textile grade asbestos. Origin and Tectonic Controls for Bokson-Kitoiskiy  Metallogenic Belt This belt is hosted in metamorphic, oceanic, accretionary wedge, and tonalite-trondhjemite-gneiss terranes that under- went Cambrian through Silurian metamorphism, hydrothermal alteration, and plutonic intrusion. A younger suture complex is the subduction-related Sumsunur complex tonalite with a U-Pb and Rb-Sr isotopic age of 790 Ma. The deposits in the belt are interpreted as having formed in multiple events. Central Yenisei Metallogenic Belt of Au in Black Shale, Au in Shear-Zone and Quartz-Vein, and Clastic-Sediment-Hosted Sb-Au Deposits (Belt CY) (Yenisei Ridge, North-Asian Craton Margin, Russia) This Late Neoproterozoic metallogenic belt is hosted in the passive continental margin of the West Angara terrane and is related to regional metamorphism and granitoid magma- tism. The belt extends north-northwest along the axial zone of the Yenisei Ridge for 450 km and is 40 to 80 km wide in the central anticlinorium formed from Proterozoic rocks metamor- phosed to amphibolite and epidote-amphibolite facies (Paleo- proterozoic Teisk series), and to greenschist facies (Mesopro- terozoic Sukhopit series). The metallogenic belt is bounded by the Tatarsk fault zone to the west and by the Ishimbinsk fault zone to the east. The central anticlinorium is cut by a north- east-striking transform fault that controls the regional struc- ture, the occurrence of synorogenic and postorogenic granitoid intrusions, and the location of major districts. Au and Au-Sb deposits are predominant in the belt and occur mainly in three districts (from north to south) (1) Severo-Yenisei (Sovetskoye, Eldorado, Ajakhta, and others); (2) Verkhne-Enashiminsk (Olimpiada, Enashiminskoye); and (3) Partizansk (Udereis- koye, Razdolninskoye). Host rocks are mainly carbonate and clastic rock and black shale in the middle and lower parts of the middle Riphean Sukhopit series. Collisional batholithic granitoid S-type plutons of the Tataro-Ayakhtinsk complex (with an isotopic age of 850 Ma) are widespread (Kornev and others, 1996). The three main types of deposits are (1) Au-quartz-vein (Sovetskoye and others); (2) Au in black shale (Olimpiada and others); and (3) clastic-sediment-hosted Sb-Au (Udereiskoye, Razdolninskoye). Most deposits are polygenetic and formed during the middle to late Riphean and Vendian. The main references on the geology and metallogen- esis of the belt are Distanov and others (1975), Li and others (1984), Brovkov and others (1985), Kornev and others (1996), and Obolenskiy and others (1999). Sovetskoye Au in Shear-Zone and Quartz-Vein  Deposit This deposit (Petrovskaya, 1967; Petrov, 1974; Smirnov, 1978; Serdyuk, 1997; Simkin, 1997) consists of quartz-Au veins cutting Neoproterozoic phyllite that is intruded by small gabbro and diabase bodies, and Paleozoic syenite porphyry. The deposit occurs in a thick, conformable shear zone that is complicated by small-scale folds. The district containing the deposit extends up to 8 km along strike, ranges up to 650 m wide, and extends to 390 m depth. The deposit consists of subparallel, branching veins, veinlets, and lenses. Separate veinlets and veins vary from less than a cm to 10 to 20 cm thick. Veins contain mainly coarse-grained quartz and fragments of low-grade altered host rock. Gangue minerals are carbonate, sericite, albite, and chlorite. Ore minerals constitute about 5 percent and are pyrite, arsenopy- rite, lesser chalcopyrite, galena, sphalerite, pyrrhotite, and marcasite. Gold is fine-grained. Fineness of Au averages 940. The deposits consist mainly of quartz, quartz-pyrite, quartz-arsenopyrite, and quartz-sulfide types. Quartz-sulfide type contains the most Au. Contact zones of deposits are more productive. Two types of hydrothermal wall-rock alterations are (1) combination of tourmaline, albite, seric- ite, and chlorite alteration; and (2) silica, sericite, chlorite, and sulfide alteration. Magmatic intrusive rocks occur 2 to 5 km to the northeast and consist of diabase and gabbro, and dikes of mica lamprophyre, syenite porphyry, and a slightly eroded granitoid pluton. A major magmatic chamber beneath the deposit is interpreted as the source of deposit-forming solutions (Brovkov and others, 1985). The deposit is medium size and has an average grade of 2.2 g/t Au. Olympiada Au in Black Shale Deposit This deposit (Li and others, 1990) (fig. 7) occurs in the central part of the Central-Yenisei metallogenic belt in the Verkhne-Enashiminsk district and consists of layered and saddle-shaped bodies of disseminated Au-sulfide in metaso- matite hosted in regionally metamorphosed Neoproterozoic carboniferous and clastic rock. The deposit occurs in a roof pendant above the large Neoproterozoic Chirimbinsk granitoid pluton. Host rocks are quartz-carbonate and micaceous schist with intercalated dolomite and carboniferous and quartz-mus- covite schist. Host rocks are hydrothermally altered to quartz- carbonate and mica, mica-carbonate and zoisite-quartz-mica metasomatite. Skarn locally occurs with metasomatite. The ore minerals are pyrrhotite, arsenopyrite, stibnite, berthierite, 5-20 Metallogenesis and Tectonics of Northeast Asia Figure 8.  Generalized geologic map and cross section of Damiao mafic-ultramafic  related Ti-Fe (V) deposit, Damiao metallogenic belt. Adapted from Dong (1993). northwest-trending major faults along the northern margin of the Sino-Korean craton. The mafic and ultramafic intrusions have isotopic ages of 992 to 604 Ma. The plutons and deposits are interpreted as having formed during interplate magmatism related to a Neoproterozoic active continental margin along the north margin of the Sino-Korean craton. Hovsgol Metallogenic Belt of Sedimentary Phosphate, Sedimentary Mn, and Sedimentary Fe-V Deposits (Belt HO) (Northern Mongolia) This Vendian through Early Cambrian metallogenic belt occurs in the Huvsgol-Bokson sedimentary overlap assem- blage. Sedimentary phosphate deposits and occurrences are mostly in the Vendian through Early Cambrian lower siliceous dolomite member of the Doodnuur or Kheseen Formations. Sedimentary Fe, sedimentary Mn, and sedi- mentary Fe-V occurrences are mainly above of the pro- ductive phosphate deposition in the Kheseen Formation, and also in clastic horizons of the Early Cambrian Khordil Formation (Ilyn, 1973). The metallogenic belt was first defined as a zone and as the Chubsugul phosphate basin by Ilyn (1973). Dejidmaa and others (1996) defined the belt as a complex metallogenic belt with sedimentary phosphorite, sedimentary Mn, Fe, Fe-Mn, and Fe-V deposits. The basin comprises approximately 30,000 km2, trends generally north-south, is approximately 300 km long, and ranges from a few tens to 120 km wide (Ilyn, 1973). The major deposits are the Urandosh, Uhaagol, Janhai, Ongilog nuur, Manhan A B 700 800 900 m Map Cross section Granodiorite(Triassic) Norite(Neoproterozoic) Anorthosite( )Neoproteraloic Monzonite Ore bodies Fault 0 400 800 m N Brecciated belt Syenite porphyry B A 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-21 uul, and Burenhaan phosphorite deposits; the Ikh-Baga Tsagaangol and other Mn occurrences; and the Hatigiin gol, Tsahir uul, and other Fe-V occurrences. The main references on the geology and metallogenesis of the belt are Dejidmaa and others (1966), Ilyn (1973), and Tomurtogoo and others (1999). Hubsugul Sedimentary Phosphate Deposit This deposit (Muzalevskii, 1970; Il’in, 1973; Byamba, 1996) consists of up to five phosphorite beds that alternate with dolomite, limestone, chert, aleurolite, and argillite in a phosphorite-bearing zone. The phosphorite beds range from 5 to 50 m thick, generally occur with carbonate rock, and form mainly aphanite and granular types. The deposit occurs in the Hubsugul Basin on the western coast of Lake Hubsugul. The basin extends 25 km stretching from south to north. The deposit occurs on both edges of the Hesen syn- cline in the lower part of the Vendian and Middle Cambrian Hubsugul series that consists of terrigenous and carbonate rock deformed in the late Riphean. The phosphorite deposit overlies Vendian sedimentary rock and is overlain by Late Cambrian limestone with archaeocyathids. The deposit is large and has an average grade of 20 to 40 percent P2O5. The deposit has produced 632.9 million tonnes. Hitagiin gol Sedimentary Fe-V Deposit The deposit (S. Tseveennamjil and others, written commun., 1983) occurs in Early Cambrian carbonate and terrigenous units in the Horidol Formation of the Hovsgol Group. Three horizons with V minerals occur, two hosted in siliceous carbonaceous slate, and one in chert. The host rocks are intercalated carbonaceous slate, siltstone, chert , and limestone, and quartzite. The deposit ranges from 600 to 2,700 m long and from 20 to 110 m thick. The resources are 11,039 million tonnes V2O5. Grades range from 0.05 to 0.235 percent V, up to 0.05 percent Mo, 0.002-0.034 percent Cu, and up 1.0 percent Pb, and 0.2 to 1.0 percent Ba. Saihangol Sedimentary Mn Deposit The deposit (C.A. Kiselov and others, written com- mun., 1959) consists of pyrolusite and minor hematite in siliceous layers in carbonate of the Early Cambrian Khori- dol Formation. Main ore mineral is pyrolusite with minor hematite. The host rock containing the pyrolusite siliceous beds ranges from 10-20 m thick. The pyrolusite beds are 300 m long and 1.5 to 2.0 m thick. The beds dip steeply to north. The deposit is large and has an average grade of 4.0 to 36.72 percent MnO, 3.2 to 21.88 percent Fe2O3. Resources are 293 million tonnes ore containing 65 million tonnes Mn, and 43 million tonnes Fe. Origin and Tectonic Controls for Hovsgol  Metallogenic Belt The belt is interpreted as having formed during shallow- water, carbonate-dominated sedimentation in the Minusa-Tuva back-arc basin. Igarsk Metallogenic Belt of Sediment-Hosted Cu Deposits (Belt IG) (Western margin of North Asian Craton, Russia) This Vendian through Early Cambrian metallogenic belt occurs in the northwestern North Asian cratonal margin and consists of lenses of red-bed sedimentary rocks that occur in a Vendian submontane basin in the Riphean Igarsk uplift (Dyuzhikov and others, 1988). The belt occurs in a sublongitudinal, narrow band up to 100 km long. The host late Riphean and Early Cambrian sedimentary rocks occur in three structural levels (1) intensely deformed clastic and carbonate rock of the Ludovsk and Gubinsk series (early and middle Riphean); (2) clastic and carbonate deposits of the Chernorechensk series, and red-bed clastic rocks of the Izluchinsk Series (late Riphean); and (3) carbonate rock with rare sandstone and siltstone of the Vendian and Early Cambrian Sukharinsk Series. There are two persis- tent horizons of Cu deposits. The lower horizon occurs in a transitional zone between the Izluchinsk red-bed suite and the underlying grey sedimentary rock of the Chernorechensk suite. This horizon is about 5 m thick (rarely up to 15 m) and consists of fine-grained disseminated digenite, bornite, and chalcopyrite. The upper horizon occurs at the base of marine grey deposits of the Sukharinsk suite and overlying red-beds of the Izluchinsk suite. The horizon is 10 to 30 m thick. Cu-rich areas often occur in the upper ore horizon (Graviiskoye and Sukharinskoye deposits). Two types of deposits are distinguished, deposits directly connected with host strata and crosscutting high-grade deposits in fracture zones. The major deposit is at Graviiskoye. The main references on the geology and metallogenesis of the belt are Malich and Tuganova (1980), Malich and others (1987), Djuzhikov and others (1988), and Lurie (1988) Graviiskoye Sediment-Hosted Cu Deposit This deposit (Rzhevskiy and others, 1980; Gablina and others, 1986; Djuzhikov and others, 1988; Lurie, 1988) (fig. 9) is hosted in late Riphean red and grey sedimentary rock consisting of alternating argillite, clay limestone, and marl. Southern, Northern, Central, and Eastern deposits are recognized. The Southern and Northern deposits occur in basal layers of lagoon sedimentary rock. The Southern deposit is 3.3 km long, and the Northern deposit is 1 km, and both vary from a few meters to 60 m thick. Sulfide minerals occur in streaks. Main ore minerals are diagenite, bornite, 5-22 Metallogenesis and Tectonics of Northeast Asia chalcopyrite, and pyrite. Slight silica alteration of wall rocks occurs. The Central deposit occurs above a paleouplift between two reefs. The deposit is 900 m long and up to 70 m thick. Main ore minerals are djurleite and bornite that occur in lenses and streaks. Sparse chalcopyrite and galena occur at the deposit periphery. Wall-rock alteration consists mainly of intense silica alteration with widespread antraxolite. The Eastern deposit consists of numerous lenses and ore-bunches of Cu minerals in conglomerate and breccias in the reef shelf. Main ore miner- als are digenite and bornite with rare chalcopyrite, galena, and pyrite. Wall-rock alteration consists of carbonate minerals, and sparse antraxolite. The deposit is small. Origin and Tectonic Controls for Igarsk  Metallogenic Belt The belt forms the northern large segment of the Pribai- kal-Yeniseisk Cu belt in the Igarsk uplift (Malich and others, 1987). The Cu-bearing rocks coincide with the late Riphean Norilsk-Turukhansk aulacogen. Cu deposits are related to the zones of lateral pinching of red-bed molasse sedimentary rock that formed in the final stage of development of oro- gen basin (Malich and Tuganova, 1980). Cu minerals were deposited in a katagenesis environment during migration of ground water. Metals precipitated along the hydrosulfuric geochemical barriers. The deposits are interpreted as having formed along flexures, anticline uplifts, and fracture zones that were favorable to migration of Cu-bearing grond waters (Lurie, 1988). Jixi Metallogenic Belt of Banded Iron Formation (BIF, Algoma Fe), Homestake Au, Metamorphic Graphite, and Metamorphic Sillimanite Deposits (Belt JX) (Northeastern China) This Neoproterozoic through Cambrian metallogenic belt occurs in the eastern Heilongjiang Province and is hosted in the Jiamusi metamorphic terrane and the Paleozoic Zhang- guangcailing continental-margin arc superterrane. The belt trends north-south, is about 400 km long, and about 100 km wide. Most of the BIF, graphite, and sillimanite deposits are related to the Al-rich clastic rock and carbonate of the Mashan and Xingdong Groups that are regionally metamorphosed to granulite or amphibolite facies. Some deposits, such as the Dongfengshan BIF and Homestake Au-vein deposits, are related to volcaniclastic rock and carbonate in the Dong- fengshan Group that is regionally metamorphosed to lower greenschist or amphibolite facies. The Mashan Group was interpreted as Late Archean or Paleoproterozoic, but recent isotopic ages suggest a Neoproterozoic age. The main deposits are at Shuangyashan, Liumao, and Dongfengshan. The main reference on the geology and metallogenesis of the belt is Lu and others (1996). Shuangyashan Banded Iron Formation (BIF,  Algoma Fe) Iron Deposit This deposit (Deng, 1980; Cao, 1993b) consists of bed- ded and stratiform BIF deposits that occur concordant to the Figure 9.  Schematic cross section of Graviiskoye sediment-hosted Cu deposit, Igarsk metallogenic belt. Adapted from  Dyuzhikov and others (1988). 0 20 40 m Sandstones and aleurolite Aleuropelites, sandstone, and aleurolite Carbonate conglomerate and breccia Dolomite and limestone Shale Ore body Red-brown rock Fault Drillhole Ve nd ia n 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-25 Lake Metallogenic Belt of Volcanogenic Cu-Zn Massive Sulfide (Urals type, Volcanogenic- sedimentary Fe, Podiform Cr, Mafic-Ultramafic Related Ti-Fe, Cu (± Au, Ag, Fe) Skarn, Fe Skarn, Granitoid-related Au Vein, Cyprus Cu-Zn Massive Sulfide, and Mafic-Ultramafic Related Cu-Ni-PGE Deposits (Belt LA) (Western Mongolia) This Late Neoproterozoic (Vendian) to Late Cambrian metallogenic belt is hosted in the Lake island-arc terrane (Tomurtogoo and others, 1999). The metallogenic belt was defined by Dejidmaa and others (1996) as a complex metal- logenic belt with different type deposits and occurrences. The northern part of the belt trends north-south and the southern part trends southeast to east. The belt is approxi- mately 30 to 100 km in the southern part, varies from 200 to 250 km wide in northern part, and is approximately 1000 km long. A large part of the belt is covered by Cenozoic surficial deposits and large lakes. Cu sulfide deposits and volcanogenic-sedimentary Fe deposits and occurrences are related to the Vendian through Early Cambrian Khantaishir ophiolite complex in basalt, andesite, dacite, and rhyolite volcanic rock in the Early Cambrian Tsol uul, Icheet, Daa- gandel, Ulaanshand, and Khanhohii Formations. The mafic- ultramafic related podiform Cr and zoned mafic-ultramafic related Fe-Te occurrences occur in ultramafic rock in the Vendian through Early Cambrian Khataishir ophiolite com- plex, and in ultramafic intrusions in the Khanhohii area. Cu skarn, Fe skarn, and granitoid-related vein, stockwork, and replacement Au deposits are related to the Middle and Late Cambrian throughgtohiin shil igneous complex that consists of gabbro, tonalite, and granite. Gabbroic Ni-Cu occurrences are related to the Middle Cambrian Khyargas nuur igneous complex that consists of layered pyroxenite, gabbro, norite, and troctolite (Izokh and others, 1990). The major deposits in the belt are (1) major dissemi- nated Cu sulfide deposits at Borts uul, Mendeeheindavaa, Narandavaa, and Suvraagiin; (2) Au massive sulfide deposits at Gozgor, Khurendosh uul and Suvraa; (3) volcanogenic- sedimentary type Fe occurrence at Bayanhudag; (3) mafic- ultramafic related podiform Cr occurrences at Nogoontolgoi and Bideriingol; (4) mafic-ultramafic related Fe-Ti occur- rences at Turgengol and Dumberel uul; (5) Cu skarn occur- rences at Togloin khudag, Alag uul, and Jargalant nuruu; (6) Fe skarn occurrence at Arvangurav; (7) granitoid-related stockwork and replacement type Au occurrence at Khyargas; and (8) alayered gabbroic type Ni-Cu(± PGE) occurrences at Bust khairhan and Altan khudag. The main references on the geology and metallogenesis of the belt are Izokh and others (1990), Dejidmaa and others (1996), and Tomurtogoo and others (1999). Bideriingol Podiform Chromite Deposit This deposit (A. Rauzer and others, written commun., 1987) consists of lenses of massive chromite and pockets of disseminated chromite in ultramafics of the Khantaishir ophiolite Complex of Vendian through Early Cambrian age. Lenses are 0.2 m by 3.0 m. Disseminated chromite mineraliza- tion forms pockets 5.0 m by 3.0 m in melanged serpentenite. Chromite constitutes from 20-30 percent to 50 to 70 percent the pockets. Grab samples from weakly disseminated ore con- tained 0.3-0.5 percent Cr, 0.2 to 0.5 percent Ni, 0.02 percent Co, and 0.01 percent. Cu Borts Uul Volcanogenic Cu-Zn Massive Sulfide  (Urals type) Deposit This deposit (D. Baatar and others, written commun., 1979) consists of sulfide rich lenses and tabular bodies in volcanic rock at the intersection of the Khangai and Zavkhan major faults. The deposit contains three parts. The Northern part hosts faulted horizons and lenses of andesite, dacite, basalt tuff and volcanic breccia. The three main bodies are tab- ular and conformable with host volcanic rocks. Sulfide bodies and host rocks are folded together. Sulfide bodies ranges from 1 to 17 m thick and extend up to 1.4 km long. Ore minerals occur in irregular masses, disseminations, stringers, and nests. A gradational contact occurs between host rock and sulfides. Grade varies widely up to 4.0 percent Cu and the average grade sulfide bodies is 0.5 to 0.6 percent Cu, up to 60.0 g/t Ag and up to 0.4 g/t Au. Ore minerals are chalcopyrite, chalcoc- ite, bornite, cuprite, covellite, and copper oxides. Host rock is altered and white. Chlorite and epidote alteration is widely developed. The Central part consists of sheets and lenses of andesite, basalt, dacite tuff, tuff, and tuff-breccia, strikes northwest, and extends for 0.5 km. Two main zones range from 2.0 to 15.0 m thick and contain sulfide lenses or tabu- lar bodies that range from 0.2 to 2.0 m thick and dip steeply. Other features are similar to the Northern part. Average grades are 1.3 percent Cu and 5.0 g/t Ag. The third or Pyrite part occurs 1.5 km east of the Central part and is hosted in dacite porphyry and tuff. Finely disseminated pyrite occurs in a zone 100 by 250 m. Pyrite is intensively oxidized and limonite is well developed. Cu minerals are rare. Grades are up to 0.1 percent Cu, up to 0.4 g/t Au, and up to 5.9 g/t Ag. The deposit is large and has an average grade of 0.6 to 1.3 percent Cu with a cutoff grade of 0.1 percent Cu. Resource in the Northern part is 28,200 tonnes Cu with average grade of 1.0 to 1.5 percent Cu to a depth of 100 m. Khyargas Granitoid-Related Au Vein Deposit This deposit (B.A. Samozvantsev and others, writ- ten commun.,1982) consists of a sublatitudinal-trending 5-26 Metallogenesis and Tectonics of Northeast Asia listwanite zone in serpentinite. The zone ranges from 50.0 m to 100.0 m wide, is up to 500.0 m long, and occurs in a melange zone. The ore minerals are pyrite and chalcopyrite, malachite, and Fe oxides. Abundant ore minerals occur in the northwest part in an area up to 16.0 m thick, and in the north- west part in an area up to 8.0 m thick. Channel samples grade up to 1.6 percent Cu, up to 3.0 g/t Au (in 1 sample 6.0 g/t), up to 20.0 g/t Ag, up to 0.3 percent Ni, and up to 0.6 percent As. To the southwest, the zone is surrounded by small out- crops of amphibole-garnet skarn with hematite and mala- chite. The skarn contains 0.01 to 0.09 percent Zn and Cu, 0.2 g/t Au and 1.0 g/t Ag. For the deposit, the average grade is 0.01 to 0.09 percent Zn+Cu, 0.2 g/t Au, and 1.0 g/t Ag. Naran Davaa Cyprus Cu-Zn Massive Sulfide  Deposit This deposit (A.A. Rauzer, and others, written commun., 1987) consists of a northwest-trending zone with chlorite, epi- dotie, quartz-sulfide stringers, and disseminated pyrite, chalco- pyrite, hematite. The zone occurs in an area 0.7 km wide and 2.5 km long in Vendian mafic-ultramafic bodies and Vendian through Lower Cambrian chlorite and chlorite-sericite schist that are overlain by Middle Devonian carbonate rock. The zone is as much as 10.0 m thick and up to a few hundred meters long. Rock chip and grab samples contain 0.01 percent to 1.0-2.0 percent Cu, 0.001 to 0.2 percent Ni, 0.001 to 0.01 percent Co, up to 0.2 percent Cr, up to 15.0 g/t Ag, 0.001 percent Mo, and up to 0.01 g/t Au. Abundant sulfides (chalcopyrite, malachite, and azurite) occur in areas of disseminated sulfides. The aver- age grade in abundant sulfide bodies ranges is as much as 10.0 percent Cu. Similar zones occur to the east and west. Tsagdaltyn Davaa Mafic-Ultramafic Related  Cu-Ni-PGE Deposit This deposit (B.N. Podkolzin and others, written commun., 1990) occurs in 3.5 km2 serpentinite massif. The ore minerals are magnetite, a black Ni mineral, chromite, and martite. Other minerals are ilmenite, limonite, chalcopyrite, pyrite, and pent- landite. The massif strikes northeast for 5.0 km, and ranges up to 0.7 km wide. Chrisotile-asbestos stringers range up to 0.5 cm thick. Grab samples contain 0.016 to 0.24 percent Ni (average of 0.175 percent); 0.003 to .023 percent Co (average of 0.008 to 0.013 percent), and up to 0.02 percent Cu. In the central part of the serpentinite massif pyroxenite us replaced by amphibole. Pyroxenite contains up to 0.4 percent, Cr, 0.02 to 0.06 percent Ni, 0.01 to 0.02 percent Co, and 0.02 to 0.1 percent Cu. One sample contains 0.003 g/t Au. Gold occurs in pan concentrates of stream sediment samples from small valleys in the massif. Origin and Tectonic Controls for Lake  Metallogenic Belt The magmatic deposits of belt are interpreted as having formed in the Late Neoproterozoic through Early Cambrian Dzhida-Lake island arc. The sediment-hosted deposits are interpreted as having formed during sea floor spreading volca- nism and related mafic-ultramafic magmatism. Pribaikalskiy Metallogenic Belt of Carbonate- Hosted Pb-Zn (Mississippi Valley Type) Deposits (Belt PrB) (Russia, Western Transbaikalia) This Riphean metallogenic belt occurs along the juncture of Paleoproterozoic Akitkan active continental margin, consisting of a volcanic-plutonic belt, with sedimentary rock of the Baikal- Patom fold- and thrust-belt that is the southern part of the North Asian craton. The belt extends along the northwestern coast of Lake Baikal for 170 km and ranges from 30 to 50 km wide. The tectonic setting of the belt is defined by tectonic and magmatic processes associated with the Akitkan volcanic-plutonic belt along the margin of North Asian craton. This Paleoproterozoic volcanic-plutonic belt consists of subalkaline, siliceous lava, minor basalt porphyry, and subaerial volcanic and sedimentary rock. Also occurring are comagmatic diorite, granodiorite, and granite, and rapakivi granitoids in the Primorsky Complex with an isotopic age of 1,690 ± 40 Ma. The overlap assemblage consists of clastic and carbonate sedimentary rock of the Baikal series (Goloustenskaya and Uluntuy suites) that extend along the margin of the craton for 1,000 km with monoclinal northwest dips. The sedimentary rocks consist of fine-grained limestone, unequigranular micro- and coarse-crystalline limestone with oolite-like internal structure, sedimentary and diagenetic dolo- mite, talc rock, and talc-carbonate rock. The monoclinal dip is complicated by longitudinal S folds and higher-order folds. The deposit controls are folds and regional shear zones that consist of lenses and sublaminated bodies of talc rock, and quartz and aragonite veins. The shear zones formed during overthrusting of the deposit-enclosing sequence over the older volcanic rock. The major deposit in the belt is at Barvinskoye. The main references on the geology and metallogenesis of the belt are Tychinsky and others (1984), and Tychinsky (1986). Barvinskoye Carbonate-hosted Pb-Zn  (Mississippi Valley type) Deposit This deposit consists mainly of sulfides in layers, lenses, veins, and disseminations (Tychinsky and others, 1984) that occur along concordant ruptures and shears that control the deposit. Also occurring are crossing verins. Sphalerite, galena, fluorite ore is the most productive. The host rocks exhibit widespread are metasomatic alteration. The deposit is inter- preted as having formed during hydrothermal activity. Origin and Tectonic Controls for Pribaikalskiy  Metallogenic Belt The belt is interpreted as having formed along shear zones and faults that occurred along an ancient active continental mar- gin on the southern margin of the North Asian craton. 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-27 Prisayanskiy Metallogenic Belt of REE (Ta, Nb, Fe) Carbonatite; Mafic-Ultramafic Related Ti-Fe (+V); Diamond-Bearing Kimberlite; and Talc (magnesite) Replacement Deposits (Belt PrS) (Russia, East Sayan) This Late Neoproterozoic metallogenic belt is related to the following units in the Onot granite-greenstone, Sharizhal- gay tonalite-trondhjemite gneiss, and Urik-Iya greenschist terranes (1) mafic-ultramafic plutons in the Ziminsky complex; (2) upper part of Onot terrane that consists of interbedded amphibolite, and magnesite and talc layers; and (3) ultramafic alkaline plutons; and (4) sparse micaceous kimberlite dikes. The age range of metallogenic belt is interpreted as Late Neoproterozoic. The belt occurs in southwest of Irkutsk Oblast in the East Sayan Mountains and trends northwest along the junction of the North Asian craton and Sayan Mountains. The belt is 400 km long and has an average width 50 to 60 km. The Sharyzhalgay terrane consists of Archean biotite- hornblende, biotite-hypesthene gneiss, schist, amphibolite, pyroxene plagiogneiss, sillimanite schist, ferruginous quartz- ite, coarse-grained marble, and granulite and charnockite. The lower part of the Onot terrane consists mainly of calc-alkaline, bimodal, volcanic rock, and the upper part consist of meta- morphosed sedimentary rock with interbedded amphibolite, magnesite rock, and talc rock. These units are intruded by gabbro of the Arbansky complex and rapakivi granitoids of the Paleoproterozoic Shumikhinsky complex. The Urik-Iya terrane consists of Paleoproterozoic schist, phyllite, metasand- stone, amphibolite, and spillite and keratophyre. The belt contains deposits and occurrences in large districts with REE, Ti, and talc replacement deposits and small diamond occurrences. The major deposits are at Belo-Zimin- skoye, Sredne-Ziminskoye; Zhidoyskoye; Ingashinskoye; and Onotskoye. The diversity of deposits suggests that this belt is fairly promising for discovery of new, large REE, Ti, magne- site, and talc-replacement deposits. The main references on the geology and metallogenesis of the belt are Frolov (1975), Levitsky (1994), Emelyanov and others (1998), and Mekhonoshin (1999). Beloziminskoye REE (Ta, Nb, Fe) Carbonatite  Deposit This deposit (Pozharitskaya and Samoilov, 1972; Frolov, 1975; Emelyanov and others, 1998) consists of a stockwork calcite carbonatite body that occurs in a core of an alkaline ultramafic pluton. The stockwork extends more than 10 km2, forms an northwest-trending ellipse, and extends to about 750 m depth. The stockwork is surrounded by a carbonatite vein zone that is about 100 m thick and extends up to 1 km long. Carbonatite contains relics of silicate rock in the peripheral part of the stockwork. The carbonatite consists of apatite, mag- netite, and phlogopite. The deposit formed in four stages and the second stage is the most economic. Outward to inward, the major mineral zones are pyroxene, forsterite, mica, and monomineral calcite. REE minerals include disanalite, bad- deleyite, zirkelite, hatchettolite, and pyrochlore. Baddeleite, dizanalite, and zirkelite occur only in peripheral parts adjacent to host rock. Hatchettolite is widespread in the external zone, and pyrochlore occurs in the internal zone. The deposit is large and has an average grade of 0.39 percent; Nb2O5 and 0.015 to 0.017 percent Ta2O5. Onotskoe Talc (Magnesite) Replacement Deposit This deposit (Korenbaum, 1967; Romanovich and others, 1982) (fig. 11) occurs in the western part of the Onotsky graben that contains early Proterozoic volcanic and carbonate rock. Most of the talc is in carbonate in the Kamchadal sequence. Two productive horizons occur (1) a lower horizon is 100 to 150 m thick and consists of dolomite and magnesite in lenses in lime- stones and various metamorphic rock, and (2) an upper horizon is 20 m thick and consists of magnesite. The deposit occurs in the lower horizon that is sheared and deformed into recum- bent steeply dipping folds. The deposit hosts seven large ore bodies of different morphology and composition. Of economic significance are veins and swells that form 32 ore bodies with thicknesses from a few to 50-80 m, lengths of 200 to 600 m, and depths of more than 260 m. Ore minerals are talc, magnesite, chlorite, graphite, dolomite, serpentine, hematite, sagenite, apa- tite, and quartz. The origin is interpreted as an apomagnesite talc deposit with massive structure (steatites). The structure is thin to scaly. The ore quality is high, and the color varies from white to light green to light gray. Chemical composition is 59.8 percent SiO2; 1.8 percent Al203, 0.3 percent Fe203, 1.4 percent FeO, 0.2 percent TiO2, 33.9 percent MgO, 0.4 percent CaO. The deposit is medium size. Ingashinskoye Diamond-Bearing Kimberlite  Deposit This deposit (Pechersky, 1965; Prokopchuk and Metel- kina, 1985; Sekerin and others, 1993) occurs in a dike field of nine small bodies (0.08-1.0 by 50-850 m) that intrude Paleoproterozoic schist. The dikes are composed mainly of olivine and phlogopite, and minor minerals are serpentine, talc, calcite, titanomagnetite, pyrope, and chrome-spinel, and rare ilmenite, apatite, diamond, chlorite, and volcanic glass, and local priderite, armalcolite, and alkaline amphibole. Most abundant are chrome spinel and orange almandine, and pyrope, and rare chrome diopside and magnetite. The dike thicknesses are extremely irregular, and the dike dip is subver- tical. Dikes are subdivided into three types (1) calcite-lacking with glassy bulk mass (olivine lamproites); (2) calcite with phlogopite (micaceous kimberlite); and (3) low-calcite with olivine (transitional). An isotopic age for the dikes is 1268 Ma. The small Yuzhnaya pipe at Belaya Zima is composed of kimberlite-like breccia. Diamonds are rhombododecahedral 5-30 Metallogenesis and Tectonics of Northeast Asia between Pb-Zn deposits and organic carbonate units exists. Five concordant layered deposits occur, and extend more than 500 m along strike and are as much as 600 m deep. The thickness of deposits ranges from 3.0 to 8.7 m, occasionally as much as 33 m. Boundaries of deposits are gradational, particularly for disseminated ores. Main ore minerals are galena, sphalerite, and pyrite, and rare pyrrhotite, chalco- pyrite, bournonite, and fahl. The main gangue minerals are quartz and Fe-carbonate. Galena and sphalerite with a Zn:Pb ratio of 2:5 are predominant. Chalcopyrite and fahl are typi- cal minerals in veins along with sphalerite, galena and pyrite. The deposit is interpreted as having formed under polygen- ous hydrothermal and sedimentary conditions. A model Pb isotopic age for the deposit is 849 to 740 Ma. The deposit is medium size and has an average grade of 2.5 percent Pb and 1.1 percent Zn. Enashiminskoye 2 Fe Skarn Deposit This deposit (Matrosov and Shaposhnikov, 1988) consists of layers and lenses of magnetite in metamorphosed middle Riphean volcanic, carbonate, and clastic rocks. Host rocks and Fe-ores are intruded by Chirimbinsk granitoid plu- ton. The contact zone is contact metamorphosed, carbonate- altered, and silicified and contains epidote-amphibole-garnet skarn. The district containing the deposit extends up to 4.7 km along strike and contains more than 20 deposits that vary from 5 to 70 m thick, are up to 700 m long, and are up to 650 m deep. The deposit minerals are magnetite, epidote, and amphibole. The deposit contains anomalous Ti, V, Cr, and Mn, and anomously low S and P. The deposit formation was polygenetic with initial formation of primary siliceous-car- bonate and ferruginous sedimentary rocks that were region- ally metamorphosed, contact-metasomatized. The deposit is large and has resources of 450 million tonnes grading 36 to 51 percent Fe. Origin and Tectonic Controls for Vorogovsko- Angarsk Metallogenic Belt The SEDEX deposits in the belt are interpreted as hav- ing formed along major fault depressions along transcrustal block in pericratonal subsidences. Carbonate-hosted Pb-Zn deposits formed in carbonate reefs. Volcanogenic-sedimentary Fe deposits are interpreted as having formed during marine volcanism and sedimentation. The metallogenic belt is inter- preted as having formed during convergence along a middle to late Riphean continental margin (Obolenskiy and others, 1999). The principal structural control for the Gorevskoye deposit was the intersection between a system of northwest block-bounding faults and the transversal Irkeneevsk plate boundary fault. Host rocks and the coeval deposits have model Pb isotopic age of about 950 Ma. Approximate coeval units are collision-related granite plutons (Tatar-Ayakhta complex) and dolerite dikes. 0 50 100 m Siderite Siliceous siderite Ore body Marl and argillaceous schist Marlstone and dolomite Cherty limestone and dolomite Siliceous dolomite marl Dolomite Fault N eo pr ot er oz oi c Contact Figre 12.  Schematic cross section of Gorevskoye sedimentary  exhalative Pb-Zn (SEDEX) deposit, Vorogovsko-Angarsk  metallogenic belt. Adapted from Kuznetsov and others (1999). 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-31 Summary of Cambrian through Silurian (540 to 410 Ma) Metallogenesis Metallogenic Belts with Granitoid-Hosted Deposits Related to Continental-Margin Arcs, Transpression, or Terrane Accretion Several metallogenic belts possess geologic units favor- able for major granitoid-hosted or related deposits, including the Bayanhongor belt (with Au in shear zone and quartz-vein, granitoid-related Au vein, Cu-Ag vein, Cu skarn deposits), the Hovd belt (with granitoid-related Au vein, Au skarn, and Cu skarn deposits), the Kizir-Kazyr belt (with Fe skarn and granitoid-related Au vein deposits), and the Martaiginsk belt (with granitoid-related Au vein and Au skarn deposits). The isotopic ages of the deposits or hosting units range from 490 to 420 Ma. The favorable geologic units and deposits are in the Altai and Yenisey-Transbaikal collage and are interpreted as having formed in a continental-margin arc or associated continental-margin turbidite terranes, back-arc basin associated with continental-margin arc magmatism, transform continental- margin faulting, island arc, or terrane accretion. The Kiyalykh- Uzen belt (with Cu skarn, W skarn, Fe skarn, W-Mo-Be greisen, stockwork, and quartz-vein deposits) and the Martaiginsk belt (with granitoid-related Au vein and Au skarn deposits) con- tain collisional granitoids that are interpreted as having been intruded during transpressive (dextral-slip) movement along the Kuznetsk Alatau fault or during terrane accretion. Metallogenic Belts with Volcanic-Hosted Deposits Related to Continental-Margin or Island Arcs Several metallogenic belts possess geologic units favorable for major volcanic-rock hosted deposits, includ- ing the Govi-Altai, Ozerninsky, and Uda-Shantar belts (with volcanogenic-sedimentary Fe, volcanogenic-sedimentary Mn, volcanogenic-hydrothermal-sedimentary massive sulfide, and sedimentary phosphate deposits). The fossil ages of the deposits or host units range from Cambrian through Silurian. The favorable geologic units and deposits are in the Mongol- Okhotsk, South Mongolia-Khingan, and Yenisey-Transbaikal collages and are interpreted as having formed in either conti- nental-margin or island arcs, or in sea floor sedimentation. The Bedobinsk belt with sediment-hosted Cu deposits is hosted in early Paleozoic sedimentary units of the North Asia craton and is interpreted as having formed in an inland-sea basin during the post-saline stage of rock deposition. Kimberlite Diamond Metallogenic Belts Three metallogenic belts possess unique favorable geologic units for diamond-bearing kimberlite deposits in the Sino-Korean craton (East Liaoning belt), evaporite sedimen- tary gypsum deposits in platform sedimentary cover on the Sino-Korean craton (Hunjiang-Taizihe and Jinzhong belts), and banded iron formation (BIF) deposits in continental-mar- gin sedimentary cover on the Sino-Korean craton (South Khin- gan belt). The latter two belts formed during sedimentation along a cratonal margin. The origin of the diamond-bearing kimberlite deposits is not well known. Major Cambrian through Silurian (540 to 410 Ma) Metallogenic Belts and Host Units The major Cambrian through Silurian metallogenic belts are the Bayanhongor-1, Bedobinsk, East Liaoning, Govi-Altai, Hovd, Hunjiang-Taizihe, Jinzhong, Kiyalykh-Uzen, Kizir- Kazyr, Martaiginsk, Ozerninsky, South Khingan, and Uda- Shantar belts (fig. 13, appendix C). Bedobinsk Metallogenic Belt of Sediment- Hosted Cu Deposits (Belt BD) (Russia, Eastern Siberia, Yenisey Ridge area) This Middle to Late Cambrian metallogenic belt occurs along the southwest margin of the North Asian craton along the margin of the Middle to Late Cambrian Priangarsk sedimentary basin. The belt contains the productive southern Priyenisei metallogenic district that extends from Angara to Podkamennaya Tunguska Rivers. The belt is 200 km long and 150 km wide (Bogdanov and others, 1973). The major Cu deposits occur in the middle and upper parts of carbon- ate and clastic rock in the Yeniseisk and Turamsk series that contains mottled anhydrite limestone and dolomite. More than 200 Cu ore occurrences occur in mottled carbonate and clastic rocks that contain the Cu-bearing Middle to Late Cambrian limestone, dolomite, siltstone, and sandstone of the Yeniseisk series. Eight Cu-bearing horizons ranging from 0.3 to 10 m thick are identified. The most significant deposit at Bedobinsk occurs in a horizon that is 2.1 m thick and consists of sand- stone and mudstone with covellite, chalcocite, bornite, fahl, up to 1 percent in cuprite, and up to 0.5 percent malachite and azurite (Borzenko and Sklyarov, 1970). The main references on the geology and metallogenesis of the belt are Bogdanov and others (1973), Narkelun and others (1977), Miroshnikov (1981), and Miroshnikov others (1981). Bedobinskoye Sediment-Hosted Cu Deposit This deposit (Narkelun and others, 1977) consists of stratiform Cu sulfides in the Middle to Late Cambrian argil- laceous, clastic, and carbonaceous rock of the Evenkiisk suite. The Cu sulfide horizon is 2 to 3 m thick. Host lithologies are 5-32 Metallogenesis and Tectonics of Northeast Asia GY GY GY NAC SKC HS HS BJ HS KR ST Bering Sea Pacific Ocean Laptev Sea CS VK VK KOM SA CH oc nb, ol uy, ma oc, us oc, us oc, us oc ol KOR VR OH PA WK OK OK PA WK OK EP WS CS tp EA BP AL AL AL YT YT YT YT YT AR AR TM SM SMAB AB SL SL SL JA WD BJ BJ BJ BJ BD HS HS ea ji sm sm at at ko nm gh lg nr se se ha, mt se ss ss ss tb tb ke us uo sv tr MO CS SH JT JT NN ES SH ja ja ib Sea of Okhotsk Lake Baikal East-Siberian Sea kk MO MO P A C I F I C P L A T E ES ES MO 156 168 188 2,000 km1,0000 EL BE TK MT KK MT HO GA BH SK US HT IB OZ JX VZ, YA Figure 13.  Generalized map of major Cambrian through Silurian metallogenic belts and major geologic units for Northeast Asia.  Refer to text and appendix C for summary descriptions of belts. Refer to figure 2 for explanation of geologic units. Metallogenic belt  outlines adapted from Obolenskiy and others (2003, 2004) and Parfenov and others (2003, 2004). Metallogenic belts for area east of  144 º E (eastern boundary of Northeast Asia project area) are described and interpreted by Nokleberg and others (2003). red aleurolite and siltstone. Host rocks are dolomitic sand- stone, limestone, and marl. Ore minerals are chalcocite, pyrite, hematite, chalcopyrite, bornite, arsenopyrite, fahl, sphalerite, and native silver. Ore minerals occur mainly in cement of sedimentary rocks in disseminations, concretions, and thin laminae. The deposit is medium size and has an average grade of 0.1 to 0.6 percent Cu. Kurishskoye Sediment-Hosted Cu Deposit This deposit (Malich and others, 1987) consists of strati- form Cu minerals in Upper Riphean terrigenous red molasse. The most abundant Cu minerals occur in variegated sedimen- tary rocks formed in a coastal-marine and deltaic facies. Four Cu horizons range from 0.5 to 4.5 m thick and display features 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-35 Prospects Boundaries of: a - Chagoyan ore field, b - Malochukan (I), Chukan (II), and Dzhurkan-Chagoyan (III) ore fields Faults Gold placerTectonic melange of overthrust zones Late Paleozoic granodiorite GraniteAndesite Lower Cretaceous magmatic rock Silurian terrigenous deposits (sandstone, siltstone) LimestoneLimy sandstone and siltstoneDolomite Vendian-Cambrian calcareous deposits: Neogene-Quaternary deposits (sand, sandy clay,siltstone) Modern deposits (gravel, sand, clay) Chagoyan Au-Pb-Zn deposit Pb & ZnFeAu III II I ‚ ŒØ PZ3 PZ3 PZ3 PZ3 PZ3 PZ3 Snr Snr Snr Snr Snr QIV QIV QIV QIV QIV QIV QIV N -Q2 1 N -Q2 1 N -Q2 1 N -Q2 1 N -Q2 1 N -Q2 1 K1 K1 K1 K1 K1 K1 K1 K1 4 km0 2 Fgure 14.  Generalized geologic map of Chagoyan sedimentary exhalative Pb-Zn (SEDEX) district,  Chagoyan metallogenic belt. Adapted from Melnikov (written commun., 1963). 5-36 Metallogenesis and Tectonics of Northeast Asia quartzite bed in amphibolite and schist of the Early to Middle Cambrian Togrog Formation. The bed is 0.5 to 1.0 m thick and extends for 2,000 m. Grade ranges from 3 to 20 percent Mn. Grab samples contain up to 0.015 percent Co, up to 0.02 percent Mo, and up to 0.01 to 0.25 percent Cu. The deposit is medium size and contains resources of 2 million tonnes Mn and 3 million tonnes Fe. Uhiin Ovoo Volcanogenic-Sedimentary Fe  Deposit This deposit (A.A. Rauzer and others, written commun., 1987; Jargalsaihan and others, 1996) consists of magnetite and hematite bearing beds hosted in Middle Cambrian through Early Ordovician chlorite-sericite slate. Beds are 5.0 to 10.0 m by 50.0 to 70.0 m thick and extend up to 4,000 m along strike. Analyses of three grab samples yield 20.5 to 48.4 percent Fe, 1.5 percent Mn, up to 0.08 percent V, and up to 0.01 percent Cu. Origin and Tectonic Control for Govi-Altai  Metallogenic Belt The belt is interpreted as having formed during sedimen- tation along an early Paleozoic continental slope close to the deformed Dzhida-Lake island arc. Hovd Metallogenic Belt of Granitoid-related Au Vein, Au Skarn, and Cu (±Fe, Au, Ag, Mo) Skarn Deposits (Belt HO) (Western Mongolia) This Ordovician through Late Silurian metallogenic belt contains granitoid-related Au vein, Au skarn, and Cu and Fe occurrences related to the Khovd and Turgen granitoid complex that intrudes an Ordovician sedimentary- volcanic-plutonic overlap assemblage in the Hovd conti- nental-margin turbidite terrane and a Silurian sedimentary- volcanic-plutonic overlap assemblage (too small to depict on map at 5 million scale) (Tomurtogoo and others, 1999). The granitoid complex consists of gabbro, diorite, granodio- rite, and biotite-amphibole granite. The metallogenic belt was first defined by Tcherbakov and Dejidmaa (1984) as the Harhiraa Au belt. The major deposits and occurrences are at Hovd, Sharhooloi, Tsetsegnuur, Tsagaantolgoi, Hagshirbu- lag, Yolochka, and Antsavyn. The main references on the geology and metallogenesis of the belt are Tcherbakov and Dejidmaa (1984), Dergunov (1989), Byamba and Dejidmaa (1999a,b), and Tomurtogoo and others (1999). Yolochka Cu (±Fe, Au, Ag, Mo) Skarn Deposit This occurrence (L.B. Chistoedov and others, written commun., 1990) occurs along the major Tsagaan Shiveet fault zone in the western margin of the Nuuryn terrane. The occurrence is hosted in the Vendian through Early Cambrian Tsol Uul Formation, Early Silurian Khutsbulag Formation, and Upper Silurian Hovd intrusive complex. The Tsol Uul Formation consists of andesite, basalt, andesite porphyry, tuff, volcanic breccia, spilite, and limestone. The Khutsbulag Formation consists of sandstone, siltstone and greywacke. The Hovd complex is a small intrusive and consists of a first phase of fine-grained diorite and a second phase of medium- grained granodiorite. Also occurring are abundant dikes of granodiorite porphyry, syenite porphyry, and diabase por- phyry, two fault zones that vary from 20.0 to 200.0 m wide, and small fracture zones that vary from 0.1 to 1.0 m wide. Quartz and siderite veins occur in the fault zones and contain chalcopyrite, chalcocite, malachite, and azurite. Hydrother- mal replacements consist of skarn, and alteration to epidote and silica. The skarns vary from 0.4 to 2.5 m wide and 20.0to 00.0 m long. Some skarns contain pyrite and chalcopyrite. Gangue minerals are epidote, quartz, calcite, and garnet. The average grades in skarn are 0.4 to 1.0 g/t Au, 0.1 to 0.5 percent Cu, up to 0.06 percent Zn, up to 0.2 percent Pb, and up to 2.5 g/t Ag. Origin and Tectonic Controls for Hovd  Metallogenic Belt The belt is interpreted as having formed during oblique accretion and collision of Kuznetsk-Tannuola and Dzhida-Lake island arcs onto the Siberian Continent margin and during subsequent transpression-dextral-slip faulting. The Hovd terrane is part of the Ordovician Tsagaanshiveet continental-margin arc that is built on the Vendian through Cambrian Lake island-arc terrane, and it is linked to the Late Ordovician, subduction- related Turgen complex consisting of gabbro, diorite, granodio- rite and biotitic, biotite-amphibolic granite. Hunjiang-Taizihe Metallogenic Belt of Evaporate Sedimentary Gypsum Deposits (Belt HT) (Northeastern China) This Cambrian through Ordovician metallogenic belt is hosted in the Sino-Korea craton sedimentary cover and occurs in the East Liaoning and East Jilin Provinces, North- eastern China. The belt occurs in the Hunjiang River, East Jilin, Taizihe River, and East Liaoning Provinces. The belt is hosted in the Cambrian and Ordovician overlap sedimentary assemblages of the Jilin-Liaoning-East Shandong terrane. The evaporate sedimentary gypsum deposits occur in the Early Cambrian Mantou Formation in dolomite mudstone, dolomite, and limestone. The metallogenic belt is 300 km long and 20 to 30 km wide. The significant deposit is at Rouguan. The main reference on the geology and metallogenesis of the belt is Ren and Cai (1989). 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-37 Rouguan Evaporate Sedimentary Gypsum  Deposit This deposit (Ren and Cai 1989) consists of thin, concor- dant gypsum beds in Early Cambrian carbonate in the Mantou Formation. Four horizons occur and the main horizon is 2,800 m long and 5.5 m thick. The ores are carbonate and sulphate type with a simple mineralogy. The main minerals are gypsum, karstenite, dolomite, calcite, quartz, illite, and minor mont- morillonite. The sedimentary environment is interpreted as a super-tidal vaporizing Sabkha or high saline basin. The deposit is medium size. Origin and Tectonic Controls for Hunjiang-Taizihe  Metallogenic Belt Gypsum deposits in the belt are interpreted as having formed in a super-tidal sabkha sedimentary environment (Ren and Cai, 1989). The host Cambrian and Ordovician sedimen- tary rock are part of the overlap sedimentary assemblages on the Archean Jilin-Liaoning-East Shandong terrane and consist mainly of very thick carbonates and clastic rock. During the Early Cambrian period, the limited Hunjiang-Taizihe Basins formed along a northeast trend. Jinzhong Metallogenic Belt of Evaporate Sedimentary Gypsum (Belt JZ) (North China) This Cambrian through Silurian metallogenic belt is hosted in sedimentary units in the the Sino-Korea craton sedimentary cover and occurs in the central part of southeast Shanxi Province, Northern China. The belt is hosted in an overlap sedimentary assemblage deposited on the Archean West Liaoning-Hebei-Shanxi terrane. The belt trends north- south, is more than 600 km long, and ranges from 20 to 30 km wide. The gypsum deposits are hosted in limestone horizons in Early and Middle Ordovician strata. The most significant deposit is at Taiyuan. The main references on the geology and metallogenesis of the belt are Wang Hongzhen (1985) and Tao Weiping and others (1994). Taiyuan Evaporate Sedimentary Gypsum Deposit This deposit (Yuan, Jianqi, and Cai, Keqin, 1994) consists of gypsum-bearing strata in evaporate rocks in the Early Ordovician Majiagou Formation. The gypsum-bearing strata range from 118 to 207 m thick. The strata are divided into the following members: (1) lower limestone; (2) lower gypsum; (3) middle limestone; (4) upper gypsum; (5) inter- bedded dolomite and limestone; and (6) upper limestone. Ten layers of gypsum occur, with nine layers in the upper gypsum member and one in the lower gypsum member. The average thickness of each layer is 1.0 to 2.49 m. Generally, where the gypsum member is thicker, the thickness of gypsum layer is correspondingly larger. The gypsum layers occur continuously along strike for several thousand meters and extend downdip to more than 1,000 m. Some laminated and banded gypsum layers frequently contain halite pseudomorphs and mud cracks. However, most gypsum layers consist of crystalloblas- tic, coarse-grained gypsum replacing anhydrite. The deposit is interpreted as evaporate layers that formed in a tidal zone. The deposit is large. Origin and Controls for Jinzhong Metallogenic  Belt The gypsum deposits in the belt are interpreted as having formed in a large epicontinental marine basin that comprises the most extensive sedimentary cover on the North China Platform. The metallogenic belt is the most significant in the North China Platform and is hosted in Middle Ordovician limestone and gypsum formations that contain multiple cycles with a group of large gypsum deposits (Wang, 1985; Tao and others, 1994). Jixi Metallogenic Belt of Banded Iron Formation (BIF, Algoma Fe), Homestake Au, Metamorphic Graphite, and Metamorphic Sillimanite Deposits (Belt JX) (Northeastern China) (Started in Neoproterozoic (See above description) Kiyalykh-Uzen Metallogenic Belt of Cu (±Fe, Au, Ag, Mo) Skarn, W±Mo± Be Skarn, Fe Skarn, and W-Mo-Be Greisen, Stockwork, and Quartz-Vein Deposits (Belt Kiy) (Kuznetsk Alatau, Russia, Southern Siberia) This Early Ordovician through Early Silurian metallo- genic belt is related to the Tannuola plutonic belt located in the Altai-Sayan back-arc basin (Mrassu-Bateni unit) and occurs along the southeastern slopes of the Kuznetsk Alatau Ridge. The belt is oval and trends sublongitudinally for 150 km and ranges from 50 to 80 km wide. The deposits are concentrated in early Paleozoic granitoids that intrude Vendian and Cam- brian carbonate and clastic shelf rocks, and rarely in Cambrian volcaniclastic and carbonate sedimentary rock. The deposits occur in (1) contact zones of granitoid intrusions and as skarn in large xenoliths of host rocks; and (2) endocontact zones and cupolas of granitoid plutons in greisens and veins. The depos- its are controlled by zones of intersection of northwest- and northeast-trending faults. Cu skarn deposits are predominant. Most deposits are small. The Kiyalykh-Uzen, Juliya Mednaya Cu (±Fe, Au, Ag, Mo) skarn and the Tuim W (±Mo±Be) skarn deposits are mined. 5-40 Metallogenesis and Tectonics of Northeast Asia and the Altai-Sayan back-arc basin. The belt extends along the eastern slope of the Kuznetsk Alatau Ridge for up to 500 km with breaks and ranges from 30 to 60 km wide. The belt is 250 km wide in the Kuznetsk Alatau. Most of the Au deposits occur along the Kuznetsk Alatau branch of the belt. The belt occurs along the hanging wall of the Kuznetsk Alatau fault zone that exhibits complex relations between Precambrian and early Paleozoic sedimentary, extrusive, and intrusive rocks. The granitoid-related Au deposits occur in early Paleozoic granitoid batholiths, in relatively older gabbro and norite intru- sions, in andesite, basalt, and andesite porphyry, and in com- plexly deformed volcanic and sedimentary rock (Alabin and Kalinin, 1999). Au skarn deposits occur along contact between the early Paleozoic granitoid plutons and companion stocks and consist of magnesium-silicate and calc-silicate skarn. The most abundant Au deposits occur in brecciated and recrystal- lized skarn. Au-rich wollastonite skarn at the Sinyukhinskoye deposit extends to 500 m depth. Also occurring are Au-sulfide- quartz veins in some Au-skarn deposits. This relation links the two types of Au deposits in the belt. The majority of Au-skarn deposits occur at the western part of the Martaiginskiy metal- logenic belt where it overlaps with the Taidon-Kondomsk Fe-Mn metallogenic belt. Lode-Au deposits are the sources of numerous Au placers that have been mined during last 150 years. The major deposits are at Sarala, Natal’evskoye, Kom- somolskoye, and Sinyukhinskoye. The main references on the geology and metallogenesis of the belt are Sotnikov and others (1995, 1999), Berzin and Kungurtsev (1996), Sharov and others (1998), Shirokich and others (1998), and Alabin and Kalinin (1999). Komsomolskoye Granitoid-Related Au Vein  Deposit This deposit (Denisov, 1968) (fig. 15) consists of quartz- sulfide veins hosted in Ordovician-Silurian gabbro and diorite stock that intrudes Cambrian carbonaceous and volcanic rock. The stock is oval with dimensions of 5 by 3.5 km. Multiple xenoliths of contact metamorphosed and skarn-altered host rock occur in gabbro and diorite massif. About 150 quartz veins occur in the five districts. Single veins range up to 1.5 km long and 5 m thick. Wallrock alterations are beresite alteration, silica alteration and sulfide alteration. The deposit minerals are pyrite, pyrrhotite, sphalerite, arsenopyrite, galena, chalcopyrite, scheelite, and native gold. Native gold is associ- ated with arsenopyrite and galena. The deposit is small. Sarala Granitoid-Related Au Vein Deposit This deposit (Miroshnikov and Prochorov, 1974; Sazonov and others, 1997; Shirokich and others, 1998) consists of a group of quartz-carbonate and sulfide veins hosted in Early to Middle Cambrian volcanic and sedimentary rock that is meta- morphosed and hydrothermally altered. The veins are related to early Paleozoic gabbro, diorite and granite intrusives. More than 250 veins occur in seven districts. Two types of veins are defined according to size (1) single veins that are up to 3 km long and 1.5 to 2 m thick (up to 4 to 5 m in swells) are the most economically important and comprise the bulk of Au reserves; and (2) more common veins that are several hundred meters long (rarely up to 1 km), are 0.2 to 0.6 m thick, and occur in berezite, silica, sericite and listvenite alteration zones. Grade of Au in altered wall rock varies from minor to 57 g/t Au. Ore minerals assemblages are quartz, pyrite, and scheelite; quartz, pyrite, and arsenopyrite; and quartz, pyrite, sphalerite, galena, and calcite. Average sulfide content is 4.75 percent. Native Au occurs mainly with arsenopyrite, sphalerite, and galena. Fineness of Au ranges from 483 to 911 (mainly 680 to 790). The deposit is medium size and has an average grade of 8.4 g/t Au. Natal’evskoye Au Skarn Deposit This deposit (Alabin and Kalinin, 1999) consists of a group of Au skarn bodies with a complicated mineral assem- blage that occur along the contact of the Ordovician and Silurian Natal’evsk granitoid stock that intrudes Vendian and Cambrian andesite and basalt porphyry and tuff that are interbedded with chlorite and carbonaceous-siliceous schist, limestone, and dolomite. The skarn contains an older assemblage of magnesium-silicate minerals (diopside, spinel, phlogopite, and serpentine), and a younger assemblage of calcsilicate minerals (garnet, pyroxene, wollastonite, tremolite, and vesuvianite). Ore minerals are mainly magnetite, chal- copyrite, cubanite, and bornite, and lesser pyrite, pyrrhotite, sphalerite, galena, native Au, molybdenite, and native bismuth. Fineness of Au is of 760 to 820 pm. Sulfides comprise from 3 to 8 percent skarn. The main Au-minerals are chalcopyrite and bornite. Skarn, that is brecciated, recrystallized and slightly hydrothermally altered (albite, actinolite, and silica alteration), is most enriched in Au. The deposit is small. Sinyukhinskoye Au Skarn Deposit  This deposit (Luzgin, 1974; Korobeinikov and others, 1997; Sharov and others, 1998) consists of quartz-carbonate and Au-Cu-sulfide skarns that occur in a contact zone of an Ordovician and Silurian granitoid pluton intruding Middle Cambrian volcanic and sedimentary rock. Various wollas- tonite, pyroxene, and garnet skarn occurs along contact of volcanic rock and rare dikes with carbonates. Various age dike complexes are widespread. The oldest diabase and spesartite dikes intrude skarn and also metasomatized. Younger quartz diorite porphyrye and felsite dikes are not metasomatized, but contain Au-sulfide deposits that contain economic Au that formed during post-skarn hydrothermal metasomatism that resulted in silica alteration and sulfide replacement. The Au-skarn deposits occur in irregular masses, nest, lenses, and stockworks. Individual skarn bodies range from ten to several hundred meters long. The thickness of ore veins ranges from 2 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-41 Figure 15.  Generalized geologic map of Komsomolskoye Au district. Martaiginsk metallogenic belt. Adapted  from Denisov (1968). Ore-bearing structure Deposit or prospect Turbidite (J -K )3 1 Rhyolite flow (K )2 1 Andesite flow (K )2 2 Subvolkanic andesite (K )2 2 Basalt (N-Q) Diorite-granodiorite (Puril’sk complex) (K )2 Monzonite (Silinsk complex)(K ),2 Granite (Chalba complex) (K )2 Fault 0 3 6 9 km 5-42 Metallogenesis and Tectonics of Northeast Asia to 6 m. The veins occur mainly in skarn and to a lesser extent in magnetite masses and wall rocks. A gold-chalcocite-bornite assemblage is typical for upper part of deposit, and Au-chalco- pyrite is typical in deeper levels. The deposit is medium size amd has reserves of 20 tonnes Au. Origin and Tectonic Controls for Martaiginsk  Metallogenic Belt The belt is interpreted as having formed during oblique accretion and collision of Kuznetsk-Tannuola and Dzhida-Lake island arcs onto the Siberian Continent margin and during sub- sequent transpression-dextral-slip faulting. The deposits occur in clusters along branches of the Kuznetsk Alatau fault and along intersections with transversal sublatitudinal faults. The belt occurs in a terrane collage of fragments of an island-arc system and an active continental margin (Berzin and Kungurtsev, 1996; Alabin and Kalinin, 1999). The granitoids consist of an older gabbro sequence and a younger granitoid sequence. The origin of Au-sulfide-quartz vein deposits (Cen- tralnoye, Berikul, Komsomolskoye, Kommunar, Sarala) and Au skarn deposits (Natalevskoye, Sinyukhinskoye) is related to early Paleozoic collisional granitoid of the Martaiginsk and Lebed complexes (Berzin and Kungurtsev, 1996) that are interpreted as having been derived from calc-alkaline andesite mantle melt. The initial 87Sr/86Sr ratio in accessory apatite from granite ranges from 0.7043 to 0.7044 (Sotnikov and others, 1999). The 40Ar/39Ar isotopic age for granitoid of the Martai- ginsk complex is 480 to 460 Ma (Sotnikov and others, 1995). Similar data occur for granite in the Lebed complex with a K-Ar isotopic age of 445 to 427 Ma. Rb-Sr isotopic ages for gangue minerals and metasomatite are 472 ± 10 Ma at Gavrilovskoye; 458 ± 4 Ma at Centralnoye; 444 ± 4 Ma for Komsomolskoye; and 433 ± 17 Ma for Sarala. Some studies suggest the Au deposits may be related to dike complexes superimposed on the Martaiginsk and Lebed granitoids (Shirokich and others, 1998). Ozerninsky Metallogenic Belt of Volcanogenic- Hydrothermal-Sedimentary Massive Sulfide Pb, Zn (Cu), Sediment-Hosted Cu, and Volcanogenic- Sedimentary Fe Deposits (Belt OZ) (Russia, Western Transbaikalia) This Cambrian metallogenic belt is hosted in the Eravna island-arc terrane that is overlapped by the Barguzin-Vitim and Transbaikalia sedimentary and volcanic-plutonic belts. The belt occurs in the central part of Vitim Lowland in the upper drainages of the Uda and Vitim Rivers. The belt extends for more than 150 km and ranges up to 75 km wide. The Eravna island-arc terrane consists of volcanic and sedimentary rocks of the Vendian and Cambrian Oldynda suite (Beli- chenko, 1969, 1977). The volcanic part is mainly rhyolite, dacite, andesite, and rhyolite, with minor diabase and basalt porphyry. Pyroclastic units predominate over flows. Also occurring are widespread subvolcanic stocks and sills of lava breccias and minor diabase and andesite porphyry dikes and sills. The sedimentary rocks are mainly limestone and minor carbonaceous and carbonataceous shale, siltstone, and sand- stone. The carbonaceous rocks contain reefs, bioherms, and biostromes. Sedimentary rock of the Eravna terrane occur only as scattered, variable-size roof pendants in plutons in the large Barguzin-Vitim batholith with an isotopic age of 320 to 280 Ma (Yarmolyuk and others, 1997). The Ozerninsky roof pen- dant covers 200 km2 and hosts the Ozerninsky metallogenic belt that contains more than twenty stratiform pyrite, polyme- tallic sulfide, and ferric Fe deposits and ore occurrences. The main deposits are the Ozernoye, Zvezdnoye, Ulzutuyiskoye, and Nazarovskoye volcanogenic hydrothermal-sedimentary Pb, Zn, Cu deposits, the Gundui and Turkal volcanogenic hydrothermal Cu deposits. The major deposits are at Ozer- noye, Ulzutuyskoye, and Gundui. The main references on the geology and metallogenesis of the belt are Belichenko (1969, 1977), Tarasova and oth- ers (1972), Distanov (1977), Nefediev (1986), Distanov and Kovalev (1996), Belichenko and others (1994), Tsarev (1995), and Yarmolyuk and others (1997). Gundui Volcanogenic-Hydrothermal Cu Deposit This metasomatic deposit (Tsarev and Firsov, 1988; Kova- lev and Buslenko, 1992; Tsarev, 1995) occurs in an outlier of Early Cambrian carbonate and pyroclastic rocs along a contact with quartz-plagioclase porphyry. The deposit contains two large steeply dipping occurrences that range from 300 to 1000 m long, are 600 m deep, and vary from 8 to 105 m thick. Also occurring are three small occurrences along a major fault that also controls five Fe and Cu deposits. The ores minerals are chalcopyrite, barite, and magnetite. Lenses and layers of barite, chalcopyrite-barite, magnetite, apatite-magnetite, Cu-pyrite also occur and contain magnetite, chalcopyrite, pyrite, hematite, bar- ite, siderite, pyrrhotite, sphalelite, galena, bornite, and apatite. Gangue minerals are ankerite, calcite, quartz, chlorite, epidote, and K-feldspar. Chalcopyrite occurs as disseminations in and in masses with magnetite. Metamorphism formed chalcopyrite and barite nests and veins. Local siliceous and quartz-albite-chlorite metasomatite occur. The deposit is medium size and has an average grade of 0.92 percent Cu, 22 to 31 percent Fe, and 27 to 46 percent barite. Ozernoye 2 Volcanogenic-Hydrothermal- Sedimentary Massive Sulfide Deposit This deposit (Distanov, 1977; Tsarev, 1995; Distanov and Kovalev, 1996) (fig. 16) consists of stratified bodies of layered, banded, lenticular and complex form.The bodies extend from 1300 to 2340 m, thickness from 1-2 to 30-45 m.The deposit occurs in layers and extends to a depth of 350 m. The deposit is interpreted as pyrite-polymetallic type. The deposit miner- als are primarily Zn with admixture of galena. Major deposit 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-45 0 1 2 3 km Schist (Cambrian) Limestone (Cambrian) Ironstone (Cambrian) Manganese ore (Cambrian) Dolomite sedimentary breccia (Cambrian) Fault Contact basalt, ribbon chert, and siliceous shale; and (3) olistostrome. Each rock sequence occurs in independent tectonic slices and sheets that are separated by ductile faults that occur parallel to bedding in the sheets. Internal parts of the sheets are com- paratively weakly deformed. The significant deposit is the Gerbikanskoe volcanogenic-sedimentary Fe deposit. Other significant deposits are the North-Shantarskoe, Nelkanskoe, Ir-Nimiiskoe-2, and Lagapskoe sedimentary P deposits, and the Ir-Nimiiskoe-1, Milkanskoe, Galamskoe, Kurumskoe, and Itmatinskoe volcanogenic-sedimentary Fe and Mn deposits. The major deposits are at Gerbikanskoe, North-Shantarskoe, Ir-Nimiiskoe 1 and 2, Lagapsko, and Nelkanskoe. The main references on the geology and metallogenesis of the belt are Shkolnik (1973) and Khanchuk (1993). Gerbikanskoe Volcanogenic-Sedimentary Fe  Deposit This deposit (Shkolnik, 1973) (fig. 18) consists of two zones separated by a sequence of sandstone and siltstone. The zones consist of approximately 30 steeply dipping, sheeted and lenticular bodies of magnetite and hematite. Individual bodies range from several tens of m to 5 to 7 km long and are sometimes closely spaced in an en-echelon pattern. Thickness varies from 5 to 50 m and is commonly 8 to 28 m. Fe min- eral layers vary from banded to thinly banded, lenticular, and bedded, and consist of finely dispersed hematite, magnetite, and rare pyrite and chalcopyrite. The deposit is large and has an average grade of 42 to 43 percent Fe (soluble Fe 33 to 53 percent), 1.8 percent Mn, and 9.6 percent P. North-Shantarskoe Sedimentary Phosphate  Deposit This deposit (Shkolnik, 1973) consists of phosphorite deposits that occur in a sedimentary breccia with indistinct borders. The deposit ranges up to 15 to 16 m thick and is hosted in carbonate rock in a sequence of chert and volcanic rock that are partially altered to quartz-carbonate rock. The sequence occurs for approximately 8 to 10 km at the northeast end of Bolshoi Shantar Island. The deposit is small with an average grade of less than 6 to 8 percent P2O5. Nelkanskoe Sedimentary Phosphate Deposit This deposit (Shkolnik, 1973) consists of a phosphorite sedimentary breccia that occurs in a steeply dipping sequence of jasper and volcanic rock that is exposed in an erosional window below gently dipping Jurassic sedimentary rock. Host rocks are silicified dolomite and limestone. Phosphorite beds range up to 1.8 km long, however, some are only several tens of meters long. Thickness varies from 2 to 41 m. The deposit drilled to almost 300 m. In addition to fragments of primary phosphorite, the deposit contains fragments of silici- fied carbonate rocks that range from 0.5 to 2 cm wide and are cemented by phosphate and hydromica. Phosphates are radioactive. The deposit is small. The grade ranges from 4 to 30 percent P2O5 and averages 7 to 11 percent. Ir-Nimiiskoe-2 Sedimentary Phosphate Deposit This deposit (S.G. Kostan’yuan and others, written com- mun., 1973) consists of numerous and unusual phosphorite bodies that occurs in a sedimentary breccia formed in atoll fans and seamounts. The deposits occur in an area 25 to 30 km long and 6 to 8 km wide and are hosted in complex, steeply dipping, and folded rocks that comprise a reef edifice. Some carbonate is silicified. Boundaries of deposits are gradational due to variable amount of fragments of primary phosphorite in dominant host limestone, dolomite, and siliceous carbon- ate, and in rare jasper, volcanic rock, and siliceous claystone fragments. Primary phosphorite occurs mainly in thin beds and small lenses of coquina that consists predominantly of inar- ticulate brachiopods with phosphate shells and some Cambrian trilobites. Phosphorite breccia occurs at various stratigraphic levels with no clear boundaries. The margin is determined by Figure 17.  Schematic cross section of South Khingan  banded iron formation deposit, South Khingan metallogenic  belt. Adapted from V.A. Yarmolyuk and A.P. Glushkov (written  commun., 1966)  5-46 Metallogenesis and Tectonics of Northeast Asia A B BA 0 m 400 m 0 400 800 m Sandstone Interbedded sandstone, siltstone, and chert Chert Granodiorite (Early Cretaceous) Ore body Contact metamorphic zone Sedimentary rocks (Cambrian) Map Cross Section Figure 18.  Generalized geologic map and schematic cross  section of Gerbikanskoe volcanogenic-sedimentary Fe deposit,  Uda-Shantar metallogenic belt. Adapted from Shkolnik (1973). sampling. Approximately 30 phosphorite layers are identified. Layers range from several tens of m to several km long and are commonly discontinuous. The deposit generally has simple mineral composition. In addition to phosphorite, the deposit contains quartz, dolomite, calcite, rare pyrite, chert, and volcanic rock fragments. Thickness of the phosphorite ranges from 0.5 to 24 m, but varies greatly over short distances. The deposit is medium size. Phosphorus anhydrite ranges from 3 to 12 percent and averages 7 to 8 percent. Lagapskoe Sedimentary Phosphate Deposit This deposit (Zagorodnykh, 1984) consists of carbonate beds that contain phosphorite breccia with Cambrian fossils. Beds locally range up to 30 m thick, but generally range from several tens of cm to 20 m thick. Phosphorite breccia con- tains fragments of primary phosphorite, dolomite, limestone, and rare jasper, schist, and shale. Carbonate is commonly completely altered to quartz-carbonate layers intercalated with jasper, shale, schist, siltstone, spilite, basalt, and basalt tuff. The deposit is medium size and contains from 4 to 30 percent anhydrous phosphorous and averages 5 to 7 percent. Ir-Nimiiskoe-1 Volcanogenic-sedimentary Mn  Deposit This deposit (Shkolnik, 1973) consists of partly meta- morphosed, steeply dipping, lenticular and sheeted, bedded Mn bodies that occur in a diverse Early Cambrian sequence of jasper, shale, spilite, basalt, and basaltic tuff that overlies a carbonate reef complex and seamounts. Mn bodies range from several tens to several hundred m long, and vary from 1.5 to 120 m thick. Bodies vary from massive and banded to thinly banded. Mn bodies consist of oxidized braunite, hausmannite- rhodochrosite, rhodochrosite, and rhodonite-rhodochrosite. Bodies also contain quartz and minor magnetite, hematite, manganite, sulfides, piedmontite, manganophyllite, viridine, amphiboles, muscovite, and plagioclase. Mn content varies greatly, extending up to 50 to 56 percent Mn in oxidized ore and 47 percent Mn in carbonate ore, along with 0.01 to 0.12 percent P, up to 3 percent Fe, and 9 to 70 percent SiO2. The deposit is small. The average grade is about 22.4 percent Mn. Origin and Tectonic Controls for Uda-Shantar  Metallogenic Belt The belt is interpreted as having formed during sea floor hydrothermal activity associated with basaltic volcanism that was accompanied by chert deposition in basins. The volcanogenic-sedimentary Fe deposits in the belt consist of numerous lenticular and sheeted magnetite bodies that consist of conformable, steeply dipping layers. The volcanogenic- sedimentary Mn deposits consist of partly metamorphosed, steeply dipping, lenticular and sheeted, bedded Mn bodies that occur in a diverse Early Cambrian sequence of jasper, shale, schist, spilite, basalt, and basalt tuff that overlays a carbonate reef complex with seamounts. The sedimentary P deposits are interpreted as having formed in limestone caps that formed in two stages on accreted seamounts, atolls, and guyots. The host units and deposits were subsequently incor- porated into the host Galam accretionary-wedge terrane that was tectonically linked to the Devonian North Okhotsk (Uda) magmatic arc that formed along the Stanovoy block of the North Asian craton. Voznesenka Metallogenic Belt of Korean Pb-Zn Massive Sulfide Deposits (Belt VZ) (Russia, Far East) This Cambrian through Ordovician metallogenic belt occurs in layers in marine sedimentary units in the Voznesenka passive continental-margin terrane of the Khanka superterrane 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-47 that is a fragment of a Paleozoic active continental-margin arc. The Voznesenka terrane consists of two major units. (1) Cam- brian sandstone, pelitic schist, rhyolite, felsic tuff, limestone, and dolomite that range up to several thousand meters thick, are intensely deformed, and are intruded by Ordovician colli- sion biotite and Li-F protolithionite granitoids with Rb-Sr and Sm-Nd isotopic ages of 450 Ma; and (2) Ordovician through Early Silurian conglomerate and sandstone. Overlapping assemblages range from Early Devonian through Late Perm- ian. The massive sulfide deposits generally occur conformable to organic-rich, bituminous limestone near a contact with over- lying marl. Banded magnetite associated with algae bioherms is a peculiar association with stratiform sulfide deposits of the Voznesenka metallogenic belt. The significant deposits are at Voznesenka-I and Chemyshevskoe. The main references on the geology and metallogenesis of the belt are Androsov and Ratkin (1990), Khanchuk and Slate and siltstone Slate, siltstone, chert Black limestone and dolomitic limestone Dolostone and limestone Basalt and andesite dikes (Late Cretaceous and early Tertiary) Granite porphyry (Late Paleozoic) Diorite (Middle Paleozoic) Li-F granite (Early Paleozoic) Skarn Fluorite-bearing greisen (fluorite ore) Cambrian massive sulfide ore Fault Contact 0 1 km Voznesenka I Voznesenka II Sedimentary rocks (Early Cambrian) others (1996, 1998), Bazhanov (1988), and Belyatsky and Krymsky (1999). Voznesenka-I Korean Pb-Zn Massive Sulfide  Deposit This deposit (Androsov and Ratkin, 1990) (fig. 19) con- sists of massive and thick-banded sphalerite and magnetite- sphalerite layers in Early Cambrian bedded limestone turbi- dite. The deposits are lenticular, 1 to 2 m thick, 20 to 100 m long, and occur in dolomitic limestone and marl. The sulfide bodies and host rocks are folded and regionally metamor- phosed. The sulfide bodies were locally altered to skarn and greisen during emplacement of a Silurian granitic stock that intrudes the carbonate unit. The deposit is medium size and has an average grade of 4 percent Zn. Figure 19.  Generalized geologic map of Voznesenka-1 Korean Pb-Zn massive sulfide deposit, Voznesenka metallogenic belt.  Adapted from Ratkin (1995). 5-50 Metallogenesis and Tectonics of Northeast Asia ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ v v v v v + W E Surficial deposits (Quaternary) Basic and intermediate dikes (middle or late Paleozoic) Greisen (altered granite) Fluorite-altered limestone Fluorite ore Slate Limestone Fault zone Contact0 120 m 400 M 200 M 0 M Late Cambrian Early Cambrian Early to Middle Neoproterozoic (1000 to 650 Ma) Metallogenic and Tectonic Model Cratons, Passive Continental-Margin, and  Cratonal Terranes The major tectonic events in the Neoproterozoic for cratons, passive continental margins, and cratonal terranes (fig. 22) were as follows. 1. Passive continental margins formed on the submerged margins of the North-Asian craton, including the East Angara (NAE), Baikal-Patom (NAP), and Verkhoyansk (fold- and thrust-belt) terranes (NAV), and associated ter- ranes, including the Argunsky, Central Angara, Idermeg, West Angara passive continental-margin terranes; 2. Widespread intracontinental rifting was initiated along the passive continental margins; 3. Platform cover accumulated onto the inner parts of the North-Asian craton; 4. Shallow-water marine sediments accumulated on the Sino-Korean craton; and 5. Several major island-arc systems and tectonically linked subduction zones formed offshore or far away from the North Asian craton, including the Near-Yenisey, Baikal- Muya, and Zavhan magmatic arcs. Near-Yenisey Island Arc Remnants of the late Proterozoic Near-Yenisey arc are preserved in the Circum-Siberia collage (figs. 2, 22; appendix B), that is Proterozoic and accreted in the Neopro- terozoic, in the Isakov (IS) and Predivinsk (PR) island-arc terranes (Kuzmichev, 1990; Vernikovskiy, 1996, 2002). The terranes are overthrust eastward onto either the West Angara (WAG) passive continental-margin terrane or older units of the North Asian craton (NAC). The polarity of the subduc- tion zone based on the structural position of the ophiolite- clastic melange is interpreted as dipping oceanward, away from continent (fig. 22). The age of the arc is still a question. Dating of island-arc plagiogranite and volcanic units has yielded ages ranging from 700 to 630 Ma (Vernikovskiy, 2002). The Isakov terrane is unconformably overlapped by the Neoproterozoic-Vendian sediments of the Vorogovka- Chapa Basin (Sovetov, 2001). Figure 21.  Schematic cross section of Voznesenka-2 fluorite fluorite greisen deposit, Yaroslavka belt. Adapted from Androsov and  Ratkin (1990) and Ryazantzeva (1998). 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-51 Baikal-Muya Island Arc Remnants of the Neoproterozoic Baikal-Muya arc are part of the Tuva-Mongolia superterrane that is late Riphean and older and accreted in the late Neoproterozoic (figs. 2, 22; appendix B) in the Baikal-Muya (BM) and Sarkhoy (SR) terranes in the Transbaikal region and northern Mon- golia (Berzin and Dobretsov, 1994; Konnikov and others, 1994; Kuzmichev and others, 2001; Obolenskiy and others, 1999). Remnants of the arc are unconformably overlapped by Vendian-Cambrian rocks of the Upper Angara Basin and Huvsgol-Bokson overlap assemblage. Tectonically paired to the Baikal-Muya island arc was a subduction zone that is now preserved in the Hug (HU) and Olokit-Delunuran accretionary-wedge (OD) terranes (fig. 22). The position of accretionary-wedge terranes relative to the island-arc igneous-rock units, and the lack of the subduction signs at the periphery of the Baikal-Patom passive continen- tal margin suggest that the subduction zone dipped to the southeast under the island arc (fig. 22) (Berzin and Dobretsov, 1994). Strike-slip faulting occurred between the Baikal-Muya and Near-Yenisey arcs along the Main Sayan strike-slip fault (fig. 22). The arc is associated with back-arc, forearc, rift, and mélange units in the Kuvai terrane (KUV). The terrane is unconformably overlapped by the Vendian-Cambrian sedi- ments of the Mana Basin (Khomentovskiy and others, 1978). Zavhan Magmatic Arc A fragment of the Late Proterozoic Zavhan magmatic arc occurs in Central Mongolia in the Zavhan (ZA) active continental-margin terrane (Tomurtogoo, 2002) that is also a part of the Circum-Siberia collage (figs. 2, 22, appendix B) that is Proterozoic and accreted in the Neoproterozoic. The ini- tial relation of the magmatic arc to the adjacent Baydrag (BY) cratonal terrane is unknown. The Zavhan and Baydrag terranes are unconformably overlapped by the latest Neoproterozoic through Middle Cambrian Huvsgol-Bokson (hb) sedimentary assemblage (Il’in, 1982). The subduction zone was southwest of the magmatic arc. Alpine-type ultramafic and associated units in the Tasuul terrane (TS) form part of an accretionary wedge assemblage that was obducted onto western margin of the Zavhan terrane (Tomurtogoo, 2002). The western and eastern ends of the magmatic arc occurred along dextral shear zones that were subparallel to the continental margin (fig. 22). Metallogenesis The major Neoproterozoic metallogenic belts formed in a variety of tectonic environments (figs. 3, 22; appendix C). In the Angara-Pit belt (AP, figs. 3, 22; appendix C), the sedimentary Fe-oxide deposits are interpreted as hav- ing formed during Upper Riphean preorogenic subsidence of the North Asian cratonal margin in a back-arc (interland) sedimentary basin. The Baikalo-Muiskiy belt (BM, figs. 3, 22; appendix C) is hosted in the Yenisey-Transbaikal collage and Tuva-mongolia superterrane, and it contains volcanogenic-hydrothermal-sedi- mentary massive sulfide Pb-Zn (±Cu), polymetallic (Pb, Zn, Ag) carbonate-hosted metasomatite, and serpentinite-hosted asbestos deposits. These deposits are interpreted as having formed in the Baikal-Muya island arc (part of the Tuva-Mongolia superter- rane), or during Riphean accretion of the Muya metamorphic and Olokit-Delunuran subduction-zone terranes. The Bodaibinskiy belt (BO, figs. 3, 22; appendix C) con- tains Au in black shale deposits that are interpreted as having formed in the Baikal-Muya island arc or during Riphean accre- tion of terrane with the Muya metamorphic terrane and Olokit- Delunuran subduction-zone terrane. Initial gold deposition occurred during sedimentation and during later metamorphism and hydrothermal activity. Subsequent Neoproterozoic post-col- lisional magmatic and hydrothermal activity formed economic deposits. Subsequent formation of gold-silver-sulfosalt deposits occurred during magmatic and hydrothermal activity in the middle and late Paleozoic. The formation of these Au deposits began from early syngenetic sedimentary stage in the Riphean and continued with formation of nappes and folds, and intrusion of collisional granitoids and associated metamorphism in the Vendian and Early Cambrian, and continued with anorogenic granitoid magmatism in the Mississippian. The Bokson-Kitoiskiy belt (BK, figs. 3, 22; appendix C) is hosted in the North Asian cratonal margin, Patom fold- and thrust-belt and contains sedimentary bauxite, magmatic neph- eline, and serpentine-hosted asbestos, and Au in shear-zone and quartz-vein deposits that are interpreted as having formed in multiple events. The metallogenic belt is a composite that includes several mineral-deposit types. The belt is hosted in met- amorphic, oceanic, subduction-zone, and tonalite-trondhjemite- gneiss terranes that underwent Cambrian through Silurian metamorphism, hydrothermal alternation, and plutonic intrusion. The Central-Yenisei belt (CY, figs. 3, 22; appendix C) contains Au in black shale, Au in shear-zone and quartz-vein, and clastic-sediment-hosted Sb-Au deposits that are hosted in the Central Angara passive continental-margin terrane, part of Central Siberia collage. The gold deposits are interpreted as having formed during collisional development of the late Riphean continental margin of the North Asian craton. Gold initially occurring in black shale was subsequently concen- trated and remobilized during collision-related metamorphism, granitoid intrusion, and hydrothermal activity. Most of the large Au and Au-Sb deposits in the Yenisei Ridge consist of multistage polygenetic sedimentary, metamorphic, and hydro- thermal origins with primary accumulation of gold in black shales and subsequent concentration and remobilization during metamorphism and granitoid-related hydrothermal activity (Li, 1974a,b; Berger, 1981; Nekludov, 1995). The Damiao belt (DM, figs. 3, 22; appendix C) contains mafic-ultramafic related Ti-Fe (V), zoned mafic-ultramafic Cr-PGE deposits that are hosted in mafic-ultramafic plutons intruding the West Liaoning-Hebei-Shanxi granulite-orthog- neiss terrane in the Sino-Korean craton. The belt is interpreted 5-52 M etallogenesis and Tectonics of N ortheast Asia -30 60 PB IG AP CY VA BK BM KY DM BO JX PS HO KA MS GG MM GOBI - AMUR MICROCONTINENT BRG HM SINO-KOREAN CRATON N N E E AR Y ISE A Y R C BA IK AL -M UY A ARC ZAVHAN ARC KOM OH AK KOP 0 2,000 km1,000 HX JI OL GN AR ID NAT NAP NAE NAV DR SA CTC HU SR KUV Central Taimyr Superterrane WST WST BY SHE AY PR IS GEOLOGIC UNITS METALLOGENIC BELTS AK - AR - Argunsky terrane AY - Ayansk terrane BRG - Barguzin terrane BY - Baydrag terrane CTC Chelyuskin terrane DR - Derba terrane Gargan terrane GN - Gonzha terrane HM - Hamar-Davaa terrane HX - Hutaguul-Xilinhot terrane Hug terrane ID - Idermeg terrane Isakov terrane JI - Jiamusi terrane Kan terrane KOM - Kolyma-Omolon superterrane KOP - Kuvai terrane MM - Mamyn terrane Muya terrane NAE - North Asian Craton Margin (East Angara fold and thrust belt NAP - North Asian Craton Margin (Patom-Baikal fold and thrust belt NAT - North Asian Craton Margin (South-Taimyr fold belt NAV - North Asian Craton Margin (Verkhoyansk fold and thrust belt OL - Oldoy terrane SA - Sangilen terrane SHE - Shevli terrane Sarkhoy terrane WST - West Stanovoy terrane AP - Angara-Pit BK - Bokson-Kitoiskiy BM - Baikalo-Muiskiy BO - Bodaibinskiy CY - Central-Yenisei DM - Damiao HO - Hovsgol IG - Igarsk JX - Jixi KY - Kyllakh PB - Pribaikalskiy - Prisayanskiy VA - Vorogovsko-Angarsk Avekov - GG - HU - IS - KA - Prik KUV - MS - SR - PS terrane olyma terrane Okhotsk terraneOH - PR - terranePredivinsk Circum-Siberia Collage Circum-Siberia CollageFragments to become Tuva-Mongolia Superterrane that forms the backstop to the Baikal-Muya arc system Another fragment of Tuva-Mongolia Superterrane Kolyma-Omolon Superterrane Barguzin island arc terrane. 5. N eoproterozoic through Silurian M etallogenesis and Tectonics of N ortheast Asia 5-55 Figure 23.  Early Cambrian (545 Ma) metallogenic and tectonic model for Northeast Asia. Refer to figure 22 for explanation. Figure adapted from Parfenov and others (chapter  9, this volume). 15 -30 -30 JX LA BKBE HT OZ PS CG SK JZ 0 2,000 km1,000 SINO-KOREAN CRATON GOBI - AMUR MICROCONTINEN T KUZNETSK-TANNUOLA ARC D Z H I D A - L A K E A R CTRANSBAIKAL BASIN Paleo-Asian Ocean MINUSA - TUVA BASIN BU JI HX BYBRG ZA KOM KOP OH WST WST ID AR SHE AY MMGN OL SADR HM Baikal Lake AK NAE NAP NAV NAT N O R T H A S I A N C R A T O N SALAIR ARC SAL - UC DZ EROI KU - NRS - KK T T -K O Z -K I-U L-U G KHM - UO - OM - TO MK LK GEOLOGIC UNITS North Asian Craton Margin NAE - East Angara NAP - Patom-Baikal NAT - South-Taimyr NAV - Verkhoyansk ZA - Zavhan terrane (Continental margin arc) (Late Neoproterozoic) BK - Bokson-Kitoiskiy Terranes METALLOGENIC BELTS AK - Avekov terrane AR - Argunsky terrane AY - Ayansk terrane BRG - Barguzin terrane BU - Bureya terrane (Metamorphic) BY - Baydrag terrane DR - Derba terrane DZ - Dzhida terrane (Island arc) ER - Eravna terrane (Island arc) GN - Gonzha terrane HM - Hamar-Davaa terrane HX - Hutaguul-Xilinhot terrane ID - Idermeg terrane JI - Jiamusi terrane KHM - Khamsara terrane (Island arc) KI - Kanim terrane (Island arc) KK - Kizir-Kazir terrane (Island arc) KOM - Kolyma-Omolon superterrane KOP - Prekolyma KOZ - Kozhukhov terrane (Island arc) KU - Kurai terrane (Island arc) LK - Lake terrane (Island arc) MK - Malokhingansk terrane (Accretionary wedge, type B) (Neoproterozoic and Cambrian) MM - Mamyn terrane NRS - North Sayan terrane (Island arc) OH - Okhotsk terrane OI - Orhon-Ikatsky terrane (Continental margin arc) OL - Oldoy terrane OM - Ondum terrane (Island arc) SA - Sangilen terrane SAL - Salair terrane (Island arc) SHE - Shevli terrane TO - Tannuola subterrane (Island arc) TT - Telbes-Kitat terrane (Island-arc) UC - Ulus-Cherga terrane (Island arc) UG - Ulgey terrane (Island arc) UL - Uimen-Lebed terrane (Island arc) UO - Ulugo terrane (Island arc) WST - West Stanovoy terrane BE - Bedobinsk CG - Chagoyan HT - Hunjiang-Taizihe JZ - Jinzhong JX - Jixi LA - Lake P - Prisayanskiy OZ - Ozerninsky SK - South Khingan S Altai Collage Yenisey-Transbaikal Collage Accreted Circum-Siberia Collage and Tuva-Mongolia Microcontinent Argun-Idermeg Superterrane 5-56 Metallogenesis and Tectonics of Northeast Asia (TT), Uimen-Lebed (UL), North Sayan (NRS), Khamsara (KHM), Ulugo (UO), Ondum (OM), and Tannuola (TO) ter- ranes (figs. 2, 23; appendix B). Oceanward of, and parallel to the Kuznetsk-Tannuola island arc were tectonically linked accretionary-wedge terranes, including the Teletsk (TL), Dzhebash (DZE), Amil (AI), Borus (BS), and Kurtushiba (KRT) terranes that consist of Late Neoproterozoic and Early Cambrian oceanic crustal rock, upper mantle rock, and turbi- dite deposits. Blueschist facies assemblages occur in the Borus and Kurtushiba terranes. During the Vendian and Early and Middle Cambrian, mainly sedimentary rocks were deposited in the Minusa-Tuva basin that separated the island arc from the North Asia cratonal margin. Salair Island Arc Remnants of the Salair island arc are preserved in the Altai collage (figs. 2, 23; appendix B) in the Salair (SAL) and Ulus-Cherga (UC) island-arc terranes that are tectonically linked to the Alambai (AL) and Baratal (BR) accretionary- wedge terranes. The Salair arc is the western-most extent of the Late Neoproterozoic and Cambrian island-arc system.And as with the eastern segments of the Late Neoproterozoic and Cambrian island-arc systems that occurred south of the North Asian craton and margin, the major igneous activity in the Salair arc occurred in the Early Cambrian. Origin of Late Neoproterozoic (Vendian) and  Early Cambrian Island Arcs The late Neoproterozoic and Early Cambrian island-arc units are interpreted by most workers as having formed from subduction of the Paleo-Asian oceanic plate (Al’mukhamedov and others, 1996; Belichenko and others, 1994; Berzin and Dobretsov, 1994; Gordienko, 1987; Dergunov, 1989; Didenko and others, 1994; Mossakovskiy and others, 1994; Pecherskiy and Didenko, 1995; Sengör and Natal’in 1996; Zonenshain and others, 1990). The island arcs commenced activity after the formation of the late Neoproterozoic accretional-collisional belt along the continent and after the migration of the subduction zone towards the Paleo-Asian Ocean. The underthrusting of oce- anic plate occurred northward (present-day coordinates), toward the Siberian continent, as indicated confirmed by the spatial arrangement of island-arc, accretionary and turbidite terranes. At this time, blique subduction (a combination strike-slip and under- thrusting) was already occurring in this area (Berzin, 1995). Associated with magmatic arcs are the Minusa-Tuva and Transbaikal back-arc basins that were separated by island arcs and fragments of oceanic plates. During the Vendian and Early Cambrian, dominantly carbonate-terrigenous rocks closely associated with underlying sediments were deposited. Coeval sediments unconformably overlapped the Neoproterozoic terrane collage along the periphery of the North Asian craton. These units are preserved in the Mana (ma), Huvsgol-Bokson (hb), Upper Angara (ua), Gazimur (ga), and Argun (ags) overlap units. The formation of the island arcs is interpreted as having ended in the early Middle Cambrian when oblique subduction changed into dextral-slip faulting along the outboard (ocean- ward) margin of arcs (Berzin, 1995). Metallogenesis The major Late Neoproterozoic through Early Cambian metallogenic belts formed in a variety of tectonic environ- ments (figs. 13, 23, 24; appendix C). Some of the belts contin- ued to form throughout the Cambrian (fig. 24). The Bedobinsk belt (BE, figs. 13, 23; appendix C) is hosted in the North Asian craton, contains sediment-hosted Cu deposits, and is interpreted as having formed in an inland-sea basin during post-saline stage of rock deposition. The main source of copper was weathered Riphean rocks as well as lode deposits in the Yenisei Ridge, and from hydrothermal activity along deep-fault zones related to rifting. The Chagoyan belt (CG, figs. 13, 23, 24; appendix C) contains sedimentary exhalative Pb-Zn (SEDEX) deposits that are hosted in metasedimentary units in Bureya metamorphic terrane that is interpreted as part of the Gobi-Amur microcon- tinent. The belt is interpreted as having formed during rifting and submarine hydrothermal activity that included intrusion of intermediate composition dikes, and during chemical marine sedimentation along the continental margin of the Gobi-Amur microcontinent. The Hunjiang-Taizihe belt (HT, figs. 13, 23, 24; appendix C) contains evaporite sedimentary gypsum deposits and is hosted in platform sedimentary cover on Sino-Korean craton. The belt is interpreted as having formed in a super-tidal sab- kha sedimentary environment. The Jixi belt (JX, figs. 13, 23, 24; appendix C), that started in the Neoproterozoic, continued to form. This belt contains banded iron formation (BIF, Algoma Fe), Home- stake Au, metamorphic graphite, and metamorphic sillimanite deposits that are hosted in the Jiamusi metamorphic terrane and Zhangguangcailing (Continental margin arc) superterrane that is part of Gobi-Amur microcontinent. The belt is part of a khondalite that is interpreted as having been derived from Al-rich mudstone and carbonates of the Mashan and the Xing- dong groups that were deposited in a shallow sea and isolated oceanic basin and lagoon. The Lake belt (LA, figs. 13, 23; appendix C) contains volcanogenic Cu-Zn massive sulfide (Urals type), volca- nogenic-sedimentary Fe; podiform Cr; mafic-ultramafic related Ti-Fe (+V); Cu (±Fe, Au, Ag, Mo) skarn, Fe skarn, granitoid-related Au vein, Cyprus Cu-Zn massive sulfide, and mafic-ultramafic related Cu-Ni-PGE deposits. The magmatic deposits are interpreted as having formed in the Dzhida-Lake island arc. The sediment-hosted deposits are interpreted as having formed during sea floor spreading volcanism and related mafic-ultramafic magmatism. The Prisayanskiy belt (PR, figs. 3, 23; appendix C) contains REE (±Ta, Nb, Fe) carbonatite and mafic-ultramafic 5. N eoproterozoic through Silurian M etallogenesis and Tectonics of N ortheast Asia 5-57Figure 24.  Late Cambrian (520 to 500 Ma) metallogenic and tectonic model for Northeast Asia. Figure adapted from Parfenov and others (chapter 9, this volume). 15 +15 = = +15 HT JZ BE BK GA JX CG SK VZ, YA US GOBI - AMUR MICROCONTINEN T BU JI HX MK SINO-KOREAN CRATON SALAIR ARC 0 2,000 km1,000 PALEO - ASIAN OCEAN NRS WSY TO SA AT BM HM DZ BM ER BRG HV WST KOM KOP OH BY ZA LK AR ID AK NAE NAP NAV NAT SHE AY Baikal Lake N O R T H A S I A N C R A T O N CHR ACH tn tn tn VS tl MO MO GA MO GEOLOGIC UNITS North Asian Craton Margin NAE - East Angara NAP - Patom-Baikal NAT - South-Taimyr NAV - Verkhoyansk tl Telmen plutonic belt (Middle Cambrian through Early Ordovician) tn Tannuola plutonic belt (Cambrian and Ordovician) Terranes Overlap Continenta-Margin Arcs and Granite Belts METALLOGENIC BELTS ACH - Anui-Chuya terrane (Continental margin turbidite) AK - Avekov terrane AR - Argunsky terrane AT - Altai terrane (Continental margin turbidite) (Precambrian and Cambrian through Devonian) AY - Ayansk terrane BM - Baikal-Muya terrane (Island arc) (Neoproterozoic) BRG - Barguzin terrane BU - Bureya terrane (Metamorphic) BY - Baydrag terrane CHR - Charysh terrane (Continental margin turbidite) (Cambrian through Devonian) DZ - Dzhida terrane (Island arc) ER - Eravna terrane (Island arc) GA - Govi Altai terrane (Continental-margin turbidite) (Cambrian through Devonian) HM - Hamar-Davaa terrane HV - Hovd terrane (Continental-margin turbidite) (Neoproterozoic through Silurian) HX - Hutaguul-Xilinhot terrane ID - Idermeg terrane JI - Jiamusi terrane KOM - Kolyma-Omolon superterrane KOP - Prekolyma LK - Lake terrane (Island arc) MK - Malokhingansk terrane (Accretionary wedge, type B) (Neoproterozoic and Cambrian) MO - Mandalovoo-Onor terrane (Island arc) (Middle Ordovician through Early Carboniferous) NRS - North Sayan terrane (Island arc) OH - Okhotsk terrane SA - Sangilen terrane SHE - Shevli terrane TO - Tannuola subterrane (Island arc) VS - Voznesenka terrane (Passive continentalal margin) (Cambrian through Permian) WST - West Stanovoy terrane WSY - West Sayan terrane (Continental margin turbidite) (Late Neoproterozoic through Devonian) ZA - Zavhan terrane (Continental margin arc) (Late Neoproterozoic) BE - Bedobinsk BK - Bokson-Kitoiskiy CG Chagoyan GA - Govi-Altai HT - Hunjiang-Taizihe JX - Jixi JZ - Jinzhong SK - South Khingan US - Uda-Shantar VZ - Voznesenka YA - Yaroslavka - - Altai Collage with Salair Arc Accreted Yenisey-Transbaikal Collage Argun-Idermeg Superterrane 5-60 Metallogenesis and Tectonics of Northeast Asia the Siberian Continent margin and during subsequent transpression-dextral-slip faulting. 5. The Hunjiang-Taizihe belt (HT, figs. 13, 25; appendix C) with evaporite sedimentary gypsum deposits contin- ued forming from the previous time span. 6. The Jinzhong belt (JZ, figs. 13, 25; appendix C) with evaporite sedimentary gypsum deposits continued form- ing from the previous time span. 7. The Kiyalykh-Uzen belt (KK, figs. 13, 24; appendix C) contains Cu (±Fe, Au, Ag, Mo) skarn, W±Mo±Be skarn, Fe skarn, and W-Mo-Be greisen, stockwork, and quartz- vein deposits. The belt is interpreted as having formed during oblique accretion and collision of Kuznetsk- Tannuola and Dzhida-Lake island arcs onto the Siberian Continent margin and during subsequent transpression- dextral-slip faulting along the Kuznetsk Alatau fault. This major orogenic event resulted in intrusion of Telmen plutonic belt that hosts the dposits. 8. The Kizir-Kazyr belt (KK, figs. 13, 25; appendix C) con- tains Fe skarn, volcanogenic-sedimentary Fe, and granit- oid-related Au-vein deposits and is hosted in the Tannuola plutonic belt, part of the Yenisey-Transbaikal collage. The belt is interpreted as having formed during oblique accre- tion and collision of Kuznetsk-Tannuola and Dzhida-Lake island arcs onto the southern North Asian cratonal margin and during subsequent transpression-dextral-slip faulting. The sediment-hosted deposits are interpreted as being part of the Kizir-Kazir island-arc terrane, part of the Yenisey- Transbaikal collage. 9. The Martaiginsk belt (MT, figs. 13, 25; appendix C) with granitoid-related Au vein and Fe skarn deposits is hosted in the Tannuola plutonic belt, part of the Yenisey-Trans- baikal collage. The belt is interpreted as having formed during oblique accretion and collision of Kuznetsk- Tannuola and Dzhida-Lake island arcs onto the southern North Asian cratonal margin and during subsequent transpression-dextral-slip faulting. The sediment-hosted deposits are interpreted as part of the Kizir-Kazir island- arc terrane, part of the Yenisey-Transbaikal collage. 10. The Yaroslavka belt (YA, figs. 13, 24, 25, 26; appendix C) contains fluorite greisen and Sn-W greisen, stock- work, and quartz-vein deposits that are hosted in Paleo- zoic granitoid plutons that intrude in Cambrian clastic and limestone units of the Vosensenka continental-margin terrane of the Khanka superterrane. The belt is inter- preted as having formed in a collisional arc that formed along the passive continental margin of a fragment of Gondwanaland. 5. Neoproterozoic through Silurian Metallogenesis and Tectonics of Northeast Asia 5-61 Figure 25.  Early to Middle Ordovician (500 to 450 Ma) metallogenic and tectonic model for Northeast Asia. Refer to figure 22 for  explanation. Figure adapted from Parfenov and others (chapter 9, this volume). +20 +3(?) +15(?) +20(?)MT BK BH HT EL JZ AG OH VZ, YA KY KK SOUTH MONGOL AI - KHIN GAN AR C SAL NAEROK-ONIS NOTARC mk 000,20 1,000 NRS WSY TO SA BY DN ND OZ ZN HE MO WDZA ER HM DZ BM AT BRG HV LK KOM OH WST GA ID AR MM NAE NAP NAV NAT Baikal Lake IS PR KUV SHE AY GOBI - AMUR MICROCONTINENT BU JI HX tn tn tn tl CHR ACH A R C N A I S A H T R O N N OT TG kbu zg kbu Amandykan Arc LA GEOLOGIC UNITS North Asian Craton Margin NAE - East Angara NAP - Patom-Baikal NAT - South-Taimyr NAV - Verkhoyansk ACH - Anui-Chuya terrane (Continental margin turbidite) AT - Altai terrane (Continental margin turbidite) (Precambrian and Cambrian through Devonian) BM - Baikal-Muya terrane (Island arc) (Neoproterozoic) CHR - Charysh terrane (Continental margin turbidite) (Cambrian through Devonian) DN Dongwuzhumuqin-Nuhetdavaa terrane (Island arc) (Cambrian through Middle Devonian) GA - Govi Altai terrane (Continental-margin turbidite) (Cambrian through Devonian) HV - Hovd terrane (Continental-margin turbidite) (Neoproterozoic through Silurian) MO - Mandalovoo-Onor terrane (Island arc) (Middle Ordovician through Early Carboniferous) ND Nora-Sukhotin-Duobaoshan terrane (Island arc) (Neoproterozoic through Early Carboniferous) WSY - West Sayan terrane (Continental margin turbidite) (Late Neoproterozoic through Devonian) ZA - Zavhan terrane (Continental margin arc) (Late Neoproterozoic) ZN Zhangguangcailing superterrane (Continental margin arc) (Neoproterozoic through Devonian) kbu Khanka-Bureya granitic belt (Ordovician and Silurian) tl Telmen plutonic belt (Middle Cambrian through Early Ordovician) tn Tannuola plutonic belt (Cambrian and Ordovician) zg Zhangguangcailing plutonic belt (Silurian through Ordovician) BK - Bokson-Kitoiskiy - Kizir-Kazyr VZ - Voznesenka YA - Yaroslavka Terranes Overlap Continental Margin Arcs and Granite Belts METALLOGENIC BELTS AR - Argunsky terrane AY - Ayansk terrane BRG - Barguzin terrane BU - Bureya terrane (Metamorphic) BY - Baydrag terrane DZ - Dzhida terrane (Island arc) ER - Eravna terrane (Island arc) Heilongjiang terrane (Accretionary wedge, type B) (Ordovician and Silurian) HM - Hamar-Davaa terrane HX - Hutaguul-Xilinhot terrane ID - Idermeg terrane Isakov terrane (Island arc) (Neoproterozoic) JI - Jiamusi terrane KOM - Kolyma-Omolon superterrane Kuvai terrane (Accretionary wedge, type A) (Neoproterozoic) Laoling terrane (Island arc) (Late Ordovician through Silurian) LK - Lake terrane (Island arc) MM - Mamyn terrane NRS - North Sayan terrane (Island arc) OH - Okhotsk terrane OZ Orogen-Zalantun terrane (Metamorphic) (Proterozoic) PR - Predivinsk terrane (Island arc) (Late Neoproterozoic) SA - Sangilen terrane SAL - Salair terrane (Island arc) SHE - Shevli terrane TG Tsagaan Uul-Guoershan Terrane (Continental margin arc) (Paleoproterozoic through Permian) TO - Tannuola subterrane (Island arc) WD Wundurmiao terrane (Accretionary wedge, type B) (Mesoproterozoic through Middle Ordovician) WST - West Stanovoy terrane BH - Bayanhongor EL - East Liaoning GA - Govi Altai HO - Hovd HT Hunjiang-Taizihe JZ Jinzhong KY - Kiyalykh-Uzen MT- Martaiginsk - - - - - - - KK HE - IS - KUV - LA - - - - Argun-Idermeg Superterrane Accreted Yenisey-Transbaikal Collage Altai Collage with Salair Arc South Mongolia- Khingan Collage Zhangguangcailing superterrane - Continental-margin arc 5-62 Metallogenesis and Tectonics of Northeast Asia Figure 26.  Late Silurian (420 to 410 Ma) metallogenic and tectonic model for Northeast Asia. Refer to figure 22 for explanation.  Figure adapted from Parfenov and others (chapter 9, this volume) +30 +30 YA HO EL GEOLOGIC UNITS North Asian Craton Margin NAE - East Angara NAP - Patom-Baikal NAT - South-Taimyr NAV - Verkhoyansk ACH - Anui-Chuya terrane (Continental margin turbidite) AR - Argunsky terrane AT - Altai terrane (Continental margin turbidite) (Precambrian and Cambrian through Devonian) AY - Ayansk terrane BM - Baikal-Muya terrane (Island arc) (Neoproterozoic) BRG - Barguzin terrane BU - Bureya terrane (Metamorphic) BY - Baydrag terrane CHR - Charysh terrane (Continental margin turbidite) (Cambrian through Devonian) DN - Dongwuzhumuqin-Nuhetdavaa terrane (Island arc) (Cambrian through Middle Devonian) DZ - Dzhida terrane (Island arc) ER - Eravna terrane (Island arc) GA - Govi Altai terrane (Continental-margin turbidite) (Cambrian through Devonian) GN - Gonzha terrane (Passive continental margin) (Late Archean(?), Paleoproterozoic(?), and early Paleozoic) HM - Hamar-Davaa terrane HV - Hovd terrane (Continental-margin turbidite) (Neoproterozoic through Silurian) HX - Hutaguul-Xilinhot terrane ID - Idermeg terrane IS - Isakov terrane (Island arc) (Neoproterozoic) JI - Jiamusi terrane KHM - Khamsara terrane (Island arc) (Cambrian) KOM - Kolyma-Omolon superterrane LA - Laoling terrane (Island arc) (Late Ordovician through Silurian) LK - Lake terrane (Island arc) MM - Mamyn terrane MO - Mandalovoo-Onor terrane (Island arc) (Middle Ordovician through Early Carboniferous) MT - Matveevka terrane (Metamorphic) ND - Nora-Sukhotin-Duobaoshan terrane (Island arc) (Neoproterozoic through Early Carboniferous) NK - Nakhimovka terrane (Metamorphic) NRS - North Sayan terrane (Island arc) OH - Okhotsk terrane OZ - Orogen-Zalantun terrane (Metamorphic) (Proterozoic) PR - Predivinsk terrane (Island arc) (Late Neoproterozoic) SA - Sangilen terrane SAL - Salair terrane (Island arc) SHE - Shevli terrane TG - Tsagaan Uul-Guoershan Terrane (Continental- margin arc) (Paleoproterozoic through Permian) TO - Tannuola subterrane (Island arc) WD - Wundurmiao terrane (Accretionary wedge, type B) (Mesoproterozoic through Middle Ordovician) WST - West Stanovoy terrane WSY - West Sayan terrane (Continental-margin turbidite) (Late Neoproterozoic through Devonian) ZA - Zavhan terrane (Continental-margin arc) (Late Neoproterozoic) at - Altai volcanic-plutonic belt (Devonian and Early Carboniferous) kbu - Khanka-Bureya granitic belt (Ordovician and Silurian) ks - Kuznetsk-Sayan plutonic belt (Early Silurian to Early Devonian) ss - South Siberian volcanic-plutonic belt (Early Devonian) zg - Zhangguangcailing plutonic belt (Silurian through Ordovician) YA - Yaroslavka Terranes Overlap Continental-Margin Arcs and Granite Belts METALLOGENIC BELTS EL - East Liaoning HO - Hovd mk 000,20 1,000 NRS WSY TO KHM SA BY ZA ER HM DZ ER DN ND MO ? 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