Mineral DepositResearch:Meeting theGlobal ChallengeProceedings of the Eighth Biennial SGA MeetingBeijing, China, 18–21 August 2005

Jingwen MaoFrank P. Bierlein(Eds.)

With 791 Figures

Editors

Professor Dr. Jingwen Mao

Chinese Academy of Geological SciencesInstitute of Mineral Resources26 Baiwanzhuang RoadBeijing 100037China

Dr. Frank P. Bierlein

University of Western AustraliaSchool of Earth and Geographical SciencesTectonics Special Research Centre35 Stirling HighwayCrawley WA 6009Australia

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Abstract. The regional characteristics of ore deposit distribution inthe Northeast Asia are obtained via examination of the mineral re-sources database prepared by the international project on the Min-eral Resources, Metallogenesis, and Tectonics of Northeast Asia. Thespatial distribution of the mineral deposits indicates the differencesbetween the eastern and the western sub-regions, suggesting dis-tinct geological development of these regions. The temporal varia-tion of the development of metallogenic belts indicates intenseore-forming events occurred in the Cenomanian-Campanian time.The importance of the regional geological and mineral resourcesinformation can be evaluated by examining the project data andinterpretations.

Keywords. Northeast Asia, mineral resources, database, metallogenicbelts

1 Introduction

Examination of regional distribution characteristics ofore deposits in a given region is useful for area selectionfor further exploration. The regional characteristics ofore deposit distribution in Northeast Asia are obtainedwith examination of the mineral resources database pre-pared by the international project on Mineral Resources,Metallogenesis, and Tectonics of Northeast Asia(Nokleberg et al. 2003). The project recently presentedvarious digital geoscience data for the Northeast Asia. Theproject area consists of Eastern and Southern Siberia,Mongolia, Northern China, South Korea, Japan, and ad-

jacent offshore areas. This area is approximately boundedby 30 to 82° N. latitude and 75 to 144° E. longitude. Themineral resources database is one of the major publica-tions resulting from this project. In this paper, we exam-ine the regional distribution pattern of mineral depositsand temporal variation of numbers of metallogenic beltsin the Northeast Asia, using data compiled by the project.Northeast Asia contains several stable cratons, Paleozoicand Mesozoic orogenic zones, and Mesozoic to CenozoicCircum Pacific orogenic zones. The regional distributionpattern of the ore deposits is examined according to thesegeodynamic settings.

2 Characteristics of ore deposit distribution innortheast Asia

Ariunbileg et al. (2003) provided a mineral resources da-tabase with various computer formats. The lode depositdatabase that was used for this examination contains de-scriptions for 1674 deposits. Although the deposits wereselected from large data set for each region, both majorand significant deposits were included in the databaseand the database is representative for showing the regionaldistribution of ore deposits for the Northeast Asia. Fig-ure 1 shows the location of these deposits in NortheastAsia. It is apparent that the deposits are clustered in spe-cific zones probably related to geodynamic environments.

10-7Chapter 10-7

Characteristics of ore deposit distribution in Northeast Asia,as derived from data compiled by the “Mineral Resources,Metallogenesis, and Tectonics of Northeast Asia” projectOgasawara MasatsuguInstitute of Geology and Geoinformation, Geological Survey of Japan/AIST, Tsukuba, 305-8567, Japan

Sergey RodionovInstitute of Tectonics and Geophysics, Russian Academy of Sciences, Khabarovsk, Russia

Warren J. NoklebergU.S. Geological Survey, Menlo Park, California, USA

Alexander A. ObolenskiyInstitute of Geology, Russian Academy of Sciences, Novosibirsk, Russia

Alexander I. KhanchukFar East Geological Institute, Russia Academy of Sciences, Vladivostok, Russia

Gunchin DejidmaaGeologic Information Center, Mineral Resources Authority of Mongolia

Yan HongquanGeological Research Institute, Jilin University, China

Duk-Hwan HwangKorea Institute of Geosciences and Mineral Resources, Taejon, Korea

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The numbers of deposits occur within 4 degree lati-tude are obtained from the mineral database, and plottedagainst the latitude (Fig. 2) that illustrates north-southvariation of numbers of deposits. The maximum numberof deposits occur at around 48° N. To the north of thispoint, the number of deposit decreases steeply. The north-ern area is covered by stable platform sediments, and thesmall number of the deposits could be the result of ex-tensive sedimentary cover.

The difference in mineral deposit distribution betweenthe eastern and western parts of the project area has beenexamined by grouping of the data for three sub-regions,western, central, and eastern regions. Those are boundedby 100 and 122° E (Fig. 1). Each region has an east-westwidth of 22 degrees. Numbers of deposits in the western,central, and eastern regions are 571, 491, and 612, respec-tively. Thus, each region contains almost the same numberof ore deposits. However, the southern part of the westernregion is limited to between 40° and 52° N, and the actualsizes of the regions are different. The number of depositsin the central and western region normalized to the size ofeastern region can be calculated, and are 614 and 1243, re-spectively. The figures indicate high concentration of de-posits in the western region. Further more, the populationof deposits obtained for every 10,000 km2 in the eastern,central, and western regions are 0.82, 0.84, and 1.68, respec-tively. As the eastern region contains a large area coveredby ocean, the actual population of deposits should be higher.In the case of the Japanese islands, 4.8 deposits per 10,000 km2 are listed on the Northeast Asia database; this figure ismuch higher than for the western region.

The north-south difference of numbers of deposits foreach sub-region is also shown on the Figure 2. The westernregion has a maximum number of deposits at around 48°N, similar to the trend to all of Northeast Asia. However,the number steeply decreases to the south. The central re-gion shows two peaks at around 48 and 40° N, and a smallernumber of deposits occurs in the northern part of the re-gion where an extensive stable platform cover occurs. Largenumbers of deposits in the western and central regionsformed in the Paleozoic and early Mesozoic. Maximum dis-tribution of deposits around 50° N for the western and cen-tral region is explained by presence of Paleozoic and earlyMesozoic orogenic zones of the area. The southern part ofthe eastern region (south of 44° N) contains large numbersof deposits, but a large number of deposits also occurs inthe northern part of the region, indicating the influence ofthe north-south belt of Circum Pacific orogeny along theeastern margin of the Asian continent. The southern partof the eastern region contains young island arcs, which mayexplain the high concentration of deposits. As the large num-bers of deposits were compiled for the Northeast Asia da-tabase, plotting of the data clearly shows regions which ex-perienced intense ore-forming events.

Deposits with Au as major commodity were selectedfrom the database. 331 deposits in the database list Au asmajor commodity. The data are also plotted on Figure 3.The Au deposit distribution pattern indicates large num-bers of deposits occur between 36° N and 60° N, with twopeaks at 40° N and 48° N. In the western region the maxi-mum number of the Au deposits occur at around 52° N.The central region has a small peak at around 52° N, sug-gesting a continuation of the peak from the west. How-ever, an additional higher peak occurs at around 40° Nfor central region. The eastern region has two peaks onthe diagram, similar to the overall distribution pattern

O. Masatsugu · S. Rodionov · W.J. Nokleberg · A.A. Obolenskiy · A.I. Khanchuk · G. Dejidmaa · Y. Hongquan · D.-H. Hwang

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for Northeast Asia. The characteristics of Au deposits dis-tribution can be understood by the regional tectonic his-tory of the Northeast Asia as described as above.

3 Metallogenic belts of northeast Asia

The temporal variation of ore forming events is examinedusing the metallogenic belt data of Northeast Asia that werecompiled by Rodionov et al. (2004). Although the estimatedformation age of the deposits is listed in the mineral re-sources database, not all deposits have age data. Thus, theonly metallogenic belts data which include timing of themetallogenic events were used. The metallogenic belts arecharacterized by a narrow age of formation and are de-fined with information from ore-forming events, tectonics,terranes and overlap assemblages, and mineral depositmodels. The metallogenic belts were defined for 12 timeslices (Rodionov, et al, 2004). The number of metallogenicbelts for each time slices is summarized and plotted againsttime on Figure 4. It shows the variation of numbers ofmetallogenic belts in the Northeast Asia through geologi-cal time. As the time stages have different duration, the num-bers of metallogenic belts normalized for the duration arealso presented on Figure 4. This figure shows two majortime stages of the metallogenic belts, Cambrian-Early Car-boniferous and Cretaceous (Cenomanian-Campanian). TheCretaceous interval hosts the maximum number ofmetallogenic belts that occur mainly along the eastern mar-gin of the Asian continent. The number of metallogenicbelts peaks during the Middle Jurassic-Early Cretaceousinterval. However, the Cenomanian-Campanisan intervalshows a higher normalized metallogenic belts number, sug-gesting more intense metallogenic events at this time. Thosebelts formed during subduction of the Pacific ocean plateunder the Asian continent. The timing of development of

metallogenic belts clearly shows a link of metallogeny tothe geodynamic settings.

4 Conclusions

The regional characteristics of ore deposit distribution inthe Northeast Asia are obtained via examination of the min-eral resources database prepared by the international projecton Mineral Resources, Metallogenesis, and Tectonics of North-east Asia. The spatial distribution of the mineral depositshighlight the difference between the eastern and the west-ern sub-region, suggesting distinct geological developmentof these regions. The temporal variation of the developmentof metallogenic belts are analyzed. The results indicate tim-ing of major ore forming events in the Northeast Asia. Thetectonic environments for the ore forming events are con-sidered. The importance of the regional geological and min-eral resources information can be indicated with the pre-liminary evaluation of the data presented by the project.

Chapter 10-7 · Characteristics of ore deposit distribution in Northeast Asia

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Acknowledgements

Project members of the international project on MineralResources, Metallogenesis, and Tectonics of Northeast Asiaare thanked for valuable discussion for this work.

References

Ariunbileg, Sodov, Biryul’kin, G.V., Byamba, Jamba, Davydov, Y.V.,Dejidmaa, Gunchin, Distanov, E.G., Dorjgotov, Gamyanin, G.N.,Gerel, Ochir, Fridovskiy, V.Yu., Gotovsuren, Ayurzana, Hwang, DukHwan, Kochnev, A.P., Kostin, A.V., Kuzmin, M.I., Letunov, S.A., Li,Jiliang, Li, Xujun, Malceva, G.D., Melnikov, V.D., Nikitin, V.M.,Obolenskiy, A.A., Ogasawara, Masatsugu, Orolmaa, Demberel,Parfenov, L.M., Popov, N.V., Prokopiev, A.V., Ratkin, V.V., Rodionov,S.M., Seminskiy, Z.V., Shpikerman, V.I., Smelov, A.P., Sotnikov, V.I.,Spiridonov, A.V., Stogniy, V.V., Sudo, Sadahisa, Sun, Fengyue, Sun,

Jiapeng, Sun, Weizhi,. Supletsov, V.M., Timofeev, V.F., Tyan, O.A.,Vetluzhskikh, V.G., Xi, Aihua, Yakovlev, Y.V., Yan, Hongquan,Zhizhin, V.I., Zinchuk, N.N., and Zorina, L.M., (2003) Significantmetalliferous and selected non-metalliferous lode deposits, andselected placer districts of Northeast Asia, by U.S. GeologicalSurvey Open-File Report 03-220 (CD-ROM), 422 p

Nokleberg, W.J., Miller, R.J., Naumova, V.V., Khanchuk, A.I., Parfenov,L.M., Kuzmin, M.I., Bounaeva, T.M., Obolenskiy, A.A., Rodionov,S.M., Seminskiy, Z.V., and Diggles, M.F.(2003) Preliminary Publi-cations Book 2 from Project on Mineral Resources, Metallogenesis,and Tectonics of Northeast Asia: U.S. Geological Survey Open-FileReport 03-203 (CD-ROM)

Rodionov, S.M., Obolenskiy, A.A., Dejidmaa, G., Gerel, O., Hwang,D.H., Miller, R.J., Nokleberg, W.J., Ogasawara, M., Smelov, A.P.,Yan, H., and Seminskiy, Z.V. (2004) Descriptions of metallogenicbelts, methodology, and definitions for Northeast Asia mineraldeposit location and metallogenic belt maps. U.S.G.S. Open-FileReport 2004-1252 (CD-ROM), explanatory text, 442 p

O. Masatsugu · S. Rodionov · W.J. Nokleberg · A.A. Obolenskiy · A.I. Khanchuk · G. Dejidmaa · Y. Hongquan · D.-H. Hwang

Abstract. These studies are part of a major international collabora-tive study of the ‘Mineral Resources, Metallogenesis, and Tectonicsof Northeast Asia’ that was conducted from 1997 through 2004 bygeologists from earth science agencies and universities in Russia,Mongolia, Northeastern China, South Korea, Japan, and the USA.The metallogenic analyses included several steps: metallogenic belts,mineral deposit models, relation between metallogenesis, tecton-ics, and geodynamic. Major results of the project are available byInternet at the following web site: http://minerals.usgs.gov/west/projects/minres.html

Keywords. Metallogenesis, North-East Asia, mineral deposit

1 Metallogenic belts of NE Asia

The metallogenic belts of Northeast Asia are herein syn-thesized, compiled, described, and interpreted with theuse of modern concepts of plate tectonics, analysis of ter-ranes and overlap assemblages, and synthesis of mineraldeposit models. The data supporting the compilation are:(1) comprehensive descriptions of mineral deposits; (2)compilation and synthesis of a regional geodynamics mapthe region at 5 million scale with detailed explanationsand cited references; and (3) compilation and synthesisof metallogenic belt maps at 10 million scale with de-tailed explanations and cited references.

Metallogenic belts are characterized by a narrow ageof formation, and include districts, deposits, and occur-rences. The metallogenic belts are synthesized and de-scribed for the main structural units of the North AsianCraton and Sino-Korean Craton, framing orogenic beltsthat consist of collage of accreted tectonostratigraphicterranes, younger overlap volcanic and sedimentary rocksequences, and younger stitching plutonic sequences. Themajor units in the region are the North Asian Craton, ex-terior passive continental margin units (Baikal-Patom,Enisey Ridge, Southern Taymir, and Verkhoyansk passivecontinental margin units), the early Paleozoic CentralAsian orogenic belt, and various Mesozoic and Cenozoiccontinental margin arcs. Metallogenic belts are interpretedaccording to specific geodynamic environments includ-ing cratonal, active and passive continental margin, con-tinental-margin arc, island arc, oceanic or continental rift,collisional, transform-continental margin, and impact.

The following concepts are employed for the synthe-sis of metallogenic belts.

� Mineral Deposit Association. Each metallogenic beltincludes a single mineral deposit type or a group ofcoeval, closely-located and genetically-related mineraldeposits types.

� Geodynamic Event for Deposit Formation. Eachmetallogenic belt contains a group of coeval and ge-netically related deposits that were formed in a spe-cific geodynamic event. Examples are collision, conti-nental-margin arc, accretion, rifting and others.

� Favorable Geological Environment. Each metallogenicbelt is underlain by a geological host rock and (or)structure that is favorable for a particular suite of min-eral deposit types.

� Tectonic or Geological Boundaries. Each metallogenicbelt is usually bounded by favorable either strati-graphic or magmatic units, or by major faults (sutures)along which substantial translations have occurred.

� Relation of Features of Metallogenic Belt to Host Unit.The name, boundaries, and inner composition of eachmetallogenic belt corresponds to previously definecharacteristics of rocks or structures hosting the de-posits, and to a suite of characteristics for the group ofdeposits and host rocks.

With these definitions and principles, the area definedfor a metallogenic belt is predictive or prognostic for un-discovered deposits. Consequently, the synthesis and com-pilation of metallogenic belts is a powerful tool for min-eral exploration, land-use planning, and environmentalstudies.

For modern metallogenic analysis, three interrelatedproblems exist.

1. What is the relation of geodynamics to regional or glo-bal metallogeny? As discussed by Zonenshain and oth-ers (1992) and Dobretsov and Kirdyashkin (1994), thisproblem includes the role of convective processes inmantle and mantle plumes, the global processes of for-mation of the continents and oceans, the dynamics ofdevelopment of major tectonic units of the earth’s crust,

10-9Chapter 10-9

Metallogenesis of northeast AsiaS.M. Rodionov1, A.A. Obolenskiy2, G. Badarch3, G. Dejidmaa4, E.G. Distanov2, O. Gerel5, D.H. Hwang6, W.J. Nokleberg7, M. Ogasawara8,A.V. Prokopiev10, Zh.V. Seminsky 9, A.P. Smelov10, V.I. Sotnikov2, A.A. Spiridonov11, H. Yan12

1 Russian Academy of Sciences, Khabarovsk; 2 Russian Academy of Sciences, Novosibirsk; 3 Mongolian Academy of Sci-ences, Ulaanbaatar; 4 Mineral Resources Authority of Mongolia, Ulaanbaatar; 5 Mongolian University of Science and Tech-nology, Ulaanbaatar; 6 Korea Institute of Geology, Mining, and Materials, Taejon; 7 U.S. Geological Survey, Menlo Park;8 Geological Survey of Japan/AIST, Tsukuba; 9 Irkutsk State Technical University, Irkutsk; 10 Russian Academy of Sciences,Yakutsk; 11 Russian Academy of Sciences, Irkutsk; 12 Jilin University, Changchun, China

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metallogenic evolution of the earth, and the role mantleprocesses in the origin of major-belts of deposits.

2. What is relation of regional metallogeny to individuallithosphere blocks? As discussed by Guild (1978),Mitchell and Garson (1981), and Koroteev (1996), thisproblem includes the genesis of specific metallogenicbelts as a function of specific geodynamic environ-ments using the modem concepts of plate tectonics.

3. What is the relation of metallogeny to individualtectonostratigraphic terranes and overlap assem-blages? As discussed by Nokleberg and others (1993,1998) and Parfenov and others (1999), this problemincludes the genesis of specific metallogenic belts inindividual fault-bounded units of distinctive stratig-raphy, defined as tectonostratigraphic terranes, and inyounger overlapping assemblages often containing ig-neous rocks formed in continental margin or islandarcs, along rift systems in continents, or along trans-form continental margins.

2 Methodology of metallogenic analysis

The compilation, synthesis, description, and interpreta-tion of metallogenic belts of Northeast Asia is part of aintricate process to analyze the complex metallogenic andtectonic history of the region. The methodology for thistype of analysis consists of the following steps. (1) Themajor lode deposits are described and classified accord-ing to defined mineral deposit models. (2) Metallogenicbelts are delineated. (3) Tectonic environments for thecratons, craton margins, orogenic collages of terranes,overlap assemblages, and contained metallogenic belts areassigned from regional compilation and synthesis of strati-graphic, structural, metamorphic, isotopic, faunal, andprovenance data. The tectonic environments includecratonal, passive continental margin, metamorphosedcontinental margin, continental-margin arc, island arc,transform continental-margin arc, oceanic crust, sea-mount, ophiolite, accretionary wedge, subduction zone,turbidite basin, and metamorphic. (4) Correlations aremade between terranes, fragments of overlap assemblages,and fragments of contained metallogenic belts. (5) Co-eval terranes and their contained metallogenic belts aregrouped into a single metallogenic and tectonic origin,for instance, a single island arc or subduction zone. (6)Igneous-arc and subduction-zone terranes, which are in-terpreted as being tectonically linked, and their containedmetallogenic belts, are grouped into coeval, curvilinear arc-subduction-zone-complexes. (7) By use of geologic, faunal,and paleomagnetic data, the original positions of terranesand their metallogenic belts are interpreted. (8) The pathsof tectonic migration of terranes and contained metallogenicbelts are constructed. (9) The timings and nature of accre-tions of terranes and contained metallogenic belts are de-

termined from geologic, age, and structural data; (10) Thenature of collision-related geologic units and their con-tained metallogenic belts are determined from geologicdata. And (11) the nature and timing of post-accretion-ary overlap assemblages and contained metallogenic beltsare determined from geologic and age data.

According to the main geodynamic events and themajor deposit-forming and metallogenic belt-formingevents for Northeast Asia, the following twelve time spansare used for groupings of metalogenic belts:

� Archean (> 2500 Ma).� Paleoproterozoic (2500 to 1600 Ma).� Mesoproterozoic (1600 to 1000 Ma).� Neoproterozoic (1000 to 540 Ma).� Cambrian through Silurian (540 to 410 Ma).� Devonian through Early Carboniferous (Mississippian)

(410 to 320 Ma).� Late Carboniferous (Pennsylvanian) through Middle

Triassic (320 to 230 Ma).� Late Triassic through Early Jurassic (230 to 175 Ma).� Middle Jurassic through Early Cretaceous (175 to 96

Ma).� Cenomanian through Campanian (96 to 72 Ma).� Maastrichnian through Oligocene (72 to 24 Ma).� Miocene through Quaternary (24 to 0 Ma).

Paleogeodynamic and related metallogenic analyseswere made separately for each time span. The examplefor Cenomanian-Campanian time span is shown below(Fig. 1).

Rodionov · Obolenskiy · Badarch · Dejidmaa · Distanov · Gerel · Hwang · Nokleberg · Ogasawara · Prokopiev · Seminsky · Smelov · Sotnikov · Spiridonov · Yan

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3 Mineral deposit models

For descriptions of metallogenic belts, lode mineral de-posits are classified into various models or types. The fol-lowing three main principles are employed for synthesisof mineral deposit models for this study. (1) Deposit form-ing processes are close related to rock forming processes(Obruchev 1928) and mineral deposits originate as theresult of mineral mass differentiation under their con-stant circulation in sedimentary, magmatic, and metamor-phic circles of formation of rocks and geological struc-tures (Smirnov 1969). (2) The classification must be asmore comfortable and understandable for appropriateuser as possible. And (3) the classification must be openso that new types of the deposits can be added in thefuture (Cox and Singer 1986).

In this classification for this study, lode deposits aregrouped into the hierarchic levels of metallogenic taxonsaccording to such their stable features as: (a) environ-ment of formation of host and genetically-related rocks,(b) genetic features of the deposit, and (c) mineral and(or) elemental composition of the ore. The six hierarchiallevels are as follows:

Group of depositsClass of deposits

Clan of depositsFamily of deposits

Genus of depositsDeposit types (models)

The deposit models are subdivided into the follow-ing four large groups according to major geologicalrock-forming processes: (1) deposits related to magmaticprocesses; (2) deposits related to hydrothermal-sedimen-tary processes; (3) deposits related to metamorphic pro-cesses; (4) deposits related to surficial processes and (6)exotic deposits. Each group includes several classes. Forexample, the group of deposits related to magmaticprocesses includes two classes: (1) those related to in-trusive rocks; and (2) those related to extrusive rocks.Each class includes several clans, and so on. The mostdetailed subdivisions are for magmatic-related depositsbecause they are the most abundant in the project area.In the below classification, lode deposit types modelsthat share a similar origin, such as magnesian and (or)calcic skarns, or porphyry deposits, are grouped togeth-er under a single genus with several types (or species)within the genus.

Some of the below deposit models differ from citeddescriptions. For example, the Bayan Obo type was de-scribed previously as a carbonatite-related deposit. How-ever, modern isotopic, mineralogical, and geological datarecently obtained by Chinese geologists have resulted in

a new interpretation of the deposit origin. These newdata indicate that the deposit consists of ores that formedduring Mesoproterozoic sedimentary-exhalative process,and along with coeval metasomatic activity, sedimen-tary diagenesis of dolomite, and alteration. The sedimen-tary-exhalative process consisted of both sedimentationand metasomatism. Later deformation, especially dur-ing the Caledonian orogeny, further enriched the ore.Consequently, the Bayan Obo deposit type is hereindescribed as related to sedimentary-exhalative process-es, not to magmatic processes. However, magmatic pro-cesses also played an important role in deposit for-mation. Consequently, this deposit model is part of thefamily of polygenetic carbonate-hosted deposits. Simi-lar revisions are made for carbonate-hosted Hg-Sb andother deposit models.

Metalliferous and selected non-metalliferous lode andplacer deposits for Northeast Asia are classified into vari-ous models or types described below. The mineral de-posit types used in this study are based on both descrip-tive and genetic information that is systematically ar-ranged to describe the essential properties of a class ofmineral deposits. Some types are descriptive (empirical),in which instance the various attributes are recognizedas essential, even though their relationships are unknown.An example of a descriptive mineral deposit type is thebasaltic Cu type in which the empirical datum of a geo-logic association of Cu sulfide minerals with relativelyCu-rich metabasalt or greenstone is the essential attribute.Other types are genetic (theoretical), in which case theattributes are related through some fundamental concept.An example is the W skarn deposit type in which casethe genetic process of contact metasomatism is the ge-netic attribute.

References

Cox DP, Singer DA (eds) (1986) Mineral deposit models: U.S. Geo-logical Survey Bulletin, 379

Dobretsov NL, Kirdyashkin AG (1994) Deep level geodynamics: Si-berian Branch, Russian Academy of Sciences Press, Novosibirsk,455 (in Russian)

Guild PW (1978) Metallogenic maps; principles and progress: Glo-bal Tectonics Metallogeny 1: 10-15

Koroteev VA (ed) (1996) Metallogeny of fold system with respect toplate tectonics: Urals Branch, Russian Academy of Sciences Press,Ekaterinburg, 228 (in Russian)

Mitchell AG, Garson MS (1981) Mineral deposits and global tectonicsettings: Academic Press, London, 421

Nokleberg WJ, Bundtzen TK, Grybeck D, Koch RD, Eremin, RA,Rozenblum IS, Sidorov AA, Byalobzhesky SG, Sosunov GM,Shpikennan VI, Gorodinsky ME (1993) Metallogenesis of main-land Alaska and the Russian Northeast: Mineral deposit maps,models, and tables, metallogenic belt maps and interpretation,and references cited: U.S. Geological Survey Open-File Report93-339, 222 pages, 1 map, scale 1:4, 000,000, 5 maps, scale1:10,000,000

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Nokleberg WJ, West TD, Dawson KM, Shpikerman VI, Bundtzen TK,Parfenov LM, Monger JWH, Ratkin VV, Baranov BV, ByalobzheskySG, Diggles MF, Eremin RA, Fujita K, Gordey SP, Gorodinskiy ME,Goryachev NA, Feeney TD, Frolov YF, Grantz A, Khanchuk AI,Koch RD, Natalin BA, Natapov LM, Norton IO, Patton WWJ,Plafker G, Pozdeev AI, Rozenblum, IS, Scholl DW, Sokolov SD,Sosunov GM, Stone DV, Tabor RW, Tsukanov NV, Vallier, TL (1998)Summary terrane, mineral deposit, and metallogenic belt mapsof the Russian Far East, Alaska, and the Canadian Cordillera: U.S.Geological Survey Open-File Report 98-136, 1 CD-ROM

Obruchev VV (1928) Various investigations on ore deposit systematics:

J Mineralogy, Geology, and Paleontology A-4: 143-146 (in German)Parfenov LM, Vetluzhskikh VG, Gamyanin GN, Davydov YuV,

Deikunenko AV, Kostin AV, Nikitin VM, Prokopyev AV, SmelovAP, Supletsov VM, Timofeev VF, Fridovsky VYU, KholmogorovAI, Yakovlev YaV (1999) Metallogenic zonation of the territory ofSakha Republic: Pacific Ocean Geology, 2: 8-40

Smirnov VI (1969) Geology of useful minerals: Nedra, Moscow, 687(in Russian)

Zonenshain LP, Kuzmin MI, Natapov LM (1992) Plate tectonics andore deposits in Northern Eurasia (the former USSR) [abs]: Colo-rado School of Mines Quarterly Review, 92: 13

Rodionov · Obolenskiy · Badarch · Dejidmaa · Distanov · Gerel · Hwang · Nokleberg · Ogasawara · Prokopiev · Seminsky · Smelov · Sotnikov · Spiridonov · Yan

Abstract. The northern part of the Eastern Asia Tin Belt occurs in theRussian Far East and contains five tin-bearing areas. The Russian FarEast is one of the largest tin regions in the world. Numerous andwell-known districts with tin lode deposits are known fromVladivostok in the south to the Chukchi Peninsula in the north. About43,000 tonnes of tin concentrate were produced in the Russian FarEast from 1991 to 1995. The geodynamic setting of the tin areas ofRussian Far East is determined by their occurrence at the junctionzones of various tectonic-stratigraphic units. The age of tin bearingintrusive rocks and associated Sn deposits of the Russian Far Eastranges from Devonian to Miocene with a maximum in the Creta-ceous

Keywords. Tin, metallogeny, Russia, intrusive, geodynamic

1 Regional setting of tin districts

The Russian Far East is a part of the Eastern Asia Tin Beltthat extends from Indonesia in the south to the ChukchiPeninsula in the north. The northern part of the EasternAsia Tin Belt in the Russian Far East is represented byfive tin districts – Chukotka, Kolyma, Yana-Indigirka,Khingan-Okhotsk, and Sikhote-Alin (Fig. 1).

The Russian Far East is one of the largest tin regionsin the world. Numerous well-known districts with tin lodedeposits were discovered from Vladivostok in the southto the Chukchi Peninsula in the north from 1937 to 1980.About 43,000 tonnes of tin concentrate were produced inthe Russian Far East from 1991 to 1995.

Previous studies of tin metallogeny of the Russian FarEast were mainly based on the geosynclinal concept anddid consider the correlation between geodynamics and tinmetallogeny. Various modern publications interpret the tinmetallogeny of the Far East Russia from a plate tectonicpoint of view (Rodionov 1988, 2000; Gonevchuk 2002;Mitrofanov 2002).

According to Rodionov (1998, 2000), the geodynamicsetting of the tin districts of the Russian Far East is de-termined by their location at the junction zones of differ-ent tectonic-stratigraphic units of the following types: (1)cratonal and (or) metamorphosed continental marginterranes composed of Paleozoic and older metamorphicrocks; (2) accretionary wedge or subduction zone terranescomposed predominantly of Paleozoic and early Meso-zoic chert-volcanic-terrigenous rocks; (3) turbidite ba-sin terranes composed predominantly of Mesozoic con-tinental slope terrigenous rocks with local tectonic lensesand inclusions of deep-water oceanic calcareous, sandy-argillaceous, and chert-volcanic rocks of Paleozoic andearly Mesozoic age; and (4) overlapping and stitching as-

semblages of calc-alkaline volcanic-plutonic belts of pre-dominantly late Mesozoic and Cenozoic age.

The geodynamic settings are illustrated by the rela-tion of tin deposits to corresponding structural elements(Fig. 2) and by composition features of tin magmatic com-plexes (Fig. 3).

2 Associated intrusive rocks

The age of tin-bearing intrusive rocks and associated Sndeposits of the Russian Far East varies from Devonian toMiocene with a maximum in the Cretaceous. The intru-sive rocks are characterized by a wide range of composi-tion, ranging from diorite, granodiorite, adamellite, bi-otite and (or) hornblende-biotite granite, to leucograniteand granite porphyry. These granitoids form two typesof multiple intrusive complexes that were were firstrecognised by Govorov (1973) and Rub et al. (1982).

The intrusive complex of the first type named as gra-nodiorite-granite complex, typically consists of granodior-ite and granite that form large batholiths. Spatially andtemporarily related are rare gabbro, gabbro-diorite, anddiorite that occur as dikes, or in the outer parts of grano-diorite-granite massifs, or as xenoliths in granite. Thesemore mafic rocks are interpreted as the earliest phase ofthe complex. The late, immediately pre-ore phase of thecomplex consists of dikes and stocks of leucocratic gran-ite, granite porphyry, and aplite that occur in or near thegranodiorite-granite batholiths. Mafic dikes, eithersynmineral or postmineral, also locally occur. The rocksof the granodiorite-granite complexes belong to the il-menite series with Fe2O3/FeO < 0.5 (Ishihara 1977), andare I-type (Chappell and White, 1974) mostly with a mo-lecular ratio of Al2O3/ (Na2O+K2O+CaO) of less than 1.1.

The granodiorite-granite complexes host tin quartzvein, tin greisen, and rare tin pegmatite deposits. The ore-magmatic systems including the granodiorite-granitecomplex and associated tin deposits occur mainly mainlyin the inner parts of tin-bearing areas. The formation ofthese ore-magmatic systems proceeded in a relativelystable tectonic environment. The intrusive bodies and re-lated deposits occur either at the margins of cratonal ter-ranes or in close proximity. Tin deposits occur close to smallintrusive bodies formed in the final magmatic stages of ore-magmatic systems. Mineralised fractures occur in foldedrocks and in the margins of magmatic bodies. The frac-tures are interpreted as having formed during either fold-ing, or intrusion and cooling of the magmatic bodies.

10-11 Chapter 10-11

Tin metallogeny of Far East RussiaS.M. RodionovInstitute of Tectonics and Geophysics, Far East Branch of Russian Academy of Sciences, Khabarovsk, Russia

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The second type of tin-bearing magmatic complex, i.e.,the diorite-granodiorite complex, comprises abundantmafic and intermediate rocks. Although the sequence of

the intrusive rocks is the same as in the first type of mag-matic complex, diorite and granodiorite are predominant.Gabbro and diorite of the first phases are of I-type ac-

S.M. Rodionov

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cording to the classification of Chappell and White (1974)with a molecular ratio of Al2O3/(CaO+Na2O+K2O) lessthan 1.1. Quartz diorite, granodiorite, and granite of thesecond phases have Al2O3/(Na2O+K2O+CaO) molecularratio of about 1.1 and less. The rocks of the third, imme-diately pre-ore phases are mostly S-type with a molecu-lar ratio of Al2O3/(Na2O+K2O+CaO) ≥ 1.1.

The diorite-granodiorite intrusive complexes occurmainly in the peripheral parts of tin-bearing areas, andare usually accompanied by comagmatic volcanic se-quences. This type of complex is associated with tinpolymetallic veins and porphyry tin deposits. The finalstages of the ore-magmatic systems occurred in areas thatwere tectonically active. Mineralized fractures are local-ized far from the intrusive bodies and are associated withregional structures.

The rocks of both intrusive complexes belong mainlyto ilmenite series (Ishihara 1977) with small variations.

To understand the differences and similarities of abovetwo tin magmatic complexes, the author studiedgeochemical evolution because the style of geochemicalevolution is one of the important features of tin granites(Lehmann 1990). Figure 4 shows contrasting tin contentsin different phases of the two tin magmatic complexes ofthe Russian Far East. The granodiorite-granite complexis characterized by a gradual increase in tin content inconsecutive order from early to late magmatic phases(Fig. 4a). The evolution of the diorite-granodiorite com-plex corresponds to tin enrichment of the interim phasesas well, but the last magmatic phase shows a relative de-crease of tin content (Fig. 4b).

This assumption is confirmed by employing theRittmann method (Rittmann 1973). The fields of early, in-terim, and late phases of both magmatic complexes occupythe corresponding close positions in a Streckeisen AQP dia-gram. The differentiation trends are also close (Fig. 6).

Figure 5 illustrates a gradual increase of initial Sr iso-tope ratio for tin magmatic complexes of the Russian FarEast. The value of initial Sr isotope ratio almost for allisochrons corresponds to the field of mixed mantle-crustalmaterial.

The two complexes were compared by the degree offractionating using the ratio of 1/K2O (according toTogashi 1985), and Sr differentiation for the example ofthe South-Sikhote-Alin belt. A relatively low degree of frac-tionation was discovered for the rocks of the granodior-ite-granite complex in contrast to the diorite-granodior-ite complex. The Sr differentiation is comparable in bothcomplexes. The fractionating trend of the rocks of themain phase of granodiorite-granite complex (low valueof 1/K2O ratio and low Sr value) continues for the samephase of diorite-granodiorite complex (relatively highvalue of 1/K2O ratio and Sr). Based on that comparison, itis possible to assume the propinquity of the initial mag-matic melt of both magmatic complexes.

Chapter 10-11 · Tin metallogeny of Far East Russia

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The correlation of K and Rb contents in host rockscan be a confirmation of the assumption of the propin-quity of the initial magmatic melt for both complexes. Asshown by Kovalenko et al. (1981) and Rub et al. (1983),the Rb content in initially mantle magma is about 80 ppmor less, and the K/Rb ratio is about 500 or more. Palinge-netic crustal magmas contain Rb of about 150 ppm ormore, and the K/Rb ratio is about 200 or less. The analy-sis of K-Rb correlation shows that rocks of the two tinmagmatic complexes occupy the same intermediate areabetween mantle and crustal magmas.

References

Chappel B, White A (1974) Two contrasting types of granites. PacificGeology 8: 173-174

Gonevchuk VG (2002) Tin-bearing systems of the Far East:magmatism and ore genesis. Vladivostok, Dalnauka, 298 (in Rus-sian)

Govorov IN (1973) Geochemical cycles and types of tin-bearingmagmatic complexes. In: Spatial regularities of useful minerals.Nauka, Moscow 10: 153-167 (in Russian)

Ishihara S. (1977) The magnetic-series and ilmenite series graniticrocks. Mining Geology 27: 293-305

Khanchuk AI, Ivanov VV (1999) Geodynamics of Eastern Russiaduring Mesozoic-Cenozoic gold mineralization. Geodynamicsand Metallogeny. Dalnauka, Vladivostok, 7-30 (in Russian)

Kovalenko VI, Antipin VS, Ryabchikov ID (1981) Variations of coef-ficient of Rb dispersion in magmatic rocks. Geokhimiya 6: 1017-1029 (in Russian)

Lehmann B (1982) Metallogeny of tin: Magmatic differentiation ver-sus geochemical heritage. Economic Geology 77: 50-59

Mitrofanov NP (2002) Geodynamic conditions of tin deposits forma-tion in northwestern part of Pacific ore belt. VIMS, Moscow, 47 (inRussian)

Nokleberg W, Parfenov LM, Khanchuk AI (1997) Circum-North Pa-cific Tectonostratigraphic Terrane Map. U.S. Geological SurveyOpen File Report 97-513-A, scale 1:5,000,000

Pearce JA, Harris NBW, Tindle AG (1981) Trace element discrimina-tion diagrams for the tectonic interpretation of granite rocks.Journal of Petrology 76: 956-983

Rittmann A (1973) Stable mineral associations of igneous rocks. Mir,Moscow, 288 (in Russian)

Rodionov SM (1988) Geology of-porphyry deposits of Zvezdny oredistrict. Primorie. Geologia Rudnykh Mestorozhdeniy 6: 45-55(in Russian)

Rodionov SM (2000) Tin metallogeny of the Russian Far East. In:Ore-bearing granites of Russia and adjacent countries. IMGRE,Moscow, 234-262

Rub MG, Pavlov VA, Gladkov NG (1982) Tin-bearing and tungsten-bearing granitoids of some ore districts of the USSR. Nauka,Moscow, 259 (in Russian)

Togashi Sh (1985) Sr variation by fractional crystallization for vol-canic rocks from island arc and continental margin. ChemicalGeology 51: 41-53

Whalen JB, Currce KL, Chappel BM (1987) A-type granites: geochemi-cal characteristics, discrimination and petrogenesis. Contributionsto Mineralogy and Petrology 95: 407-41

S.M. Rodionov

Keywords. Tectonics, metallogenesis, regional, geology, Northeast Asia

Abstract

The vast, mountainous terranes of Northeast Asia holdthe key to the tectonic and metallogenic evolution of amajor and geologically complicated region of the world.This region stretches from the Ural Mountains and theArctic Islands of central Russia to the Kamchatka vol-canic arc in the Russian Far East. The region also in-cludes northern Kazakhstan, China, Mongolia, the Ko-rean Peninsula, and Japan. The tectonic development ofthe region is recorded in a series of cratons, craton mar-gins, oceanic plates, active rifts, and orogenic collages ofthe present-day Northeast Asia continent. The collagesconsist of tectonostratigraphic terranes that are com-posed of fragments of igneous arcs, accretionary-wedgeand subduction-zone complexes, passive continentalmargins, and cratons. The tectonostratigraphic terranesare overlapped by continental-margin-arc and sedimen-tary-basin assemblages. The tectonic history of cratons,

craton margins, oceanic plates, terranes, and overlap as-semblages is complex due to extensional dispersion andtranslation during strike-slip faulting that occurred sub-parallel to continental margins.

This talk presents a series of regional tectonic time-slicemaps and a computer animation that dynamically illus-trate the tectonic assembly and major metallogenic eventsof Northeast Asia since the late Precambrian. The key eventsin the tectonic history of Northeast Asia are: (1) the forma-tion of the Siberian craton during the breakup of a latePrecambrian supercontinent (Pannotia); (2) the establish-ment, during the late Precambrian and early Paleozoic, ofan active subduction zone along the present-day, southernmargin of Siberia (Mongolian subduction zone); (3) clo-sure of oceans between Siberia and Baltica (Ural Moun-tains), Kazakhstan and Siberia (Tien Shan Mountains), andNorth China and Amuria (Solonker zone) during the latePaleozoic; (4) the progressive closure of the Amurian sea-way between northern China and Siberia during the Triassicand Jurassic to form the core of present-day Northeast Asia;(5) the Late Jurassic through early Cenozoic arrival of

10-13 Chapter 10-13

Tectonic and metallogenic evolution of northeast Asia:Key to regional understandingChristopher R. ScoteseDepartment of Geology, University of Texas, Arlington, TX 76019 USA

Warren J. NoklebergU.S. Geological Survey, Menlo Park, CA 94025 USA

Leonid M. ParfenovInstitute of Diamond and Noble Metal Geology, Russian Academy of Sciences, Yakutsk, 677000 Russia

Gombosuren BadarchInstitute of Geology and Mineral Resources Mongolian Academy of Sciences, Ulaanbaatar 210351 Mongolia

Nikolai A. BerzinInstitute of Geology, Russian Academy of Sciences, Novosibirsk 630090 Russia

Alexander I. KhanchukFar East Geological Institute, Russian Academy of Sciences, Vladivostok 690022 Russia

Mikhail I. KuzminInstitute of Geochemistry, Russian Academy of Sciences, Irkutsk 664033 Russia

Alexander A. ObolenskiyInstitute of Geology, Russian Academy of Sciences, Novosibirsk 630090 Russia

Andrei V. ProkopievInstitute of Diamond and Noble Metal Geology, Russian Academy of Sciences, Yakutsk, 677000 Russia

Sergey M. RodionovInstitute of Tectonics and Geophysics, Russian Academy of Sciences, Khabarovsk 680052 Russia

Hongquan YanGeological Research Institute, College of Earth Sciences, Jilin University, Changchun 130061 China

1184

allochtonous terranes in northern Siberia and the RussianFar East; (6) in the early Cretaceous, for the first time for-mation of a continuous continental complex between theRussian Northeast northwestern North America; and finally(7) in the Cenozoic, the formation of continental-marginarcs and back-arc basins along the entire Pacific-facing

margin of Northeast Asia. We hope that this preliminarytectonic and metallogenic model of Northeast Asia, throughincomplete and speculative, will provide new insights intothe geologic, tectonic, and metallogenic evolution of thiscomplex region, and will provide a basis for further studyand investigation.

C.R. Scotese · W.J. Nokleberg · L.M. Parfenov · G. Badarch · N.A. Berzin · A.I. Khanchuk · M.I. Kuzmin · A.A. Obolenskiy · A.V. Prokopiev · S.M. Rodionov · H. Yan

Геодинамика, магматизм и металлогения Востока России: - Владивосток: Дальнаука, 2006. -Кн.1-2. – 981с. + цв. карта+ 5 п.л. цв.вкл.

Монография представляет собой наиболее полную современную сводку по тектонике, геодинамике, сейсмичности,магматизму и полезным ископаемым дальневосточной окраины России.Охарактеризованы террейны различной геоди-намической природы, детально описаны перекрывающие геологические комплексы,магматические и металлогенические пояса, а также месторождения полезных ископаемых, сформировавшиеся в обстановках субдукционного, трансформного и коллизионного взаимодействия литосферных плит и внедрения мантийных плюмов.Показаны современная геодина-мика и сейсмичность территории, расшифровано ее глубинное строение. Впервые мезозойская и кайнозойская геодина-мическая история Восточной Азии представлена как чередование во времени и пространстве надсубдукционных итрансформных континентальных окраин и установлены тектонические, геохимические и металлогенические индикаторы древних трансформных окраин региона.

Для специалистов в области наук о Земле, горнорудной промышленности, аспирантов и студентов геологических специальностей вузов.

Ил. 318, табл. 73, библ. 2138.

Р е д а к ц и о н н а я к о л л е г и я :А.И. Ханчук (ответственный редактор)

СМ. Родионов, Н.А. Горячев, В.К. Попов,В.В. Голозубов, В. В. Наумова

Рецензенты: чл.-корр. РАН Е.В. Скляров, д.г.-м.н.А.С Борисенко

© Дальневосточное отделение РАН, 2006 ISBN 5-8044-0634-5 © Редакционно-издательское оформление.Дальнаука, 2006

По вопросам содержания монографии можно обращаться по адресам:naumova@fegi.rurodionov@itig.as.khv.ru