Summary of Northeast Asia geodynamics and tectonics · 4/11/2009 · summary geodynamics map of the region, and also pro-vides a general introduction for readers who are unfamil-iar

Stephan Mueller Spec. Publ. Ser., 4, 11–33, 2009www.stephan-mueller-spec-publ-ser.net/4/11/2009/© Author(s) 2009. This work is distributed underthe Creative Commons Attribution 3.0 License.

SpecialPublication

Series

Summary of Northeast Asia geodynamics and tectonics∗

L. M. Parfenov1,†, G. Badarch2, N. A. Berzin3, A. I. Khanchuk 4, M. I. Kuzmin 5, W. J. Nokleberg6, A. V. Prokopiev1,M. Ogasawara7, and H. Yan8

1Russian Academy of Sciences, Yakutsk, Russia2Mongolian Academy of Sciences, Ulaanbaatar, Mongolia3Russian Academy of Sciences, Novosibirsk, Russia4Russian Academy of Sciences, Vladivostok, Russia5Russian Academy of Sciences, Irkutsk, Russia6US Geological Survey, Menlo Park, USA7Geological Survey of Japan/AIST, Tsukuba, Japan8Jilin University, Changchun, China†deceased∗Prepared in memory of Leonid M. Parfenov, the leader of the geodynamics map team for the International collaborativeproject on NE Asia tectonics and metallogenesis.

Abstract. The compilation, synthesis, description, and inter-pretation of regional geology and tectonics of major regions,such as Northeast Asia (Eastern Russia, Mongolia, NorthernChina, South Korea, and Japan) and the Circum-North Pa-cific (the Russian Far East, Alaska, and Canadian Cordillera),requires a complex methodology that includes: (1) defini-tions of key terms; (2) compilation of a regional geodynam-ics map that can be constructed according to modern tectonicconcepts and definitions; and (3) formulation of a compre-hensive tectonic model. This article presents a summary ofthe regional dynamics and tectonics of Northeast Asia as de-veloped for a new summary geodynamics map of the region.This article also describes how a high-quality summary geo-dynamics map and companion tectonic analysis substantiallyaids in the understanding of the origin of major rock units,major structures, and contained mineral and fuel resources,and provides important guidelines for new research.

1 Introduction

This article presents an overview of the regional geodynam-ics and tectonics of Northeast Asia as presented in a newsummary geodynamics map of the region, and also pro-vides a general introduction for readers who are unfamil-iar with Northeast Asia. For this analysis, the region of

Correspondence to:A. V. Prokopiev([email protected])

Northeast Asia project area consists of Eastern Russia (East-ern Siberia and the Russian Far East), Mongolia, NorthernChina, the Korean Peninsula, Japan, and adjacent offshoreareas (Fig. 1).

The summary of regional geodynamics and tectonics inthis article is based upon publications of a major interna-tional collaborative study of the metallogenesis and tectonicsof Northeast Asia and of the Circum-North Pacific, whichwere led by W. J. Nokleberg of the the US Geological Sur-vey. Two broad types of publications have been produced bythis collaboration. One type is a series of regional geologic,mineral deposit, and metallogenic belt maps and companiondescriptions for the region (Greninger et al., 1999; Obolen-skiy et al., 2003a, b, 2004; Parfenov et al., 2003, 2004a, b;Nokleberg et al., 1994, 1997a, b, c, 1998, 2004; Rodionov etal., 2004; and Naumova et al., 2006). The other type is a suiteof metallogenic and tectonic analyses of these same regions(Nokleberg et al., 2000, 2005; Rodionov et al., 2004).

2 Definitions, geologic time scale, and tectonicenvironments

In order to illustrate the regional geology of a large regionmost clearly in a page-size format, Fig. 2 utilizes the conceptof tectonic collages (see definition, Table 1). This definitionof tectonic collage enables: (1) a readily-understood concep-tual framework for understanding the geology and tectonicsof large regions; (2) the depiction at small scales of majorgeologic units and structures that formed in a single tectonic

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12 L. M. Parfenov et al.: Summary of Northeast Asia geodynamics and tectonics

International boundaries for onshore area are approximate and do not indicate endorsement by participating countries.

0 500 1000 Km

96

Hatgal

LakeBaikal

Khanka

Ulaangom

VLADIVOSTOK

KHABAROVSK

CHANGCHUN

TAEJON

TOKYO

TSUKUBA

SEOUL BEIJING

IRKUTSK

ULAN UDE

ULAANBAATAR

YAKUTSK

MAGADAN

PETROPAVLOVSK

NOVOSIBIRSK

646872768082

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108 114 120

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M O N G O L I A

C H I N A

R U S S I A

NORTH-CENTRALCHINA

NORTHWESTCHINA

SORT EA T

N HHINAC

C

uk

ot k

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a

KOREANPENINSULA

A

JA

P

N

P

ac

fc

Oea

ii

cn

ig

Ber

nS

ea

ptev aLa

Se

S

ea of

Okhotsk

Ku

rle

Ila

ns

is

d

aS

e

a

st

ibria

n Se

E

Karal Sea

Y k ia u t a

S

ri

e

a

ib

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

ss

R u

i a

n Fa

r

ac

a

K

m

h k

ta

a s tE

Figure 1Fig. 1. Regional summary geographic map for Northeast Asia showing major regions and countries.

event; and (3) the understanding of the origins of major min-eral and hydrocarbon deposits related to the formations andmodification of tectonic collages.

Definitions of other key terms for the analysis of regionalgeology and tectonics are provided in Table 1. These def-initions are adapted from Howell et al. (1985), Jones etal. (1983), and Nokleberg et al. (2000, 2005). Geologic timescale units are according to the IUGS Global StratigraphicChart (Remane, 1998). For this study and in some of thecited publications, the termRipheanis used for the Mesopro-terozoic to Middle Neoproterozoic (1600 to 650 Ma), and thetermVendianis used for Neoproterozoic III (650 to 540 Ma).

For a modern geologic analysis, the classification into tec-tonic environments is essential for determining the geologicorigins of major units and contained mineral and hydrocar-bon resources. This permits the interpretations of originof both host rocks and associated resources. For the tec-tonic analyses of Northeast Asia and the Circum-North Pa-cific (Nokleberg et al., 1997b, c, 2000, 2005; Scotese etal., 2001; Obolenskiy et al., 2003; Parfenov et al., 2003,2004a, b), the major geologic units (terranes, overlap as-semblages, plates), mineral deposits, mineral deposit types,and metallogenic belts, are classified into the following tec-tonic environments (Table 1): (1) cratonal and craton margin;

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L. M. Parfenov et al.: Summary of Northeast Asia geodynamics and tectonics 13

(a)Devonian aulacogene

Figure 2 - Map

Riphean aulacogeneThrust

Strike - slip fault

Fault

Oceanic rift

Contact

Symbols, Faults, and Contacts

Overlap continental margin arc

Transform continental margin arc

Active subduction zone

2000 KM10000

Kuril-Kamchatka

Arc

GYGY

GYGY

GYGY

NACNAC

SKCSKC

HS

HS

BJ

HSHS

KR

ST

BeringSea

PacificOcean

LaptevSea

CS

VK

VK

KOM

SA CH

oc

nb, ol

uy, ma

oc

oc

KOR

VR

OH

PA

WK

OK

OK

PA

WK

OK

EP

WS

CS

EA

BP

AL

AL

AL

YT

YT

YT

YT

YT

AR

AR

TM

SM

SMAB

ABSL

SL

SLJA

WD

BJ BJ

BJ

BJ

BD

HS

HS

ea

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Sea ofOkhotsk

LakeBaikal

East-SiberianSea

kk

MO

MO

P A C I F I C

P L A T E

ES

ESMO

Fig. 2a. Northeast Asia summary geodynamics map. Map is derived from: (1) a generalized Northeast Asia geodynamics map at 10 millionscale (Parfenov et al., 2004); (2) a more detailed Northeast Asia geodynamics map at 5 million scale (Parfenov et al., 2003); and (3) thewestern part of a Circum-North Pacific tectono-stratigraphic terrane map at 10 million scale (Nokleberg et al., 1997). Map shows locationsmajor geologic and tectonic units including cratons, craton margins; cratonal terranes and superterranes; tectonic collages; overlap andtransform continental-margin arcs; island arcs, and sea and ocean units.(a) Map. (b) Explanation. Refer to Appendix for descriptions ofmap units.

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(b)

EXPLANATION

Cratons and Craton Margins

Figure 2 - Explanation

NAC - North Asian Craton (Archean andProterozoic);SKC - Sino-Korean Craton(Archean and Proterozoic)

Craton Margin: BP - Baikal-Patom(Riphean to Cambrian and older basement;EA - East Angara (Riphean and older basement; ST - South Taimyr (Ordovician toJurassic); VR - Verkhoyansk (Devonian toJurassic).

Tectonic Collages Between North Asian andSino-Korean Cratons (older to younger)

Tectonic Collages Along Northern andEastern Margins of North Asian andSino-Korean Cratons (older to younger)

Active Subduction Zones

CS - Circum-Siberia (Proterozoic)

YT - Yenisey-Transbaikal (Vendianto Early Ordovician)

AL - Altay (Vendian to Ordovician)WD - Wundurmiao (Riphean to Ordovician)

AB - Atasbogd ( ; SM - South Mongolia-Khingan (Ordovician toCarboniferous); WS - West Siberian (Ordovician to Carboniferous)

Ordovician through Permian)

MO - Mongol-Ohkotsk (Devonian to Late Jurassic); SL - Solon (Carboniferousto Permian)

CH - Chukotka (Paleozoic to Triassic)

BD - Badzhal (Triassic to Early Cretaceous); PA - Penzhina-Anadyr (Late Jurassic toCretaceous); HS - Honshu-Sikhote-Alin (Jurassic to Early Cretaceous); SA - South Anyui (Permian to Jurassic);

VK - Verkhoyansk-Kolyma Paleozoic to Early Jurassic)

KOR - Koryak (Late Jurassic to Paleocene;SH - Sakhalin-Hokkaido (Cretaceous); WK - West Kamchatka (Mid-Cretaceous toEarly Tertiary)

ES - East Sakhalin (Late Cretaceous toEarly Tertiary); OK - Olyutorka-Kamchatka (Late Cretaceous to Paleocene)

Cratonal Terranes (Archean andProterozoic): GY - Gyeonggi-Yeongnam; JA - Jiaonan; OH - Okhotsk

Cratonal Terranes (Archean andProterozoic): GY - Gyeonggi-Yeongnam; JA - Jiaonan; OH - Okhotsk

Late Proterozoic to Cambrian Supterterranes;AR - Argun-Idermeg; TM - Tuva-Mongolia

Archean to Permian Superterranes: BJ - Bureya-Jiamusi; KR - Kara

Jurassic Superterrane:KOM - Kolyma-Omolon (Archean to Jurassic)

Oceanic crust

Surficial units

Sea and Ocean Units

Cratonal Terranes and Superterranes

Overlap Continental Margin Arcs and Granite Belts

- Altay arc (Devonian and early Carboniferous, 381-290 Ma))East Sikhote-Alin arc (Late Cretaceous to early

Tertiary, 96-65 to Ma) - arc

- Lugyngol arc (Permian, 295-250 Ma)- Hangay arc (

arc arc

- Norovlin arc (Devonian, 410-255 Ma) - Okhotsk-Chukotka arc (Late Cretaceous to early

Tertiary, 96-53 Ma)- arc - Selenga arc (- South Mongolian arc (Middle Carboniferous through Triassic , 320-203

Ma)- South Verkhoyansk granite belt (Late Jurassic to mid-Cretaceous, 157-

93 Ma)- Transverse granite belt (Early Cretaceous, 134-124 Ma)- Uda-Murgal and Stanovoy arc (

arc (Late Jurassic to Early Cretaceous, 154-120 Ma)

- arc

Active Arcs

- Izu-Bonin (Late Cenozoic, 20-0 Ma)- Japan (Late Cenozoic, 23-0 Ma)- Kuril-Kamchatka (Late Cenozoic, 11-0 Ma)

at ea -

gh lg ha

nr oc

ol sesm

sv

tr us

uo

ib ja kk

Gobi-Khankaisk-Daxing'anling (Permian, 295-250 Ma)

Late Carboniferous to Early Permian, 320-272 Ma)- Jihei (Permian, 295-250 Ma)

- Khingan-Okhotsk (Early and mid-Cretaceous)Main granite belt (Late Jurassic, 144-134 Ma)

- Northern granite belt (Early Cretaceous, 138-120 Ma)North Margin (Late Carboniferous to Permian, 320-272 Ma)

Oloy (Late Jurassic, 154-135 Ma)Permian to Jurassic, 295-135 Ma)

Jurassic to Early Cretaceous, 203-96 Ma)- Uyandina-Yasachnaya

Umlekan-Ogodzhin (Cretaceous, 135-65 Ma)

ji ko ma nb nm -

uy

Transpressional Arcs

- Mongol-Transbaikal (- South Siberian

-

mt ss tr

Late Triassic to Early Cretaceous, 230-96 Ma) (Early Devonian, 415-400 Ma)

Trans-Baikalian-Daxinganling (Middle Jurassic through Early Cretaceous,175-96 Ma)

EP - East Kamchatka Peninsular (Mainly Paleocene)

JT- Japan Trench (including Kuril-Kamchatka trench) (Miocene to Present); NN - Nankai (Miocene to Present)

Fig. 2b. Continued.



Table 1. Definitions of key terms for the regional geologic and tectonic analysis of Northeast Asia. Adapted from Jones et al. (1983), Howellet al. (1985), and Nokleberg et al. (2000, 2003).

Term Definition

Accretion Tectonic juxtaposition of terranes to a craton or craton or continental margin. Accretion of terranes to one another orto a craton margin also definesa major change in the tectonic evolution of terranes and craton margins.

Accretionary-wedge Fragment of a mildly to intensely deformed complex consisting of varying amounts of turbidite deposits continental-margin,terrane rocks, oceanic crust and overlying units, and oceanic mantle. Units are interpreted to have formed during tectonic

juxtaposition in a zone of major thrusting of one lithosphere plate beneath another, generally in zones of thrusting alongthe margin of a continent or an island arc. May include large fault-bounded fragments with a coherent stratigraphy. Manysubduction-zone terranes contain fragments of oceanic crust and associated rocks that exhibit a complex structural history,occur in a major thrust zone, and possess blueschist-facies metamorphism.

Amalgamation Tectonic juxtaposition of two or more terranes before accretion to a continental margin.

Craton Chiefly regionally metamorphosed and deformed shield assemblages of Archean and Early Proterozoic sedimentary, volcanic,and plutonic rocks, and overlying platform successions of Late Proterozoic, Paleozoic, and local Mesozoic andCenozoic sedimentary and lesser volcanic rocks.

Continent A large section of continental crust surrounded by oceans on all sides, which consist, in its core, of oneor more cratons framed by younger tectonic collages (accretionary and collisional orogenic belts).

Continental-margin Fragment of an igneous belt of coeval plutonic and volcanic rocks and associatedarc terrane sedimentary rocks that formed above a subduction zone dipping beneath a continent.

Inferred to possess a sialic basement.

Craton Chiefly regionally metamorphosed and deformed shield assemblages of Archean, Paleoproterozoic, andMesoproterozoic sedimentary, volcanic, and plutonic rocks, and overlying platform successions ofPaleoproterozoic, Paleozoic, and local Mesozoic and Cenozoic sedimentary and lesser volcanic rock.

Craton margin Chiefly Neoproterozoic to Jurassic sedimentary rocks deposited on a continental shelf or slope. Consists mainlyof platform successions. Locally has, or may have had an Archean and Early Proterozoic cratonal basement.

Cratonal terrane Fragment of a craton.

Island-arc system An island arc and tectonically linked subduction zone terranes.

Island-arc terrane Fragment of an igneous belt of plutonic rocks, coeval volcanic rocks, and associated sedimentary rocks that formedabove an oceanic subduction zone. Inferred to possess a simatic basement.

Metamorphic terrane Fragment of a highly metamorphosed or deformed assemblage of sedimentary, volcanic, or plutonic rocks that cannot beassigned to a single tectonic environment because the original stratigraphy and structure are obscured. Includesintensely deformed structural melanges that contain intensely deformed fragments of two or more terranes.

Oceanic crust, Fragment of part or all of a suite of deep-marine sedimentary rocks, pillow basalt, gabbro, and ultramafic rocks (former eugeoclinalseamount, and eugeoclinal suite) that are interpreted as oceanic sedimentary and volcanic rocks and the upper mantle. Includes both inferredophiolite terrane offshore oceanic and marginal ocean basin rocks, minor volcaniclastic rocks of magmatic-arc derivation, and major

marine volcanic accumulations formed at a hotspot, fracture zone, or spreading axis.

Overlap assemblage A postaccretion unit of sedimentary or igneous rocks deposited on, or intruded into, two or more adjacent terranes.

Passive continental-margin terrane Fragment of a craton (continental) margin.

Subduction zone terrane Fragment of a mildly to intensely deformed complex consisting of varying amounts of turbidite deposits,continental-margin rocks, oceanic crust and overlying units, and oceanic mantle. Units are interpreted to have formedduring tectonic juxtaposition in a zone of major thrusting of one lithosphere plate beneath another, generally in zonesof thrusting along the margin of a continent or an island arc. May include large fault-bounded fragments with a coherent .stratigraphy Many subduction-zone terranes contain fragments of oceanic crust and associated rocks that exhibit a complexstructural history, occur in a major thrust zone, and possess blueschist-facies metamorphism.

Superterrane A series of amalgamated terranes and/or a rifted fragment of a craton and (or) craton margin which exhibitsa long and complicated geologic history. May contain overlap island arc complexes and tectonically-linked subduction zones.

Tectonic collage A series of linear island arcs or continental margin arcs and tectonically-linked (companion) subduction zones, and (or)fore-arc and back-arc basins that formed in a major tectonic event during a relatively narrow geologic time span. The collagesof igneous arcs and companion subduction zone terranes have been successively accreted to the margins of major cratons.The ages of collages with subduction zone units are for time of active formation of an accretionary wedge in a subductionzone, rather than the older range of units that comprise the accretionary wedge. A few collages consist of fragmentsof craton margin and cratonal terranes that were amalgamated before accretion to a continent.

Tectonic linkage A genetic relation of a continental margin arc or an island arc with a companion accretionary wedge that formed in a subductionzone that was adjacent to, and was underthrusting the arc.

Tectonostratigraphic An aggregate of terranes that is interpreted to share either a similar stratigraphic kindred or affinity, or a common geologic history afterterrane (terrane) accretion (Jones and others, 1983; Howell and others, 1985). An approximate synonym is composite terrane (Plafker and Berg, 1994).

Terrane A fault-bounded geologic entity or fragment that is characterized by a distinctive geologic history that differsmarkedly from that of adjacent terranes (Jones and others, 1983; Howell and others, 1985).

Turbidite terrane Fragment of a basin filled with deep-marine clastic deposits in either an orogenic forearc or back-arc setting.May include continental-slope and continental-rise turbidite deposits, and submarine-fan turbiditedeposits deposited on oceanic crust. May include minor epiclastic and volcaniclastic deposits.



(2) passive continental margin; (3) metamorphosed continen-tal margin; (4) continental-margin arc and back-arc; (5) is-land arc and back-arc; (6) oceanic crust, seamount, or ophio-lite related to rifting and sea-floor spreading; (7) accretionarywedge and subduction zone; (8) turbidite basin; (9) colli-sional; (10) transform continental-margin faulting and asso-ciated bimodal volcanic-plutonic belt; (11) plume; and (12)metamorphic. For terranes with complex geologic and tec-tonic histories, the chosen tectonic environment is the onethat was the most prevalent during the history of the terrane.The reader should refer to the associated citations for moredetailed descriptions of these terranes with complex histo-ries.

3 Compilation of regional geodynamics map

A regional geodynamics map was initially compiled at ascale of 1:5 000 000 (Nokleberg et al., 1997b, c; Parfenovet al., 2003, 2004a, b). However, in order to display ma-jor features of host rock geology and structures and majorbelts of mineral and hydrocarbon resources a page-size il-lustration, a summary regional geodynamics map (Fig. 2)was constructed at a scale of about 1:34 000 000 in orderto display: (1) the regional surface extent of major geologicunits (cratons, craton margins, tectonic collages of island arc,continental-margin arc, accretionary wedge, and passive con-tinental margin terranes, volcanic and plutonic igneous arcs);(2) major fault and rift systems; and (3) active subductionzones. A list of major host-rock geologic units in the expla-nation and a description of major geologic units for the mapis provided in Appendix A. The tectonic interpretations forthe summary map are derived from the major publications ofthe collaborative international studies on Northeast Asia andthe Circum-North Pacific (listed above).

4 Methodology of regional geologic and tectonicanalysis

The methodology employed for synthesizing the summarygeodynamics map consisted of: (1) correlation of major ge-ologic units; (2) tectonic linking (pairing) of major geo-logic units; and (3) alignment of coeval arc and tectonically-linked subduction zones into curvilinear complexes. A sim-ilar methodology was utilized for a synthesis of the Circum-North Pacific (Nokleberg et al., 2000).

Initially, correlations are attempted for major geologicunits which are interpreted as having been originally con-tiguous but were subsequently tectonically displaced duringrifting, major thrusting, or along strike-slip faults. Correla-tions are attempted for all regional units (cratons, craton mar-gins, terranes, and overlap assemblages) that are understoodto have the same tectonic origin, (i.e., as parts of a singleelongate passive continental margin, continental-margin arc,island arc, or subduction zone) at the same geologic time and

originally on strike with each other. This correlation of ma-jor geologic units also illustrates the original continuity ofrock units, provides important constraints on the past tecton-ics of the region, and provides a series of interpretations tobe further evaluated by additional stratigraphic, geochemical,isotopic, paleomagnetic, and geophysical studies.

Following this step, tectonic linking (pairing) was basedon pairing of: (1) subduction-related igneous arcs, now pre-served as various igneous-arc terranes or overlap assem-blages, with former subduction zones, now preserved assubduction-zone terranes; (2) belts of anatectic-related ig-neous rocks and major faults (sutures) that bound the col-lisional margins of terranes with each other or terranes witha craton margin; and (3) belts of igneous rocks that are coevalwith, and occur along major transpressional fault zones.

The first type of tectonic linking can be based on: (1) rec-ognizing an original physical proximity between an arc andsubduction zone; (2) determining the similarity in age of for-mation of an igneous-arc and subduction-zone terrane, (3)determining a subduction polarity from tectonic transport di-rection in a melange for subduction-zone terranes, where notdisrupted by later deformation, and (4) recognizing the oc-currence of disrupted layers of arc-derived volcanic or vol-caniclastic units from a specific igneous arc in the melangeof the linked subduction zone terrane.

A second type of tectonic linking is based on the spa-tial and temporal association of collisional (S-type) graniticplutons and associated volcanic rocks with: (1) major faultzones (sutures) between terranes or between a terrane anda craton margin; and (or) (2) belts of highly deformed,regional-grade metamorphic rocks that occur along the faultzones. Collision-related igneous belts are understood asforming either during accretion of one terrane to another orduring the accretion of one or more terranes to a craton mar-gin.

A third type of tectonic linking is based on the spatialand temporal association of mainly intermediate and silicicigneous belts that are coeval with, and intrude along majortranspressional fault zones.

Following these steps, terranes and overlap assemblagesare grouped into larger entities that are understood tohave been continuous, coeval igneous arcs and companionsubduction-zones. This grouping of units is based, to vary-ing degrees, on: (1) similar stratigraphy, fauna, rock-unitage, and structure; (2) paleomagnetic data, to a lesser de-gree; and (3) an assumption of simplicity. The result of thesegroupings is the alignment of coeval igneous-arc overlap as-semblages and igneous-arc terranes, and tectonically-linked(companion) subduction-zone terranes into coeval, curvilin-ear arc-subduction-zone complexes.



5 Summary of regional geology and tectonicsof Northeast Asia

The major regional geologic and tectonic units of North-east Asia are cratons, craton margins; cratonal terranesand superterranes; tectonic collages; overlap and transformcontinental-margin arcs; island arcs, and sea and oceanunits (Fig. 2). Detailed descriptions of geologic units are pre-sented by Nokleberg et al. (2000) and Parfenov et al. (2004b).Abbreviations in parentheses in the following list of geo-logic units refer to units on the summary geodynamics map(Fig. 2). More detailed descriptions of map units are given inAppendix A. Two geologic ages are staged for each collage,one for the age of formation of the units in a collage, such,and another age for the time of accretion (formation) of thecollage to another terrane, superterrane, or continent.

5.1 Major cratons and craton margins

The backstop or core units for the region of Northeast Asiaare the Archean and Proterozoic North Asia Craton and Sino-Korean Craton and their Craton Margins (Baikal-Patom, An-gara, South Taimyr, and Verkhoyansk (North Asian)).

The North Asian Craton (NAC) consists of Archean andProterozoic metamorphic basement, and non-deformed, flat-laying platform cover consisting of Late Precambrian, Pale-ozoic, and Mesozoic sedimentary and volcanic rock.

The Sino-Korean Craton (SKC) consists of several ma-jor Archean and Proterozoic metamorphic basement terranesand younger Paleozoic through Cenozoic overlap units.

The Baikal-Patom Craton Margin (BP) consists of a fault-bounded basin containing Riphean carbonate and terrigenoussedimentary rock, and younger Vendian and Cambrian sedi-mentary rock that discordantly overly a fragment of the pre-Riphean basement of the North Asian Craton.

The East Angara Craton Margin (EA) consists of LateRiphean terrigenous-carbonate sedimentary rock (sandstone,siltstone, mudstone with interlayered dolomite and lime-stone) that overlie a fragment of the North Asia Craton.

The South Taimyr Craton Margin (ST) consists chiefly of athick wedge of Ordovician to Jurassic craton margin depositsand deep basin deposits.

The Verkhoyansk (North Asian) Craton Margin (VR) con-sists chiefly of a thick wedge of Devonian to Jurassic mio-geoclinal deposits.

5.2 Cratonal terranes and superterranes

Three cratonal terranes occur along the margins of the NorthAsian and Sino-Korean Cratons and are understood as riftedand reaccreted fragments of these cratons, in contrast to ex-otic terranes which are understood to be far travelled. Thecratonal terranes are as follows. (1) The Okhotsk terrane(OH) terrane consists of Archean and Proterozoic gneissand schist and Early and Middle Paleozoic miogeoclinal

sedimentary rock. The terrane is considered to be a fragmentof the North Asian Craton and Margin that was rifted in theLate Devonian or Early Carboniferous. (2) The Gyenggi-Yeongnam terrane (GY) consists of two major Archean andProterozoic basement rock terranes. The terrane is consid-ered to be a displaced fragment of the Sino-Korean Craton.(3) The last of these terranes is the Jiaonan cratonal terrane(JA) which consists of a Paleoproterozoic major high pres-sure terrane that is interpreted as a displaced fragment of theSino-Korean Craton.

Six superterranes occur along the margins of the NorthAsian and Sino-Korean Cratons. Some of the superterranesare considered to be rifted and reaccreted fragments of thecratons whereas others are understtod to having formed else-where.

The Proterozoic to Cambrian Argun-Idermeg superterrane(AR) consists of the Paleoproterozoic to Late Paleozoic Ar-gunsky, Idermeg, and West Stanovoy metamorphosed pas-sive continental-margin terranes. The superterrane may beeither exotic with respect to the North Asian Craton or maybe a rifted fragment of the craton.

The Late Riphean and older Tuva-Mongolia superterrane(TM) consists of a series of Archean and Paleoproterozoiccratonal terranes (Gargan and Baydrag), the Snagilen pas-sive continental-margin terrane, and the Muya metamorphicterrane. These terranes are understood to have accreted to-gether to form the rear or back arc part of the Baikal-Myraisland arc described below.

The Proterozoic to Permian Bureya-Jiamusi supterter-rane (BJ) consists of a collage of Early Paleozoic meta-morphic, continental-margin arc, subduction zone, passivecontinental-margin and island arc terranes. The superterraneis considered to be a fragment of Gondwana that was ac-creted to the Sino-Korean Craton in the Late Permian andaccreted to the North Asian Craton in the Late Jurassic dur-ing final closure of the Mongol-Okhotsk Ocean.

The Proterozoic to Ordovician Kara superterrane (KR)consists of the Late Neoproterozoic to Ordovician Karacontinental-margin turbidite terrane. The superterrane is un-derstood to be a rift fragment of the North Asian Craton thatwas reaccreted in the Jurassic.

The Archean to Jurassic Kolyma-Omolon superterrane(KOM) consists of a tectonic collage of cratonal, passivecontinental margin, island arc, ophiolite terranes. The cra-tonal and passive continental core of the superterrane wasrifted from the North Asian Craton and Margin in Late De-vonian or Early Carboniferous. After subsequent buildingof overlying island arcs, the superterrane was reaccreted tothe North Asian Craton Margin in the Late Jurassic with for-mation of the collisional granites of the Main and Northerngranite belts.



5.3 Tectonic collages between North Asian andSino-Korean Cratons

Between the North Asian and Sino-Korean Cratons are a se-ries of accreted tectonic collages composed primarily of Pa-leozoic island arcs and tectonically-linked subduction zones.These tectonic collages were accreted successively fromnorth to south during successive closures of the Paleo-Asian,Solon, and Mongol-Okhotsk Oceans. Most of the tectoniccollages contain one or more island arcs and tectonically-linked subduction zones. Because of successive terrane ac-cretions from north to south, the ages of collages generallyyoung from north to south. However, this pattern is locallyinterrupted because some collages or parts of collages wereinterspersed because of subsequent strike-slip faulting.

The tectonic collages between the North Asian and Sino-Korean Cratons are as follows.

(1) The Circum-Siberia collage (CS) (Paleoproterozoicand Mesoproterozoic age and accreted in Neoproterozoic)consists of the Baikal-Muya island arc, the Near YeniseyRidge island arc, and the Zavhan continental-margin arc,all of Neoproterozoic age, and small fragments of cratonaland metamorphic terranes of Archean and Proterozoic age.The three separate Neoproterozoic island arc systems formedsouth (present-day coordinates) of the North Asian Cratonand Margin.

(2) The Yenisey-Transbaikal collage (YT) (Vendian to De-vonian age and accreted in Vendian to Early Ordovician) con-sists of the Vendian to Middle Cambrian Kuznetsk-Tannuola,Dzhida-Lake island arc terranes, tectonically-linked back-arc basins, and now tectonically-eroded subduction zone ter-ranes. The collage contains a linear array of island arcsystems that formed south (present-day coordinates) of theNorth Asian Craton and Margin and previously accreted ter-ranes.

(3) The Altai collage (AL) (Vendian to Ordovician age andaccreted in Late Silurian) consists of the Vendian to EarlyOrdovician Salair island arc and various fragments of arc-related turbidite terranes, subduction zone terranes, meta-morphic terranes derived from arc-related units, thick Cam-brian and Ordovician overlap turbidite units that formed ona continental slope and rise, and fragments of originally-adjacent oceanic terranes. The collage is an island arc sys-tem that was active near the southwest margin (present-daycoordinates) of the North Asian Craton and Margin andpreviously-accreted terranes.

(4) The Wundurmiao collage (WD) (Mesoproterozoic toSilurian age and accreted in Late Silurian) consists of theLate Ordovician to Silurian Laoling island arc terrane, theMesoproterozoic to Middle Ordovician Wundurmiao sub-duction zone terrane, and the Neoproterozoic Seluohe sub-duction zone terrane. The collage contains the Laoling islandarc system which formed near the Sino-Korean Craton. Boththe island arc system and craton were widely separated fromNorth Asian Craton in the Early Paleozoic.

(5) The Atasbogd collage (AB) (Ordovician to Per-mian age and accreted in Late Carboniferous or Early Per-mian) consists of: the Ordovician to Permian Waizunger-Baaran terrane, the Devonian to Carboniferous Beitianshan-Atasbogd terrane, and the Paleoproterozoic to PermianTsagaan Uul-Guoershan continental-margin arc terrane. Thecollage was a southwest continuation (present-day coordi-nates) of the South Mongolia-Khingan island arc that formedsouthwest and west (present-day coordinates) of the NorthAsian Craton and Margin and previously accreted terranes.The Atasbogd collage was initially separated from the NorthAsian Craton by a large back-arc basin.

(6) The South Mongolia-Khingan collage (SM) (Ordovi-cian to Carboniferous age and accreted in Late Carboniferousor Early Permian) consists of the South Mongolia-Khinganarc and tectonically-linked subduction zone terranes. Thecollage was a major island-arc system that formed southwestand west (present-day coordinates) of the North Asian Cra-ton and Margin and previously accreted terranes. The collagewas separated from the North Asian Craton by a large back-arc basin.

(7) The West Siberian collage (WS) (Ordovician to Car-boniferous age and accreted in Late Carboniferous or EarlyPermian) consists of the Late Silurian to Early CarboniferousRudny Altai island arc, and the tectonically-linked Ordovi-cian to Early Carboniferous Kalba-Narim subduction zoneterrane. The collage is a northwest continuation (present-daycoordinates) of the South Mongolia-Khingan collage.

(8) The Mongol-Okhotsk collage (MO) (Devonian toLate Jurassic age and accreted in Late Paleozoic to EarlyMesozoic) consists mainly of the Permian to Jurassic Se-lenga, Late Carboniferous and Early Permian Hangay, andUda-Murgal and Stanovoy continental-margin arcs. Thesearcs are composed of continental-margin igneous over-lap assemblages, continental-margin turbidite terranes, andtectonically-linked, outboard subduction zone terranes. Thearcs overlap the southern margin of the North Asian Cratonand Margin, and previously-accreted terranes. The collageformed during long-lived closure of the Mongol-OkhotskOcean with oblique subduction of terranes beneath of south-ern North Asian Craton Margin and previously-accreted ter-ranes.

(9) The Solon collage (SL) (Carboniferous to Permianage and accreted in Late Paleozoic to Early Mesozoic) con-sists of several subduction zone terranes: (1) Carbonifer-ous and Early Permian North Margin terrane; (2) Late Car-boniferous to Permian Solon terrane; (3) Devonian Imjin-gang terrane; (4) Paleozoic Ogcheon terrane; and (5) Sil-urian through Permian Sangun-Hidagaien-Kurosegawa ter-rane. Parts of the collage were fragments of the SolonOcean plate that were subducted to form the South Mon-golian, Lugyngol, Gobi-Khankaisk-Daxing’anling, and Jiheicontinental-margin arcs. Other parts of the collage are frag-ments of the Solon Ocean plate that were subducted to form



the North Margin continental-margin arc on the Sino-KoreanCraton.

5.4 Tectonic collages east of North Asian andSino-Korean Cratons

To the east of the North Asian and Sino-Korean Cratonsare a series of tectonic collages that were successively ac-creted from west to east (older to younger) during closuresof parts of the Ancestral Pacific and modern Pacific Oceans,and older oceans in the region. Because of successive accre-tions from west to east, the ages of collages generally youngfrom west to east. However, this pattern is locally disruptedbecause some collages have been tectonically disrupted andinterspersed by subsequent strike-slip faulting

Except for the Verkhoyansk-Kolyma and Chukotka col-lages, the other tectonic collages contain one or more islandarcs or continental-margin arcs and tectonically-linked sub-duction zones. The tectonic collages that occur east of theNorth Asian and Sino-Korean Cratons are the following.

(1) The Verkhoyansk-Kolyma collage (VK) (Late Paleo-zoic to Early Jurassic age and accreted in Late Jurassic toEarly Early Cretaceous) consists of a deformed passive con-tinental margin, accreted ophiolites, and subduction zone andformed during accretion of the outboard Kolyma-Omolon su-perterrane.

(2) The Chukotka collage (CH) (Paleozoic to Triassic ageand accreted in Late Jurassic to Early Cretaceous) consistsof passive continental-margin terranes that formed along thelong-lived Neoproterozoic to Early Mesozoic North Amer-ican Continental Margin. After subsequent rifting of theNorth American Craton Margin in the Late Jurassic andEarly Cretaceous and translation, the collage was accreted tothe northern Verkhoyansk-Kolyma collage in the Late Creta-ceous.

(3) The South Anyui collage (SA) (Permian to Early Juras-sic age and accreted in Late Cretaceous) consists of the Oloyisland arc and tectonically-linked subduction zone terranes.

(4) The Penzhina-Anadyr collage (PA) (Late Jurassic toEarly Cretaceous age and accreted in Late Cretaceous) con-sists of the Murgal island arc terrane and tectonically-linkedsubduction zone terranes to the east. The collage rimsthe eastern Kolyma-Omolon superterrane and Verkhoyansk-Kolyma collage. The collage is also linked to the Udacontinental-margin arc.

(5) The Badzhal collage (BD) (Triassic to Early Creta-ceous age and accreted in Late Cretaceous) consists of theUmlekan continental-margin arc and tectonically-linked sub-duction zone terranes to the east with Tethyan fauna.

(6) Honshu-Sikhote-Alin collage (HS) (Jurassic and EarlyCretaceous age and accreted in Cretaceous). This collageconsists of fragments of island arc, continental-margin tur-bidite (flysch), and subduction zone terranes. The collageformed along a transform continental margin.

(7) The Koryak collage (KOR) (Late Triassic to Creta-ceous age and accreted in Late Cretaceous) consists of theLate Jurassic and Early Cretaceous Manitskiy island arc andtectonically-linked subduction zone terranes to the east.

(8) The Sakhalin-Hokkaido collage (SK) (Cretaceousage and accreted in Eocene) consists of the Late Creta-ceous flysch terranes of Sakhalin and Hokkaido Islands,and tectonically-linked subduction zone terranes to the east.The collage formed a continental-margin fore-arc basin andtectonically-linked subduction zone terranes that are associ-ated with the East Sikhote-Alin continental-margin arc.

(9) The West Kamchatka collage (WK) (Mid-Cretaceousto Early Tertiary age and accreted in Early Cenozoic) con-sists of Late Paleozoic to Cretaceous subduction zone ter-ranes in the Russian Northeast. The collage was tectonicallylinked to Okhotsk-Chukotka continental-margin arc.

(10) The East Sakhalin collage (ES) (Late Cretaceous toEarly Tertiary age and accreted in Early Tertiary) consistsof the Late Cretaceous to Middle Eocene Terpeniy-Tokoro-Nemuro-Shmidt island arc and tectonically-linked subduc-tion zone terranes.

(11) The Olyutorka-Kamchatka collage (OK) (Late Cre-taceous and Paleocene age and accreted in Early Cenozoic)consists of the Olyutorka island arc and tectonically-linkedsubduction zone terranes to the east.

(12) The East Kamchatka Peninsula collage (EP) (mainlyPaleocene age and accreted in Pliocene) consists of the Kro-notskiy island arc and associated ophiolite.

5.5 Carboniferous and Permian overlap continental-margin arcs occurring south of North Asia Cratonand on Sino-Korean Craton

Several major overlap continental-margin arcs occur only onpreviously-accreted terranes south of the North Asian Cra-ton and on the Sino-Korean Craton. These arcs are related tosubduction of the Late Paleozoic and Early Mesozoic SolonOcean plate beneath the North Asian and Sino-Korean Cra-tons. This ocean occurred (in present-day geographic coordi-nates) between the Argun-Idermeg superterrane to the northand the Sino-Korean Craton to the south. The arcs are de-scribed progressing from older to younger.

(1) The Altay arc (at) (Devonian and Early Carboniferous)occurs on the Altay and Yenisey-Transbaikal collages. Thearc formed along an active continental margin in an obliquesubduction zone environment.

(2) The Gobi-Khankaisk-Daxing’anling arc (gh) (Per-mian) occurs on the Argun-Idermeg superterrane, SouthMongolian collage, and Solon collage. The arc formed dur-ing subduction of the northern part of Solon Ocean plateunder the southern margin (present-day coordinates) of theArgun-Idermeg superterrane.

(3) The South Mongolian arc (sm) (Middle Carbonifer-ous through Triassic) overlies and intrudes the South Mon-golian collage and Atasbogd collage. The arc formed during



subduction of the northern part of Solon Ocean plate underthe Argun-Idermeg superterrane.

(4) The Lugyngol arc (lg) (Permian) occurs on the SouthMongolian and Solon collages. The arc is formed duringsubduction of the northern part of Solon Ocean plate underthe southern margin (present-day coordinates) of the Argun-Idermeg superterrane.

(5) The Jihei arc (ji) (Permian) occurs on the SouthMongolia-Khingan collage. The arc intrudes the Bureya-Jiamusi superterrane and South Mongolia-Khingan collageand formed during subduction of the northern part of SolonOcean plate under the southern margin (present-day coor-dinates) of the Bureya-Jiamusi supterterrane and adjacentunits.

(6) The North Margin arc (nm) (Late Carboniferous toPermian) occurs on the northeastern margin (present-day co-ordinates) of Sino-Korean Craton. The arc formed duringsubduction of the southern part of Solon Ocean plate underthe northeastern margin (present-day coordinates) of Sino-Korean Craton.

5.6 Devonian to Early Cretaceous overlap continental-margin arcs occurring along Southeastern Marginof the North Asian Craton and adjacent accretedterranes

Several major overlap continental-margin arcs occur alongthe southeastern margin of the North Asian Craton or on ad-jacent accreted terranes. The arcs are related to subductionof the Late Paleozoic and early Mongol-Okhotsk Ocean platebeneath the North Asian Craton and Margin. This ocean oc-curred between the North Asian Craton to the north and theArgun-Idermeg superterrane to the south (present-day coor-dinates).

(1) The Norovlin arc (nr) (Devonian to Early Carbonifer-ous) occurs on the Argun-Idermeg superterrane (Amur mi-crocontinent – Argunsky and Idermeg passive continental-margin terranes). The arc is formed during subduction of theMongol-Okhotsk Ocean plate beneath northern margin (inpresent-day geographic coordinates) of the Argun-Idemegsuperterrane (Amur microcontinent).

(2) The Hangay arc (ha) (Late Carboniferous to EarlyPermian) occurs on the Yenisey-Transbaikal collage andMongol-Okhotsk collage. The arc formed during subductionof the northern part of Mongol-Okhotsk Ocean plate underthe North Asian Craton Margin and previously-accreted ter-ranes.

(3) The Selenga arc (se) (Permian to Jurassic) overlies andintrudes the Yenisey-Transbaikal collage and Tuva-Mongoliasuperterrane. The arc formed during oblique subduction ofthe Mongol-Okhotsk Ocean plate under the North Asian Cra-ton Margin and previously-accreted terranes.

(4) The Uda-Murgal and Stanovoy arcs (us) (Jurassic toEarly Cretaceous) occur on the southern margin of the North

Asian Craton. The arcs formed during final stage of subduc-tion of the Mongol-Okhotsk Ocean plate.

5.7 Jurassic and Early Cretaceous overlap island arcsoccurring on or adjacent to Kolyma-Omolonsuperterrane

The major overlap island arcs occurring on the Kolyma-Omolon superterrane are the Late Jurassic to Early Creta-ceous Uyandina-Yasachnaya island arc and the Late JurassicOloy island arc.

(1) The Uyandina-Yasachnaya arc (uy) (Late Jurassic toEarly Cretaceous) occurs along the margin of the Kolyma-Omolon superterrane. The arc formed during subduction ofthe Oimyakon Ocean plate between the North Asian CratonMargin and the Kolyma-Omolon superterrane. Remnants ofthe Oimyakon oceanic crust are preserved in small obductedophiolites along the western margin of superterrane. Thisocean occurred between the Verkhoyansk (North Asian) Cra-ton Margin to the southwest and the Kolyma-Omolon to thenortheast (present-day coordinates).

(2) The Oloy arc (ol) (Late Jurassic) occurs along the mar-gin of the Kolyma-Omolon superterrane. The arc formed onthe Kolyma-Omolon superterrane during subduction of theSouth Anyui Ocean plate beneath the superterrane to formthe South Anyui subduction-zone terrane. This ocean formednorth of the Kolyma-Omolon superterrane (present-day coor-dinates).

5.8 Jurassic through Early Tertiary overlapcontinental-margin arcs and granite beltsoccurring along eastern margin of Northern Asia

A series of Jurassic through Early Tertiary overlapcontinental-margin arcs and granite belts occur along theeastern margin of the North Asian and Sino-Korean Cratonsand outboard accreted terranes to the east. From older toyounger, the arcs and belts are as follows.

(1) The Umlekan-Ogodzhin arc (uo) (Jurassic and Creta-ceous) occurs along the margin of the Kolyma-Omkolon su-perterrane. The arc formed during subduction of the Ances-tral Pacific Ocean plate to form the Badzhal and Nadanhadaterranes in the Badzhal collage.

(2) The South Verkhoyansk Granite Belt (sv) (Late Juras-sic to Mid-Cretaceous) occurs in the Central Russian FarEast. The belt extends longitudinally along the central partof the South Verkhoyansk synclinorium in the Verkoyansk(North Asian) Craton Margin. The belt formed during theaccretion of the outboard Okhotsk terrane.

(3) The Main Granite Belt (ma) (Late Jurassic) occursalong the adjacent margins of the North Asian Craton Marginand Kolyma-Omolon superterrane. The belt formed duringand immediately after the collision of the Kolyma-Omolonsuperterrane with the North-Asian Craton Margin.



(4) The Transverse Granite Belt (tr) (Early Cretaceous) ra-diates outwards from the southwestern bend of the Kolyma-Omolon superterrane. The belt formed during the late stageof accretion of Kolyma-Omolon superterrane.

(5) The Northern Granite Belt (nb) (Early Cretaceous, 138to 120 Ma) occurs along northwestern margin of the Kolyma-Omolon superterrane. The belt formed during the subductionof oceanic crust during a closure of a small oceanic basin dur-ing late stage of accretion of Kolyma-Omolon superterrane.

(6) The Khingan-Okhotsk arc (ko) (Early and Mid-Cretaceous) occurs in the Russian Southeast and consistsof the Khingan-Okhotsk volcanic-plutonic belt. The arcwas tectonically paired to the Early Cretaceous Zhuravlevsk-Amur River and Kiselevka-Manoma subduction-zone ter-ranes that are both part of the Honshu-Sikhote-Alin collage.

(7) The Okhotsk-Chukotka arc (oc) (Late Cretaceous toEarly Tertiary) occurs along the eastern margin of the Centraland Northern Russian Far East. The arc formed during sub-duction of the Ancestral Pacific Ocean plate and formationof the West Kamchatka, Ekonay, and Yanranay subductionzone terranes.

(8) The East Sikhote-Alin arc (ea) (Late Cretaceous toEarly Tertiary) occurs along the margin of the Southern Rus-sian Far East. The arc formed during subduction of theAncestral Pacific Ocean plate with formation of the olderpart of the Hidaka subduction zone, the younger part of theAniva subduction-zone terrane, and the Nabilsky, and Tokorosubduction-zone terranes.

5.9 Active overlap continental-margin arcsoccurring along eastern margin of Northern Asia

Three active overlap continental-margin arcs occur along theeastern margin of the North Asian and Sino-Korean Cratonsand outboard accreted terranes to the east.

(1) The Izu-Bonin arc (ib) (Miocene through Present) oc-curs south of Southern Japan and consists of a volcanic arccomposed chiefly of basalt to rhyolite, associated volcani-clastic rock, and intercalated hemipelagic mudstone. The arcis formed during subduction of the Philippine Sea Plate withformation of the Nankai subduction zone. (2) The Japan arc(ja) (Miocene through Present) occurs along the Japanese Is-lands and consists of extensive Quaternary volcanic and as-sociated rock. The arc is formed during subduction of thePacific Ocean and Philippine Sea Plates with formation ofthe Japan Trench and Nankai subduction zones.

(3) The Kuril-Kamchatka arc (kk) (Miocene throughPresent) occurs along Kamchatka Peninsula and Kuril Is-lands and consists of the Pliocene to Quaternary CentralKamchatka volcanic belt, Central Kamchatka volcanic andsedimentary basin, and the East Kamchatka volcanic belt.The arc is formed during subduction of the Pacific OceanPlate and formation of the Japan Trench subduction zone.

5.10 Transpressional arcs (Devonian throughCretaceous)

Three major transpressional arcs occur along the margins ofthe North Asian Craton and previously accreted terranes tothe south. The arc formations are associated with strike-slipfaulting that is sometimes associated with local compressionand extension.

(1) The South Siberian arc (ss) (Early Devonian) occursin Southern Siberia. The arc is formed along the south-ern margin of the North Asian Craton and Craton Marginduring Early Devonian rifting that successively evolved intoa continental-margin transform margin and subsequently intoa convergent margin.

(2) The Mongol-Transbaikal arc (mt) (Late Triassic toEarly Cretaceous) occurs in Northern Mongolia and South-ern Siberia. The arc is formed during strike-slip faulting andrifting along the Mongol-Okhotsk fault during and after thefinal closure of the Mongol-Okhotsk Ocean.

(3) The Trans-Baikal-Daxinganling arc (tr) (Middle Juras-sic through Early Cretaceous) occurs in Southern Siberia,Mongolia, Northeastern China. The arc formed duringstrike-slip faulting and rifting along the Mongol-Okhotskfault during, and after the final closure of the Mongol-Okhotsk Ocean.

6 Conclusions

Compiled with the methodology described herein, the North-east Asia summary geodynamics map (Fig. 2) illustrates thepower of a regional map and provides an example for fu-ture regional studies of large parts of the earth’s continentalcrust. This map greatly benefits the interpretation of originsof major rock units, major structures, and mineral and hydro-carbon resources, and provides important guidelines for newresearch.

Appendix A

Description of map units for Northeast Asiasummary geodynamics map

A1 Introduction

The major map units on the Northeast Asia summary geo-dynamics map are cratons, craton margins, cratonal ter-ranes, superterranes, tectonic collages (Archean to Protero-zoic, Vendian to Cretaceous, Late Cretaceous and Cenozoic),overlapping continental-margin arcs (Devonian to Early Ter-tiary), transform continental-margin arcs (Devonian to EarlyCretaceous), active arcs (Miocene through Present), and ac-tive subduction zones (Miocene through Present). Units arelisted in order of map unit abbreviations within each ma-jor unit. Additional information about the map units canbe found in Greninger et al. (1999), Nokleberg et al. (1994,1997c, 2000, 2004), and Naumova et al. (2006).



A2 Cratons

NAC – North Asian Craton (Archean and Proterozoic). Con-sists of Archean and Proterozoic metamorphic basement,and non-deformed, flat-laying platform cover consisting ofLate Precambrian, Paleozoic, and Mesozoic sedimentary andvolcanic rock. Cover locally ranges up to 14 000 m thick.Metamorphic basement exposed in the Aldan-Stanovoy andAnabar shields located near southern and northern cratonmargins, respectively. Along the southwestern margin of thecraton is a narrow band of basement rocks named the Near-Sayan Uplift. Within the Aldan-Stanovoy and Anabar shieldsand the Near-Sayan Uplift are several terranes composed ofEarly Precambrian crystalline rocks of varying compositionand structural style. Four sequences comprise the platformcover: (1) Vendian and Early Paleozoic; (2) Middle Paleo-zoic; (3) Late Paleozoic; and (4) Mesozoic. Each stage ischaracterized by a unique structural style and unique suite ofsedimentary and magmatic rocks. The sequences are sepa-rated from each other by regional discontinuities and uncon-formities that are related to major tectonic events.

SKC – Sino-Korean Craton (Archean and Proterozoic).Consists of several major terranes and younger overlapunits in Northern China and in the northern Korean Penin-sula. The Archean and Proterozoic metamorphic base-ment is composed of various major terranes and firstoverlap units: (1) Paleoproterozoic Alashan granulite-paragneiss terrane in Northwestern China; (2) Archean Er-duosi Granulite-paragneiss terrane in North-Central China;(3) Archean Yinshan granite-greenstone terrane and firstoverlapped Zhangbei-Bayan Obo-Langshan metasedimen-tary and metavolcanic rocks (Paleo-Mesoproterozoic) inNorth-Central China; (4) Archean Jilin-Liaoning-East Shan-dong tonalite-trondhjemite-gneiss terrane and overlapped,metamorphosed and deformed rocks of East Shandong-EastLiaoning-East Jilin rift or foreland basin (Paleoproterozoic)in Northeastern China; (5) Archean West Liaoning-Hebei-Shanxi granulite-orthogneiss terrane and overlapped, meta-morphosed and deformed rocks of Hutuo rift basin (Pale-oproterozoic) in Northern China; (6) Archean to Paleopro-terozoic Machollyong granulite-paragneiss terrane in North-ern Korean Peninsula; and (7) Archean Rangnim granulite-paragneiss terrane in Northern Korean Peninsula. Overlapunits are extensive Proterozoic and Paleozoic continental-margin sedimentary rock and lesser volcanic rock; and ex-tensive Mesozoic and Cenozoic marine and terriginous sedi-mentary rock units, and volcanic and plutonic arc rock units.

A3 Craton margins

BP – Baikal-Patom Craton Margin (Riphean to Cambrianand older basement). Consists of a fault-bounded basin con-taining Riphean carbonate and terrigenous sedimentary rock,and Younger Vendian and Cambrian sedimentary rock thatdiscordantly overly a fragment of pre-Riphean basement of

the North Asian Craton. Local detritus suggests derivationfrom ophiolite and island arc complexes of the Bakal-Muyaterrane during accretion to the craton. Local greenschistand amphibolite facies regional metamorphism with isotopicages of about 800 Ma.

EA – East Angara Craton Margin (Riphean and older base-ment). Consists of Late Riphean terrigenous-carbonate sed-imentary rock (sandstone, siltstone, mudstone with interlay-ered dolomite and limestone) that overlie a fragment of theNorth Asia Craton. Metamorphosed up to greenschist facies.Unconformably overlapped by Late Riphean and Vendianmolasse and Vendian and Cambrian dolomite and limestone.

ST – South Taimyr Craton Margin (Ordovician to Juras-sic). Consists chiefly of a thick wedge of craton margindeposits and deep basin deposits ranging up to 20 000 mthick. Composed chiefly of Ordovician to Jurassic clasticrock, shallow-marine terrigenous and carbonate rock, andmafic volcanic and volcaniclastic rock. Late Carboniferousand Permian sedimentary rocks contain extensive sills anddikes of the Early Triassic trap subalkaline and alkaline di-abase. The terrane is tectonically detached from the crys-talline basement of the North Asian Craton but was subse-quently accreted back onto the craton.

VR – Verkhoyansk (North Asian) Craton Margin (Devo-nian to Jurassic). Consists chiefly of a thick wedge of cra-tonal margin deposits ranging up to 20 000 m thick. Ma-jor units are Carboniferous, Permian, Triassic, and Early andMiddle Jurassic clastic rock, and marine-littoral, deltaic, andshelf sedimentary rock deposited on the Verkhoyansk pas-sive continental margin of the North Asian Craton. Majorunits grade successively eastward into turbidite deposits anddeep-water black shale. Also occurring are: (1) local Mid-dle to Late Devonian and Early Carboniferous, rift-relateddeposits similar to those on the Siberian Platform; and (2)local Early Triassic and Early Jurassic alkalic basalt flows,dikes, and sills. Northern and southern parts of craton margincontain thick, Neoproterozoic and Early Paleozoic shallow-marine carbonate and clastic deposits that are finer-grainedand thicker to east. The terrane is tectonically detached fromthe passive continental margin and crystalline basement ofthe North Asian Craton.

A4 Cratonal terranes

GY – Gyenggi-Yeongnam cratonal terrane (Archean andProterozoic). Consists of two major terranes: (1) Mesopro-terozoic and Neoproterozoic and older Gyenggi granulite-paragneiss terrane in Southern Korean Peninsula; and (2)Late Archean to Paleoproterozoic Yeongnam granulite-paragneiss terrane in Southern Korean Peninsula. Locallyoverlain by extensive Paleozoic continental margin sedimen-tary rock and lesser volcanic rock; and extensive Mesozoicand Cenozoic marine and terriginous sedimentary rock units,and volcanic and plutonic arc units. The terrane is interpretedas a displaced fragment of the Sino-Korean Craton.



JA – Jiaonan cratonal terrane (Proterozoic). Consists ofa Paleoproterozoic major high pressure terrane that is a dis-placed fragment of the South China (Yangtzi) Craton. Lo-cally overlain by extensive Paleozoic continental margin sed-imentary rock and lesser volcanic rock, extensive Mesozoicand Cenozoic marine and terriginous sedimentary rock units,and volcanic and plutonic arc units.

OH – Okhotsk cratonal terrane (Archean, Proterozoic, andEarly and Middle Paleozoic). Consists chiefly of large blocksof Archean to Paleoproterozoic gneiss and schist with a U-Pb zircon age of 3.7 Ga. Overlain by: (1) gently-dipping,shallow-marine Middle and Neoproterozoic clastic and car-bonate rock; (2) Early Cambrian limestone, marl, and sand-stone; (3) Early Ordovician conglomerate, limestone, marl,and sandstone; and (4) unconformably overlying Middle De-vonian limestone, sandstone, shale, and conglomerate, andLate Devonian rhyolite, ignimbrite, andesite, dacite, and tuffthat are interlayered with nonmarine sandstone, siltstone, andconglomerate. Overlying units are Carboniferous to LateJurassic nonmarine and rare marine clastic rock. The terraneis interpreted as a fragment of the North Asian Craton andCraton margin that was rifted in the Late Devonian or EarlyCarboniferous and accreted to the Eastern Asia continentalmargin in the Late Jurassic.

A5 Superterranes

AR – Argun-Idermeg superterrane (Proterozoic to Cambrian;Timing of accretion – Late Neoproterozoic to Cambrian).Consists of: (1) Paleoproterozoic to Late Paleozoic Argun-sky metamorphosed passive continental margin terrane (AR)(Eastern Mongolia, Northeastern China, Transbaikalia); (2)Proterozoic to Cambrian Idermeg metamorphosed passivecontinental margin terrane (ID) (Eastern Mongolia); and (3)West Stanovoy metamorphosed continental margin terrane(WST) (Archean through Neoproterozoic) (Transbaikalia,Mongolia). The superterrane metamorphosed at greenschistto upper amphibolite to granulite facies.

BJ – Bureya-Jiamusi supterterrane (Proterozoic to Per-mian; Timing of accretion – Early Paleozoic). Consists ofan Early Paleozoic collage with fragments of the follow-ing metamorphic, continental-margin arc, subduction zone,passive continental-margin and island arc terranes: (1) Neo-proterozoic to Triassic Bureya terrane (BU) (the SouthernRussian Far East); (2) Neoproterozoic and older and EarlyCambrian Jiamusi terrane (JI) (Northeastern China); (3) Pro-terozoic Matveevka terrane (MT) (the Southern Russian FarEast); (4) Proterozoic Nakhimovka terrane (NK) (the South-ern Russian Far East); (5) Silurian to Permian(?) SouthKitakami metamorphosed island arc terrane (SK) (NorthernHonshu Island, Japan); and (6) Late Carboniferous and Per-mian Laoyeling-Grodekov island arc terrane (LG) (North-eastern China, the Southern Russian Far East); (7) Cambrianthrough Permian passive continental-margin Voznesenka ter-rane (the Southern Russian Far East); (8) Cambrian(?) and

Ordovician(?) Sergeevka island arc terrane (SG) (the South-ern Russian Far East); (9) Neoproterozoic through Devo-nian Zhangguangcailing continental-margin arc terrane (ZN)(Northeastern China); (10) Ordovician and Silurian Hei-longjiang subduction zone, type B terrane (HE) (Northeast-ern China); (11) Archean through Middle Triassic Urmi pas-sive continental margin terrane (UR) (Northeast China, theSouthern Russian Far East); and (12) Late Carboniferous andPermian Tumangang island arc terrane (TB) (Korea). Theseterranes are derived from a series of Late Precambrian vol-canic units, and Late Precambrian to Ordovician shallow ma-rine clastic and carbonate rock. Local amphibolite and gran-ulite facies metamorphism of Early and Middle Ordovicianage (480 to 500 Ma). Units intruded by Cambrian and Or-dovician granitoids and unconformably overlain by Devo-nian rock.

The superterrane is interpreted as a fragment of Gondwanathat was accreted to the Sino-Korean Craton in the Late Per-mian and accreted to the North Asian Craton in the LateJurassic during closure of the Mongol-Okhotsk ocean. Thesuperterrane may be a fragment of the Yenisey-Transbaikalorogenic belt that also contains Early Paleozoic granulitefacies metamorphism and Cambrian and Ordovician grani-toids.

KR – Kara superterrane (Proterozoic to Ordovician; Tim-ing of accretion – Early Paleozoic(?). Consists of a LateNeoproterozoic to Ordovician Kara continental-margin tur-bidite terrane (KR) (northern part of Taimyr Peninsula).The terrane contains mainly Late Riphean turbidite unitsmetamorphosed up to amphibolite facies. Uppermost tur-bidites contain Cambrian and Early Ordovician fauna. Tur-bidites are unconformably overlain by Ordovician-Devonianlittoral-marine and continental sedimentary rock. The supert-errane accreted to the North Asian Craton (with genesis of)generating Middle Permian two-mica and biotite-amphibolegranite and granodiorite (with U-Pb, Rb-Sr, and incrementalArgon isotopic ages of 264 to 252 Ma). Granitoids comprisean extensive belt that obliquely cuts the superterrane and themargin of the Late Riphean Circum-Siberian collage. Thesuperterrane is interpreted as a rifted fragment of the NorthAsian Craton that was reaccreted in the Jurassic.

KOM – Kolyma-Omolon superterrane (Archean to Juras-sic; Timing of accretion – Late Jurassic). Consists of acollage of cratonal, passive continental-margin, island arc,and ophiolite terranes. Major terranes are: Alazeya (islandarc), Aluchin (subduction zone), Argatass (turbidite), Bery-ozovka (turbidite), Kenkel’da (subduction zone), Khetachan(island arc), Munilkan (oceanic), including various smallophiolite fragments (Garbyn’ya, Indigirka, Kybytygas, Mu-nilkan, Uyandina, Uvyazka), Nagondzha (turbidite), Oloy(island arc), Omolon (cratonal), Omulevka (continental mar-gin), Prikolyma (continental margin), Uyandina (island arc),and Yarkvaam (island arc). The superterrane formed dur-ing accretion of terranes of cratonal, continental (Omulevka,Prikolyma, and Omolon terranes), and oceanic affinity to the



Alazeya island arc. Obduction of oceanic crust and forma-tion of small ophiolite fragments of the Munilkan terranewere associated with this process. The superterrane is uncon-formably overlain by the Late Jurassic Uyandina-Yasachnayasuperterrane marginal arc (uy) under which the Oimyakonocean basin was subducted during migration of superter-rane towards the North Asia (Verkhoyansk) Craton Margin.The superterrane was accreted to the northeast Verkhoyansk(North Asian) Craton Margin in the Late Jurassic to EarlyCretaceous. The accretion resulted in formation of colli-sional granites of the Main (mb) (Late Jurassic) and Northern(nb) (Early Cretaceous) granite belts (Yakutia).

TM – Tuva-Mongolia superterrane (Late Riphean andolder; Timing of accretion – Late Neoproterozoic). Con-sists of many fragments of the: (1) Archean and Paleo-proterozoic Gargan cratonal terrane (GG) (North Huvsgol,Mongolia, Eastern Sayan); (2) Proterozoic Sangilen passivecontinental-margin terrane (SA) (Southwest Siberia, Mon-golia); (3) Neoproterozoic and older Baydrag cratonal ter-rane (BY) (Northwest Mongolia); and (4) Late Archean(?)and Paleoproterozoic(?) Muya metamorphic terrane (MS)(Transbaikalia). The superterrane also includes the variousterranes of the Baikal-Muya island arc system (Baikal-Muya,Barguzin, Dibinsky, Hug, Ilchir, Kuvai, Olokit-Delunuran,and Sarkhoy terranes) that were amalgamated to form theTuva-Mongolian microcontinent. The superterrane is un-conformably overlain by Vendian and Cambrian sedimentaryand volcanic rock.

A6 Tectonic collages accreted between North Asian andSino-Korean Cratons (Proterozoic to EarlyMesozoic accretions

AB – Atasbogd collage (Ordovician to Permian; Timing ofaccretion – Late Carboniferous or Early Permian). Con-sists of: (1) Ordovician to Permian Waizunger-Baaran ter-rane; (2) Devonian to Carboniferous Beitianshan-Atasbogdterrane; and (3) Paleoproterozoic to Permian Tsagaan Uul-Guoershan continental-margin arc terrane; The collage is asouthwest continuation (present-day geographic coordinates)of the South Mongolia-Khingan island arc. Units in the col-lage are unconformably overlain by Permian volcanogenicand coal-bearing units. The collages comprising the arcswere accreted to the southern margin of the Siberian con-tinent in the Late Carboniferous or Early Permian (320 to300 Ma).

AL – Altai collage (Vendian to Ordovician; Timing ofaccretion – Late Silurian). Consists of Vendian to EarlyOrdovician Salair island arc and various fragments of arc-related turbidite, and subduction zone terranes, metamor-phic terranes derived from arc-related units, and thick Cam-brian and Ordovician overlap turbidite units formed on con-tinental slope and rise, and fragments of originally-adjacentoceanic terranes are the major units in the collage. Thecollage is an island arc system that lay near the southwest

margin (present-day coordinates) of the North Asian Cratonand Margin and previously-accreted terranes. These units oc-cur in the Gorny Altai, West Sayan, Central and Northwest-ern Mongolia, and adjacent regions of Northern China.

The Salair island arc (Vendian-Early Ordovician) is pre-served in various fragments in Southwestern Siberia in the:(1) Early Cambrian to Early Ordovician Salair island arcterrane; (2) the Cambrian Ulus-Cherga island arc terrane;and (3) Early and Middle Cambrian Sugash terrane. Thetectonically-linked subduction zone and oceanic crust unitsare the: (1) Vendian and Early Cambrian Alambai subductionzone terrane; and (2) Late Neoproterozoic to Early CambrianBaratal subduction zone terrane.

The arc is also preserved in various fragments in the fol-lowing metamorphic (arc-related) terranes: Middle Silurianand older Angurep terrane; Late Permian and older Be-lokurikha terrane; and Mesoproterozoic and NeoproterozoicQinghe-Tsel terrane.

The arc is also preserved in various fragments of the fol-lowing continental-margin turbidite terranes: Early to LatePaleozoic Anui-Chuya terrane; Precambrian and Cambrianto Devonian Altai terrane; Cambrian to Devonian Charyshterrane; Late Neoproterozoic to Devonian West Sayan ter-rane; and Neoproterozoic through Silurian Hovd terrane.

The arc is tectonically linked to various fragments in thefollowing subduction zone terranes: Early Paleozoic or olderKaitanak terrane; Middle Devonian or older Maralikha ter-rane; Late Neoproterozoic through Early Cambrian Terektaterrane; and Late Neoproterozoic to Early Cambrian Baratalterrane.

The arc is also tectonically linked to various fragmentsof the following oceanic terranes: Late Neoproterozoic andEarly Cambrian Mogen-Buren terrane; Late Cambrian andEarly Ordovician Zasurin terrane; and Late Neoproterozoicand Early Cambrian Saratan terrane.

The timing of the accretion of the collage to the Siberiancontinent is constrained by an angular unconformity at thebase of the Upper Silurian or Devonian units and by oro-genic granitoid magmatism of Early Devonian or older (pre-Emsian) age (about 435–415 Ma).

CS – Circum-Siberia collage (Proterozoic; Timing of ac-cretion – Neoproterozoic). The collage consists of theBaikal-Muya island arc, the Near Yenisey Ridge island arc,the Zavhan continental-margin arc, Central and West An-gara passive continental-margin terranes, all of Neoprotero-zoic age, and small fragments of cratonal and metamorphicterranes of Archean and Proterozoic age. The collage con-sists of three separate Neoproterozoic island arc systemsthat formed south (present-day geographic coordinates) ofthe North Asian Craton and Margin and previously accretedterranes. The collage is unconformably overlain by Ven-dian and Cambrian sedimentary rock units, similar to co-eval rocks of the Siberian platform, but much thicker andcontaining more marine units. Accretion of the collage to



the North Asian Craton and Craton Margin occurred in theLate Neoproterozoic.

Baikal-Muya island arc (Neoproterozoic). Preserved invarious fragments in the: (1) Paleoproterozoic to Early Cam-brian Hamar-Davaa metamorphic terrane (metamorphosedforearc prism); (2) Neoproterozoic Baikal-Muya island arcterrane; (3) Late Neoproterozoic Barguzin metamorphic ter-rane (metamorphosed forearc prism); and (4) Late Neo-proterozoic Sarkhoy island arc terrane. The tectonically-linked subduction zone or subduction zone units are the:(1) Paleoproterozoic to Neoproterozoic Olokit-Delunuransubduction zone terrane; (2) Neoproterozoic Hug subductionzone terrane; and (3) Neoproterozoic Kuvai subduction zoneterrane.

Near Yenisey Ridge island arc (Neoproterozoic). Pre-served in various fragments in the: (1) NeoproterozoicIsakov island arc terrane; (2) Late Neoproterozoic Predivinskisland arc terrane; and (3) Neoproterozoic Chelyuskin islandarc terrane.

Zavhan continental-margin arc (Neoproterozoic). Pre-served in various fragments in Northern Mongolia in the: (1)Late Neoproterozoic Zavhan continental-margin arc terrane;and (2) Neoproterozoic Tasuul oceanic terrane.

Cratonal and Metamorphic terranes (Archean and Protero-zoic). Consists mainly of relatively small (tens of kilometerswide) fragments preserved in the: (1) Archean and Paleopro-terozoic Gargan cratonal terrane; (2) Late Archean(?) andPaleoproterozoic(?) Muya metamorphic terrane; and (3) Pa-leoproterozoic Kan cratonal terrane. The terranes are frag-ments of the North Asian Craton and that were rifted awayduring the breakup of the Rodinia supercontinent. Thesecratonal and metamorphic terranes formed a tectonic back-stop for the accretion of the Neoproterozoic island arcs inthe Circum-Siberia collage.

MO – Mongol-Okhotsk collage (Devonian to Late Juras-sic; Timing of accretion – Late Paleozoic to Early Meso-zoic). Consists mainly of Middle to Late Paleozoic and EarlyMesozoic Selenga, Hangay, and Uda-Murgal and Stanovoycontinental-margin arcs composed of continental-margin ig-neous overlap assemblages, continental-margin turbidite ter-ranes, and tectonically-linked outboard subduction zone ter-ranes. The arcs overlap the southern margin of the NorthAsian Craton and Margin and previously-accreted terranes.

The major continental-margin arc overlap units in the col-lage are the: (1) Permian to Jurassic Selenga sedimentary-volcanic plutonic belt; (2) Late Carboniferous and Early Per-mian Hangay plutonic belt; and (3) Jurassic and Early Creta-ceous Uda-Murgal and Stanovoy granite belts; (4) Devonianto Triassic Lan continental-margin turbidite terrane; and (2)Late Triassic to Middle Jurassic Ulban continental-marginturbidite terrane.

Tectonically linked to the arc are the following subductionzone terranes: (1) Cambrian to Early Carboniferous Galamterrane (GL); (2) Silurian to Permian Tukuringra-Dzhagdy

terrane; (3) Silurian to Late Carboniferous Hangay-Dauriaterrane; and (4) Paleozoic Ononsky terrane.

The collage formed during long-lived closure of Mongol-Okhotsk Ocean with oblique subduction of terranes beneaththe southern North Asian Craton Margin and previously-accreted terranes. Closure and accretion extend from the Per-mian to the Late Jurassic (140 to 90 Ma). After closure ofthe Mongol-Okhotsk Ocean, left-lateral slip continued alongthe Mongol-Okhotsk fault that bounded the former oceanand resulted in formation of Trans-Baikalian-Daxinganlingbimodal igneous belt.

SL – Solon collage (Carboniferous to Permian; Timing ofaccretion – Late Paleozoic to Early Mesozoic). Consists offollowing subduction zone terranes: (1) Carboniferous andEarly Permian North Margin terrane; (2) Late Carboniferousto Permian Solon terrane; (3) Devonian Imjingang terrane;(4) Paleozoic Ogcheon terrane; and (5) Silurian through Per-mian Sangun-Hidagaien-Kurosegawa terrane. The terranesof the collage are fragments of Solon Ocean plate. The ter-ranes locally contain sedimentary units with mixed Tethyanand Boreal fossils.

The subduction zone terranes were derived from under-thrusting of the northern part of the Solon Ocean plateto form a continental-margin arc on the South Mongolia-Khingan collage and Argun-Idermeg superterrane (Amur mi-crocontinent composed of Agun and Idermeg passive con-tinental margin terranes). The arcs are: (1) South Mon-golian arc composed of Middle Carboniferous to Late Tri-assic South Mongolian volcanic-plutonic belt; (2) Lugyn-gol arc composed of Permian Lugyngol volcanic and sedi-mentary basin; (3) Gobi-Khankaisk-Daxing’anling arc com-posed of Permian Gobi-Khankaisk-Daxing’anling volcanic-plutonic belt; and (4) Jihei arc composed of Permian Jiheiplutonic belt.

Various subduction zone terranes were derived from un-derthrusting of the southern part of Solon Ocean plate and aretectonically linked to the North Margin continental-marginarc that formed on the Sino-Korean Craton. The arc is com-posed of the Carboniferous and Permian North Marginal Plu-tonic Belt of North China Platform.

The various terranes in the Solon collage were accretedto continental margins in the Permian to Triassic (290 to203 Ma).

SM – South Mongolia-Khingan collage (Ordovician toCarboniferous; Timing of accretion – Late Carboniferous orEarly Permian). Major unit in collage is the South Mongolia-Khingan arc and tectonically-linked subduction zone ter-ranes.

Collage consists mainly of extensive local Ordovician,Silurian, Devonian, and Mississippian island arc and tur-bidite terranes and tectonically-linked subduction zone ter-ranes. Preserved in various fragments in the: (1) Neo-proterozoic through Early Carboniferous Nora-Sukhotin-Duobaoshan island arc terrane; (2) Devonian to Carbonifer-ous Beitianshan-Atasbogd terrane; (3) Cambrian to Middle



Devonian Dongwuzhumuqin-Nuhetdavaa terrane; (4) Mid-dle Ordovician to Early Carboniferous Mandalovoo-Onorterrane; (5) Silurian to Early Carboniferous Gurvansayhanterrane; (6) Devonian and Early Carboniferous Edren ter-rane; (7) Cambrian to Devonian Govi Altai turbidite terrane;(8) Ordovician to Devonian Bayanleg subduction zone ter-rane; and (8) Devonian to Permian Hegenshan terrane. Thetectonically-linked subduction zone terranes are: (1) Ordovi-cian(?) and Devonian Zoolen terrane; and (2) DevonianMandan terrane.

The South Mongolia-Khingan island arc was separatedfrom the North Asian Craton by a large back-arc basin nowrepresented in fragments contained in the: (1) Ordovician toDevonian Bayanleg subduction zone terrane; and (2) Devo-nian Mandah subduction zone terrane. The collages com-prising the arcs were accreted to the southern margin of theSiberian continent in the Late Carboniferous or Early Per-mian (320 to 300 Ma).

WD – Wundurmiao collage (Mesoproterozoic to Silurian;Timing of accretion – Late Silurian). Consists of: (1) LateOrdovician to Silurian Laoling island arc terrane; (2) Meso-proterozoic to Middle Ordovician Wundurmiao subductionzone terrane; and (3) Neoproterozoic Seluohe subductionzone terrane. The collage consists of the Laoling islandarc system that formed near Sino-Korean Craton that waswidely separated from North Asian Craton in the Early Pa-leozoic. The collage intruded by granodiorite with a U-Pbage of 466 Ma and unconformably overlain by Silurian clas-tic rock. The collage was accreted to the Sino-Korean Cratonin the Late Silurian (435–415 Ma) along a transform conti-nental margin.

The timing of the accretion of the collage to the Siberiancontinent is constrained by an angular unconformity at thebase of the Upper Silurian or Devonian units and by oro-genic granitoid magmatism of Early Devonian or older (pre-Emsian) age (about 435–415 Ma).

WS – West Siberian collage (Ordovician to Carbonif-erous Timing of accretion – Late Carboniferous or EarlyPermian). Preserved in various fragments in SouthwesternSiberia. Consists of the: (1) Late Silurian to Early Carbonif-erous Rudny Altai island arc terrane; and (2) the tectonically-linked Ordovician to Early Carboniferous Kalba-Narim sub-duction zone terrane. The collage is a northwest continuation(present-day coordinates) of the South Mongolia-Khingan is-land arc. The collage extends under Cenozoic and Mesozoiccover of Southwestern Siberia.

YT – Yenisey-Transbaikal collage (Vendian to Devonian;Timing of accretion – Vendian to Early Ordovician). Con-sists of Vendian to Middle Cambrian Kuznetsk-Tannuola,Dzhida-Lake island arc terranes, tectonically-linked back-arc basins, and tectonically eroded subduction zone terranes.The collage consists of a linear array of Vendian and Cam-brian island arc systems that formed south (present-day co-ordinates) of the North Asian Craton and Margin and previ-ously accreted terranes.

The collage is unconformably overlain by Ordovician-Silurian flysch and molasse and also contains local EarlyOrdovician metamorphic and granitoid complexes. Accre-tion of the collage to the Siberian continent occurred in theLate Cambrian to Early Ordovician (500 to 460 Ma) dur-ing counter-clockwise rotation of the Siberian continent thatresulted in collision and duplexing of island arcs, and clo-sure of the back-arc basins. As a result, most of the is-land arcs and tectonically-linked subduction zones ceasedactivity in Middle Cambrian. In Late Cambrian and EarlyOrdovician, collisional granitoid batholiths were emplacedand along with high-temperature metamorphic belts.

Kuznetsk-Tannuola island arc (Vendian to Middle Devo-nian). Preserved in various fragments in Southern Siberiaand Mongolia in the: (1) Neoproterozoic to Devonian Telbes-Kitat island-arc terrane; (2) Late Neoproterozoic and Cam-brian Kozhukhov island arc terrane; (3) Late Neoproterozoicand Early Cambrian Kanim island arc terrane; (4) Cambrianto Ordovician Uimen-Lebed island arc terrane; (5) EarlyCambrian Kurai island arc terrane; (6) Neoproterozoic toDevonian Ulgey Island arc terrane; (7) Neoproterozoic toEarly Cambrian North Sayan island arc terrane; (8) Cam-brian Kizir-Kazir island arc terrane; (9) Cambrian Kham-sara island arc terrane; (10) Early Cambrian Ulugo islandarc terrane; (11) Late Neoproterozoic to Ordovician Ondumisland arc terrane; (12) Cambrian and older(?) Tannuola is-land arc terrane; and (13) Late Riphean to Middle CambrianMinusinsk back-arc basin.

The tectonically-linked subduction zone, subduction zone,and oceanic crust units are the: (1) Late NeoproterozoicTeletsk subduction zone terrane; (2) Late Neoproterozoic andEarly Cambrian Dzhebash subduction zone terrane; (3) Ven-dian and Early Cambrian Alambai subduction zone terrane;(4) Early Cambrian Borus subduction zone terrane; and (5)Late Neoproterozoic and Early Cambrian Kurtushiba sub-duction zone terrane. Blueschist facies units occur in theBorus and Kurtushiba terranes.

Behind the Kuznetsk-Tannuola island arc was the Minusaand Tuva molasse units in the Altai-Sayan and East Tuvaback-arc basins. The units in the Altai-Sayan back-arc basinare the: (1) Late Neoproterozoic and Cambrian Biya-Katununit; (2) Late Neoproterozoic and Cambrian Kiya unit; and(3) Late Neoproterozoic Kizhikhem unit. The East Tuvaback-arc basin is Late Neoproterozoic and Cambrian age.The Minusa and Tuva back-arc molasse basins represent su-perposed structures related to the formation of Hercynianocean basins.

Dzhida-Lake island arc (Vendian to Middle Cambrian).Preserved in various fragments in Southern Siberia and Mon-golia in the: (1) Late Neoproterozoic and Cambrian Lakeisland arc terrane; (2) Late Neoproterozoic and Early Cam-brian Eravna island arc terrane; (3) Late Neoproterozoic toSilurian Orhon-Ikatsky arc terrane; and (4) Late Neoprotero-zoic and Early Cambrian Dzhida island arc terrane.



Behind the Dzhida-Lake island arc was the Transbaikalback arc basin that consists of the: (1) the Ikatsky part of theLate Neoproterozoic to Silurian Orhon-Ikatsky continental-margin arc terrane; (2) part of the Paleoproterozoic throughEarly Cambrian Hamar-Davaa metamorphic terrane; and(3) part of the Late Neoproterozoic Barguzin metamorphicterrane.

A7 Tectonic collages accreted onto Eastern Margin ofNorth Asian and Sino-Korean Cratons (Mesozoicand Cenozoic accretions)

BD – Badzhal collage (Triassic to Early Cretaceous; Timingof accretion – Late Cretaceous). Consists of subduction zoneterranes composed of mainly Triassic and Jurassic turbiditewith fragments of Pennsylvanian and Permian limestone andchert containing Tethyan fauna, Late Triassic and Jurassicchert, and small basalt lenses. Preserved in fragments ofthe following terranes in the northern Russian Southeast: (1)Triassic to Middle Jurassic Badzhal subduction zone terrane;and (2) Middle Triassic through Middle Jurassic Nadanhadasubduction zone terrane.

The subduction zone terranes were subducted beneaththe Siberian continental margin and previously-accretedterranes, thereby resulting in formation of the Umlekancontinental-margin arc that is composed of the CretaceousUmlekan-Ogodzhin volcanic-plutonic belt. The collage wasamalgamated and accreted to the Siberian continental mar-gin during subsequent strike-slip emplacement of outboardterranes in the Early Cretaceous. The collage is uncon-formably overlain by the Late Albian and Late CretaceousOkhotsk-Chukotka volcanic-plutonic belt that forms a majorcontinental-margin arc.

CH – Chukotka collage (Paleozoic to Triassic; Timing ofaccretion – Late Jurassic to Early Cretaceous). Consists ofpassive continental-margin terranes that formed along thelong-lived Neoproterozoic to Early Mesozoic North Amer-ican Continental Margin. Major units are Paleozoic to Tri-assic continental shelf and slope sedimentary rock, EarlyJurassic flysch, and unconformably overlying, flat-lying LateJurassic and Early Cretaceous sedimentary overlap units.The collage consists of various passive continental marginterranes that originally formed along the North AmericanCraton Margin. The collage formed during rifting of theNorth American Craton Margin in the Late Jurassic andEarly Cretaceous and accretion of terranes to northern theNorth Asian Craton Margin in the Late Cretaceous.

EP – East Kamchatka Peninsula collage (mainly Pa-leocene; Timing of accretion – Pliocene). Consists ofConiacian-Paleocene island arc formations with ophiolitefragments that are preserved mainly in the: (1) Late Cre-taceous to Paleocene Kronotskiy island arc terrane; and (2)mainly Cretaceous and Paleocene Kamchatskiy Mys oceanicterrane. The collage is a short-lived island arc and adja-cent oceanic crust that were accreted to the Eastern Asia

continental margin during closure of an inboard ocean inthe Pliocene. The collage is unconformably overlain by flat-lying Quaternary volcanic units.

ES – East Sakhalin collage (Late Cretaceous to Early Ter-tiary; Timing of accretion – Early Tertiary). Consists of LateCretaceous to Middle Eocene island arc and tectonically-linked subduction zone terranes in fragments in the: (1) LateCretaceous Terpeniy island arc terrane; (2) Late Cretaceousto Middle Eocene Tokoro-Nemuro island arc terrane; (3)Late Jurassic through Late Cretaceous Shmidt island arc ter-rane; (4) Early Cretaceous to Miocene Shimanto subductionzone terrane; and (5) probable subduction zone terranes de-lineated by linear positive magnetic anomalies to the eastof Sakhalin Island. Accretion of the island arc to the East-ern Asia continental margin occurred during closure of aninboard ocean and resulted in formation of collision-relatedgranitoids at about 40 Ma.

HS – Honshu-Sikhote-Alin collage (Jurassic and EarlyCretaceous; Timing of accretion – Cretaceous). Consists offragments of subduction zone, continental-margin turbidite(flysch), and island arc terranes. Preserved in fragments arethe: (1) Permian to Early Cretaceous Mino Tamba Chichibusubduction zone terrane; (2) Carboniferous and PermianAkiyoshi-Maizuru subduction zone terrane containing frag-ments of sedimentary units with Tethyan fossils; (3) Creta-ceous Sambagawa metamorphic terrane; (4) Late Early Cre-taceous Kema island arc terrane; (5) Late Jurassic throughEarly Cretaceous Taukha subduction zone terrane; (6) LatePermian through Middle Jurassic Samarka subduction zoneterrane; (7) Early Paleozoic (?) Khor island arc terrane; (8)Jurassic and Early Cretaceous Kiselyovka-Manoma subduc-tion zone terrane; and (9) Late Jurassic and Early CretaceousZhuravlevsk-Amur River continental-margin turbidite ter-rane. The Zhuravlevsk-Amur River continental-margin tur-bidite terrane and companion island arc terranes that formedalong a Late Jurassic and Early Cretaceous continental-margin transform fault along which the older Mino TambaChichibu subduction zone and Akiyoshi-Maizuru subductionzone terranes were emplaced. The collage formed along atransform continental margin.The collage is unconformablyoverlain by Late Albian and younger flat-lying volcanic unitsof the East Sikhote-Alin volcanic-plutonic belt and its con-tinuation onto Honshu Island.

KOR – Koryak collage (Late Triassic to Cretaceous; Tim-ing of accretion – Late Cretaceous). Consists of a Late Juras-sic and Early Cretaceous island arc and tectonically-linkedsubduction zone terranes that are preserved in fragments arethe: (1) Late Jurassic to Mid-Cretaceous Mainitskiy islandarc terrane; (2) Late Jurassic to Paleocene Alkatvaam sub-duction zone terrane; (3) Paleozoic Zolotogorskiy passivecontinental margin terrane; and (4) Upper Paleozoic-EarlyCretaceous Ekonay subduction zone terrane.

OK – Olyutorka-Kamchatka collage (Late Cretaceous andPaleocene; Timing of accretion – Early Cenozoic). Consistsof island arc and tectonically-linked subduction zone terranes



in fragments in the: (1) Late Early Cretaceous to PaleoceneOlyutorka-Kamchatka island arc terrane; (2) Late CretaceousIruneiskiy island arc terrane; and (3) Late Cretaceous toOligocene Vetlovskiy subduction zone terrane. The collageis unconformably overlain by Late Eocene, Oligocene, andMiocene sedimentary units. The collage was accreted to theEastern Asia continental margin during closure of inboardocean.

PA – Penzhina-Anadyr collage (Late Jurassic to EarlyCretaceous; Timing of accretion – Late Cretaceous). Con-sists of Late Jurassic-Neocomian subduction zone terranesand a tectonically-linked island arc terrane that rim the east-ern Kolyma-Omolon superterrane and Verkhoyansk-Kolymacollage. Preserved in fragments are the: (1) Ordovician toMiddle Jurassic Penzhina Anadyr subduction zone terranethat includes fragments of Devonian ophiolite; (2) Middleand Late Jurassic Talovskiy subduction zone terrane; (3) theLate Triassic to Early Cretaceous Kony-Murgal arc terrane;(4) Triassic Velmay subduction zone terrane; and (5) WestPekulney island arc terrane. The subduction zone terraneswere subducted beneath the margin of the Siberian conti-nent margin and previously-accreted terranes to form theUda-Murgal continental-margin arc and offshore extensioninto the Kony-Murgal island arc. The collage was formedin the Senomanian-Campanian following the closure of theoutboard Mongol-Okhotsk Ocean. The collage consists ofthe Uda-Murgal continental-margin and island arc and andtectonically-linked subduction zone terranes. The collage isunconformably overlain by the Late Albian and Late Cre-taceous Okhotsk-Chukotka volcanic-plutonic belt (oc) thatforms a major continental-margin arc.

SA – South Anyui collage (Permian to Early Jurassic;Timing of accretion – Late Cretaceous). Consists of LateJurassic to Neocomian subduction zone terranes, and islandand continental-margin arc terranes that rim the northeast-ern Kolyma-Omolon superterrane and Verkhoyansk-Kolymacollage. Preserved in fragments are the: (1) mainly LateJurassic-Early Cretaceous South Anyui subduction-zone ter-rane; (2) Triassic and Early Jurassic Velmay subduction-zoneterrane; (3) Late Jurassic and Early Cretaceous Oloy andLate Jurassic Svyatov Nos volcanic belts along the northeastmargin of the Kolyma-Omolon superterrane; (4) and LateJurassic and Early Cretaceous Nutesyn continental-marginarc terrane that formed on the margin of the Chukotka col-lage during the closure of the South Anyui Ocean; (5) Per-mian and Triassic Shalaurov subduction zone terrane. Thecollage consists of the Oloy island arc and tectonically-linkedsubduction zone terranes. The collage was accreted onto theSiberian continent margin during closure of the South AnyuiOcean in the Early Late Cretaceous. The collage is uncon-formably overlain by the Late Albian and Late CretaceousOkhotsk-Chukotka volcanic-plutonic belt (oc) that forms amajor continental-margin arc.

The collage is unconformably overlain by Maastrichtian,Eocene and Oligocene sedimentary and volcaniclastic rock.

The accretion of collage to the Russian Northeast conti-nental margin occurred during closure of the inboard oceanand was followed by formation of the Okhotsk-Chukotkacontinental-margin arc and tectonically-linked outboard sub-duction zone.

SH – Sakhalin-Hokkaido collage (Cretaceous; Timing ofaccretion – Eocene). Consists of Late Cretaceous flysch ter-ranes of Sakhalin and Hokkaido Islands, and tectonically-linked subduction zone terranes to the east that contain frag-ments of ophiolite, glaucophane schist, Late Jurassic andEarly Cretaceous limestone with Tethyan reef corals and is-land arc terrane. Preserved in fragments are the: (1) Mid-dle Triassic to Early Late Cretaceous Aniva subduction zoneterrane; (2) Jurassic to Paleogene Sosunay-Langeri subduc-tion zone terrane; (3) Early Cretaceous to Miocene Shimantosubduction zone terrane; (4) Late Cretaceous through Paleo-gene Nabilsky subduction zone terrane; and (5) Late Juras-sic through Late Cretaceous Kamyshovy island arc terrane.The terranes were subducted beneath the Eastern Asia conti-nental margin resulting in the formation of the East-Sikhote-Alin continental-margin arc composed of the: (1) Late Cre-taceous to Miocene East Sikhote-Alin volcanic-plutonic belt;and (2) Early Cretaceous West Sakhalin turbidite basin ter-rane. The collage was a continental-margin fore-arc basinand tectonically-linked subduction zone terranes associatedwith the East Sikhote-Alin continental-margin arc. Accre-tion of the collage to the Russian Southeast continental mar-gin occurred during closure of the inboard ocean and wasfollowed by formation of outboard modern-day continental-margin arcs in Russian Northeast, Kurile Islands, and Japanand tectonically-linked outboard subduction zone.

VK – Verkhoyansk-Kolyma collage (Late Paleozoic toEarly Jurassic; Timing of accretion – Late Jurassic to EarlyEarly Cretaceous). Consists of: (1) Permian, Triassic,and Early Jurassic Kular-Nera passive continental marginterrane (KN) that formed between the North Asian CratonMargin and the Kolyma-Omolon superterrane to the eastin the Russian Northeast; The rocks of the terrane aredistal formations of the Verkhoyansk passive continentalmargin; (2) Mid-Late Jurassic Polousny-Debin subductionzone terrane; (3) Carboniferous to Jurassic Viliga passivecontinental-margin terrane; (4) Debin ophiolite terrane; and(5) Late Neoproterozoic through Late Triassic Kotel’nyipassive continental margin terrane. Part of Kular-Neraterrane was subducted beneath the Kolyma-Omolon supert-errane in the Late Jurassic resulting in formation of the LateJurassic Uyandina-Yasachnaya island arc along the southernmargin of the Kolyma-Omolon superterrane. Ophioliteterranes (Garbyn’ya, Indigirka, Kybytygas, Munilkan,and Uyhandina) derived from the collapsing ocean basinwere obducted onto the superterrane. The Polousny-Debinsubduction zone formed during subduction of the Oimyakonoceanic crust beneath the southern margin of the Kolyma-Omolon superterrane. Consists of a deformed passivecontinental margin, accreted ophiolites, and subduction zone



and formed during accretion of outboard Kolyma-Omolonsuperterrane.

WK – West Kamchatka collage (Mid-Cretaceous to EarlyTertiary; Timing of accretion – Early Cenozoic). Consistsof Late Paleozoic to Cretaceous subduction zone terranes inthe Russian Northeast in the: (1) Jurassic and CretaceousWest Kamchatka subduction zone terrane; (2) Late Jurassicand Cretaceous Yanranay subduction zone terrane; and (3)Jurassic Ekonay subduction zone terrane.

The collage is tectonically linked to Okhotsk-Chukotkacontinental-margin arc (Mid-Cretaceous to Early Tertiary,96–50 Ma) that consists of the: (1) Mid-Cretaceous to EarlyTertiary Okhotsk-Chukotka volcanic-plutonic belt; and (2)Albian and Late Cretaceous Penzhina sedimentary basin.The collage was accreted to the Eastern Asian continen-tal margin during outboard accretion of the Olyutoka-Kamchatka island arc.

A8 Overlapping continental-margin arcs – Devonian toEarly Tertiary

at – Altay arc (Devonian and Early Carboniferous, 381 to290 Ma). Occurs in Southwestern Siberia, NorthwesternMongolia, and Western Northern China. It consists of anextensive suite of mafic and intermediate, and local siliceousvolcanic rock, mafic and intermediate intrusive rock, and as-sociated sedimentary rock; stratified units deposited undercontinental to marine conditions; igneous rocks range fromcalc-alkaline to subalkaline to alkaline. The arc formed alongan active continental margin in an oblique subduction zoneenvironment.

ea – East Sikhote-Alin arc (Late Cretaceous to Early Ter-tiary, 96 to 55 Ma). Occurs along the margin of the SouthernRussian Far East and consists of Late Cretaceous and EarlyTertiary volcanic and plutonic rocks in the East Sikhote-Alinand West Sakhalin turbidite-basin terranes. The arc formedduring subduction of the Ancestral Pacific Ocean plate withformation of the older part of the Hidaka subduction zone,the younger part of the Aniva subduction-zone terrane, andthe Nabilsky, and Tokoro subduction-zone terranes.

gh – Gobi-Khankaisk-Daxing’anling arc (Permian, 295to 250 Ma). Occurs in Northern China, Mongolia,and Transbaikal Region and consists of Gobi-Khankaisk-Daxing’anling volcanic-plutonic belt that overlies and in-trudes the Argun-Idermeg superterrane; the South Mongo-lian collage, and Solon Collage; volcanic and related sed-imentary units composed of basalt, andesite, dacite, rhyo-lite, tuff, sandstone, siltstone, conglomerate, sandstone, andminor limestone; granitoid units composed of adamellite,granite, granodiorite, monzonite granite, quartz monzonite,quartz diorite, gneissic granite, and two-mica granite. Thearc formed during subduction of the northern part of SolonOcean plate under the southern margin (present-day coordi-nates) of the Argun-Idermeg superterrane.

ha – Hangay arc (Late Carboniferous to Early Permian,320 to 272 Ma). Occurs in Central Mongolia and consistsof large- to medium-size multiphase intrusions composed ofgranodiorite, tonalite, plagioclase granite, and minor gabbro-diorite, diorite, quartz diorite, and plagioclase leucogranite.These intrude the Yenisey-Transbaikal collage and Mongol-Okhotsk collage. The arc formed during subduction of thenorthern part of Mongol-Okhotsk Ocean plate under theNorth Asian Craton Margin and previously-accreted terranes.

ji – Jihei arc (Permian, 295–250 Ma). Occurs in EasternChina and consists of granodiorite, monzonite, quartz diorite,quartz monzonite, diorite, syenite, and akali-feldspar gran-ite. Unit intrudes Bureya-Jiamusi supterterrane and SouthMongolia-Khingan collage. The arc formed during subduc-tion of the northern part of Solon Ocean plate under thesouthern margin (present-day coordinates) of the Bureya-Jiamusi supterterrane and adjacent units.

ko – Khingan-Okhotsk arc (Early and Mid-Cretaceous).Occurs in the Russian Southeast and consists of the Khingan-Okhotsk volcanic-plutonic belt that contains K-rich felsicvolcanic rocks and coeval subvolcanic to plutonic grani-tioids. The arc was tectonically paired to the Early Cre-taceous Zhuravlevsk-Amur River and Kiselevka-Manomasubduction-zone terranes, part of the Honshu-Sikhote-Alincollage.

lg – Lugyngol arc (Permian, 295 to 250 Ma). Occurs inSoutheastern Mongolia and consists of Lugyngol volcanicand sedimentary basin composed of calk-alkalic andesite,dacite, rhyolite, conglomerate, sandstone, siltstone, and ex-tensive flysch. Unit overlies and intrudes the South Mon-golian collage and Solon collage. The arc formed duringsubduction of the northern part of Solon Ocean plate underthe southern margin (present-day coordinates) of the Argun-Idermeg superterrane.

ma – Main Granite Belt (Late Jurassic, 144 to 134 Ma).Occurs along adjacent margins of the North Asian CratonMargin and Kolyma-Omolon superterrane. Consists of Mainamphibole-biotite granite, two mica granite, and granodior-ite. The Granite Belt formed during and immediately af-ter collision of the Kolyma-Omolon superterrane onto theNorth-Asian Craton Margin.

nb – Northern Granite Belt (Early Cretaceous, 138 to120 Ma). Occurs along northwestern margin of the Kolyma-Omolon superterrane. Consists of large, elongated plutonscomposed of quartz diorite, monzodiorite, and biotite gran-ite, as well as amphibole-biotite granodiorite, biotite granite,and two-mica granite. The belt formed during subduction ofoceanic crust during a closure of a small oceanic basin duringlate stage of accretion of Kolyma-Omolon superterrane.

nm – North Margin arc (Late Carboniferous to Permian,320 to 272 Ma). Occurs in Northern China and consists ofnorth marginal plutonic belt composed of calc-alkalic gran-odiorite, quartz monzonite, and granite. Unit intrudes north-eastern margin (present-day coordinates) of Sino-KoreanCraton. The arc formed during subduction of the southern



part of Solon Ocean plate under the northeastern margin(present-day coordinates) of Sino-Korean Craton.

nr – Norovlin arc (Devonian to Early Carboniferous). Oc-curs in Northern Mongolia and the Transbaikal region andconsists of a continental-margin arc formed on the Argun-Idermeg superterrane (Amur microcontinent – Argunsky andIdermeg passive continental margin terranes). The arc is pre-served in Early to Middle Devonian calc-alkaline volcanicrock and in Middle to Late Devonian volcaniclastic rock,chert, and mudstone, and coeval granitoids that overlie orintrude the superterrane, and in Devonian to Early Carbonif-erous volcanic-sedimentary rock fragments in the Ononskysubduction zone terrane. The arc formed during subductionof the Mongol-Okhotsk Ocean plate beneath northern mar-gin (present-day coordinates) of Argun-Idemeg superterrane(Amur microcontinent).

oc – Okhotsk-Chukotka arc (Late Cretaceous to Early Ter-tiary, 96 to 53 Ma). Occurs along the margin of the Centraland Northern Russian Far East and consists of Mid- and LateCretaceous and Early Tertiary volcanic and plutonic units inthe Okhotsk-Chukotka volcanic-plutonic belt (oc) and thePenzhina sedimentary basin. The arc formed during sub-duction of the Ancestral Pacific Ocean plate with formationof West Kamchatka, Ekonay, and Yanranay subduction zoneterranes.

ol – Oloy arc (Late Jurassic, 154 to 135 Ma). Occurs alongthe margin of the Kolyma-Omolon superterrane and con-sists of Late Jurassic-Neocomian Oloy volcanic belt, LateJurassic Svyatov Nos volcanic belt, and the Indigirka-Oloysedimentary-volcanic-plutonic assemblage. The arc was anisland arc that formed on Kolyma-Omolon superterrane dur-ing subduction of the South Anyui Ocean plate beneath su-perterrane and formation of South Anyui subduction-zoneterrane.

se – Selenga arc (Permian to Jurassic, 295 to 135 Ma).Occurs in Mongolia and southern Transbaikal regions andconsists of large volcanic fields and granite plutons. Vol-canic rock composed of rhyolite, trachyrhyolite, dacite, tra-chydacite, andesite basalt, trachybasalt, and andesite flows,and pyroclastic rocks, and local non-marine sedimentaryrocks. Granite plutons composed of granodiorite, granite,granosyenite, and subordinate monzonite, diorite, and gab-brodiorite, REE granite, and leucogranite. Unit overlies andintrudes Yenisey-Transbaikal collage and Tuva-Mongolia su-perterrane. The arc formed during oblique subduction of theMongol-Okhotsk Ocean plate under the North Asian CratonMargin and previously-accreted terranes.

sm – South Mongolian arc (Middle Carboniferous throughTriassic, 320 to 203 Ma). Occurs in Southern Mongo-lia and consists of South Mongolian volcanic-plutonic beltcomposed of calc-alkalic basalt, andesite, basaltic andesite,dacite, and rhyolite, and interbedded tuff and tuffaceoussandstone, granodiorite, granite, and leucogranite. Unit over-lies and intrudes South Mongolian collage and Atasbogd

collage. The arc formed during subduction of northern partof Solon ocean under the Argun-Idermeg superterrane.

sv – South Verkhoyansk Granite Belt (Late Jurassic toMid-Cretaceous, 157 to 93 Ma). Occurs in the CentralRussian Far East. Extends longitudinally along the centralpart of the South Verkhoyansk synclinorium in the Verkoy-ansk (North Asian) Craton Margin. Occurs as batholiths,smaller granitoid plutons, and dikes. Compositions includeamphibole-biotite quartz diorite and granodiorite, adamellite,amphibole-biotite granite, local melanocratic syenodiorite,and local dikes of plagiogranite and granite aplite, leuco-cratic biotite granite, and pegmatite lamprophyre. Granitoidsare mainly high-K calc-alkaline series, subaluminous, andhighly ferruginous. The Granite Belt formed during the ac-cretion of the outboard Okhotsk terrane.

tv – Transverse Granite Belt (Early Cretaceous, 134 to124 Ma). Consists of several belts of granitic rocks that ex-tend up to a few hundred km and radiate outwards from thesouthwestern bend of the Kolyma-Omolon superterrane. Thebelts taper out to the southwest and north and consists offracture-related plutons and dikes swarms composed mainlyof diorite, granodiorite, and granite. The belts crosscut, athigh angle, older folds and faults of the Verkhoyansk (NorthAsian) Craton Margin. The belt formed during the late-stageof accretion of Kolyma-Omolon superterrane.

uo – Umlekan-Ogodzhin arc (Jurassic and Cretaceous, 135to 65 Ma). Occurs along the margin of the Kolyma-Omkolonsuperterrane and consists of Umlekan-Ogodzhin volcanic-plutonic belt and coeval Late Jurassic and Early Cretaceousgranitic plutons. Tectonically linked to the Badzhal andNadanhada subduction-zone terranes, part of the Badzhalcollage.

us – Uda-Murgal and Stanovoy arcs (Jurassic to EarlyCretaceous, 203 to 96 Ma). Occurs in central part of theRussian Far East and consists of Late Jurassic and EarlyCretaceous, and lesser Late Triassic to Middle Jurassicigneous-rock preserved in the Uda volcanic-plutonic belt, theUniya-Bom turbidite-basin terrane, the Umlekan-Ogodzhinvolcanic-plutonic belt, the Upper Amur sedimentary assem-blage, and the Stanovoy Granite Belt. The arc intrudes andoverlies southern margin of the North Asian Craton. Thearc formed during subduction of the Mongol-Okhotsk Oceanplate and formation of the Tukuringra-Dzhagdi subduction-zone, Galam subduction zone, and Ulban subduction zoneterranes.

uy – Uyandina-Yasachnaya arc (Late Jurassic to EarlyCretaceous, 154 to 120 Ma). Occurs along the southern mar-gin of the Kolyma-Omkolon superterrane and consists ofthe Uyandina-Yasachnaya volcanic belt, Zyryanka sedimen-tary basin, the small Ainakhkurgen, Umkuveem, and Up-per Penzhina basins, and the North Omolon basin that formpart of the Indigirka-Oloy sedimentary-volcanic-plutonic as-semblage. The arc formed during subduction the OimyakonOcean plate between the North Asian Craton Margin and theKolyma-Omolon superterrane. Remnants of oceanic crust



are preserved in small obducted ophiolites along the marginof superterrane.

A9 Transpressional arcs – Devonian to EarlyCretaceous

mt – Mongol-Transbaikal arc (Late Triassic to Early Cre-taceous, 230 to 96 Ma). Occurs in Northern Mongoliaand southern Transbaikal regions. Preserved in the LateTriassic to Early Cretaceous Mongol-Transbaikal regionvolcanic-plutonic belt (mt) that consists of volcanic rocksin separate major basins and composed of trachyandesite,dacite, and trachyrhyolite flows, stocks, necks, and extrusivedomes. The Mongol-Transbaikal arc also includes coevalgranite plutons composed of grandiorite, alkaline gabbro-granite, granite, leucogranite, and Lithiumn-Fluorine richgranite. The arc formed during strike-slip faulting and rift-ing along the Mongol-Okhotsk fault during and after the fi-nal closure of the Mongol-Okhotsk Ocean. The arc is alsoreferred to as North Gobi arc.

ss – South Siberian arc (Early Devonian, 415 to 400 Ma).Occurs in Eastern Altai-Sayan region and consists of SouthSiberian volcanic-plutonic belt, involving volcanic rockscomposed of bimodal mafic and siliceous volcanic rockincluding andesite, olivine basalt, trachybasalt, essexite,phonolite, alkaline trachite, trachyandesite, and trachyrhyo-lite. Plutonic rocks are composed of subalkaline to alkalinegabbro to granite, alkaline-syenite, granosyenite, leucogran-ite, and latite-bearing subalkaline gabbro, monzonite, andsyenogranite. The arc formed along the southern margin ofthe North Asian Craton and Craton Margin during Early De-vonian rifting that successively evolved into a continental-margin transpressive-fault margin and into a convergent mar-gin.

tr – Trans-Baikal-Daxinganling arc (Middle Jurassicthrough Early Cretaceous, 175 to 96 Ma). Occursin Transbaikal region, Mongolia, Northeastern Chinaand consists of Trans-Baikalian-Daxinganling sedimentary-volcanic-plutonic belt. Volcanic rocks are composed ofshoshonite, latite, trachyte, trachyandesite, trachybasalt, tra-chyrhyolite, latite subalkaline basalt, and basalt andesite.Plutonic rocks are composed of large calc-alkaline to subal-kaline plutons of granite, leucogranite, quartz syenite, quartzmonzonite, granodiorite, and biotite-amphibole diorite, andsmall calc-alkaline subvolcanic bodies of dacite and rhyo-lite. The arc formed during strike-slip faulting and riftingalong the Mongol-Okhotsk fault during, and after the finalclosure of the Mongol-Okhotsk Ocean.

A10 Active continental-margin arcs – Miocene toPresent

ib – Izu-Bonin arc (Miocene through Present, 20 to 0 Ma).Occurs in the south of Southern Japan and consists of a vol-canic arc composed chiefly of basalt to rhyolite, associated

volcaniclastic rocks, and intercalated hemipelagic mudstone.The arc formed during subduction of the Philippine Sea Platewith formation of Nankai subduction zone.

ja – Japan arc (Miocene through Present, 23 to 0 Ma). Oc-curs along the Japanese Islands and consists of extensiveQuaternary volcanic rock formed during subduction of thePacific and Philippine Sea Plates. Also contains associatedvolcanogenic forearc and back arc sedimentary basins. Vol-canic rocks are mainly calc-alkaline basalt and andesite. Beltincludes 83 active volcanoes and overlies all Japan terranes.The arc formed during subduction of the Pacific Ocean andPhilippine Sea Plates with formaton of Japan Trench andNankai subduction zones.

kk – Kuril-Kamchatka arc (Miocene through Present, 11 to0 Ma). Occurs along Kamchatka Peninsula and Kuril Islandsand consists of the Pliocene to Quaternary Central Kam-chatka volcanic belt, Central Kamchatka volcanic and sed-imentary basin, and the East Kamchatka volcanic belt. Thearc formed during subduction of the Pacific Ocean Plate withformation of the Japan Trench subduction zone.

A11 Active subduction zones – Miocene to Present

JT – Japan Trench subduction zone (Miocene throughPresent; Timing of accretion – 23 to 0 Ma). Consists of LateTertiary and Quaternary Japan and Kuril-Kamchatka trenchsubduction zone terranes. Tectonically linked to the: (1)Miocene to Present Japan arc (ja); (2) Miocene to PresentKuril-Kamchatka arc; and (3) Paleogene through QuaternaryJapan and Izu-Bonin forearc basins. The subduction formedduring active underthrusting of the Western Pacific OceanPlate beneath the Eastern Asia continental margin.

NN – Nankai subduction zone (Miocene through Present;Timing of accretion – 23 to 0 Ma). Consists of the Miocenethrough Quaternary Nankai subduction zone terrane. Tec-tonically linked to the: Miocene to Present Japan arc; (2)Miocene to Present Izu-Bonin volcanic belt; (3) PaleoceneKyushu-Palau island arc terrane; and (4) Miocene throughQuaternary Izu-Bonin island arc terrane. The subductionformed during active underthrusting of a fragment of the Pa-cific Ocean Plate.

Acknowledgements.In the last three decades, many persons haveassisted the authors in developing and employing the concepts ofcombined regional geodynamics and tectonic analysis, and in de-veloping methods for synthesizing a tectonic model. These per-sons include David L. Jones, James W. H. Monger, Ian O. Norton,David W. Scholl, Christopher R. Scotese, and David B. Stone. Wealso thank managers N. L. Dobretsov, L. C. Gundersen, P. P. Hearn,K. Johnson, R. Koski, L. P. Leahy, J. Medlin, M. Power, andJ. N. Weaver for their encouragement and support of the project.The constructive reviews of this article by Charles Cunningham,Jeremy Hourigan, and William Harbert are appreciated.



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Nokleberg, W. J., Bundtzen, T. K., Dawson, K. M., Eremin, R. A.,Ratkin, V. V., Shpikerman, V. I., Goryachev, N. A., Khanchuk,A. I., Koch, R. D., Rozenblum, I. S., Gorodinsky, M. E., Frolov,Y. F., Pozdeev, A. I., Parfenov, L. M., and Sidorov, A. A.:Mineral deposit and metallogenic belt maps of the Russian FarEast, Alaska, and the Canadian Cordillera, Geological Survey ofCanada, Open File 3446, 2 sheets, scale 1:5 000 000, 5 sheets,scale 1:10 000 000, 1997b.

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Nokleberg, W. J., Parfenov, L. M., Monger, J. W. H., Baranov, B. V.,Byalobzhesky, S. G., Bundtzen, T. K., Feeney, T. D., Fujita, K.,Gordey, S. P., Grantz, A., Khanchuk, A. I., Natal’in, B. A., Nat-apov, L. M., Norton, I. O., Patton Jr., W. W., Plafker, G., Scholl,D. W., Sokolov, S. D., Sosunov, G. M., Stone, D. B., Tabor, R.W., Tsukanov, N. V., and Vallier, T. L.: Summary Circum-NorthPacific tectono-stratigraphic terrane map, US Geological Survey,Open-File Report 96-727, scale 1:10 000 000, 1997c.

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Scotese, C. R., Nokleberg, W. J., Monger, J. W. H., Norton, I. O.,Parfenov, L. M., Bundtzen, T. K., Dawson, K. M., Eremin, R.A., Frolov, Y. F., Fujita, Kazuya, Goryachev, N. A., Khanchuk,A. I., Pozdeev, A. I., Ratkin, V. V., Rodinov, S. M., Rozenblum,I. S., Shpikerman, V. I., Sidorov, A. A., and Stone, D. B.: Dy-namic computer model for the metallogenesis and tectonics ofthe Circum-North Pacific, edited by: Nokleberg, W. J. and Dig-gles, M. F., US Geological Survey, Open-File Report 01-161,CD-ROM, 2001.


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Summary of Northeast Asia geodynamics and tectonics · 4/11/2009 · summary geodynamics map of the region, and also pro-vides a general introduction for readers who are unfamil-iar