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The Late Permian to TriassicHongseong-Odesan Collision Beltin South Korea, and Its TectonicCorrelation with China and JapanChang Whan Oh a & Timothy Kusky ba Chonbuk National University, South Koreab St. Louis UniversityPublished online: 06 Aug 2010.

To cite this article: Chang Whan Oh & Timothy Kusky (2007) The Late Permian to TriassicHongseong-Odesan Collision Belt in South Korea, and Its Tectonic Correlation with China and Japan,International Geology Review, 49:7, 636-657, DOI: 10.2747/0020-6814.49.7.636

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International Geology Review, Vol. 49, 2007, p. 636–657.Copyright © 2007 by V. H. Winston & Son, Inc. All rights reserved.

0020-6814/07/942/636-22 $25.00 636

The Late Permian to Triassic Hongseong-OdesanCollision Belt in South Korea, and Its Tectonic Correlation

with China and JapanCHANG WHAN OH1

Department of Earth and Environmental Sciences, Chonbuk National University, Chonju, 561-756, South Korea

AND TIMOTHY KUSKY

Department of Earth and Atmospheric Sciences, St. Louis University, St Louis, Missouri 63103

Abstract

We propose a new correlation of Middle Triassic (ca. 230 Ma) eclogites from the Hongseong areaof the southwest Gyeonggi Massif, South Korea, with the Dabie-Sulu collision belt of China. LatePermian (ca. 257 Ma) mangerites that intrude the Odesan area in the eastern part of the GyeonggiMassif show geochemical characteristics of collisional tectonic settings, implying that the Hong-seong collision belt extends to the Odesan area. In the Higo terrain of southernmost Japan, sapphirine-bearing granulites and related high-temperature metamorphic rocks reveal ca. 245 Ma ultrahigh-temperature (UHT) metamorphic conditions. This metamorphism is well matched with the 245 ± 10Ma UHT metamorphism estimated for spinel granulite in the Odesan area, suggesting that theDabie-Sulu collision zone continues through the Hongseong-Odesan belt into the Higo area and thatPaleozoic subduction complexes in southwest Japan represent an eastern extension of the Dabie-Sulu collision belt. The Paleozoic subduction complexes in Japan continue further to the Yanji belt,a Carboniferous and Permian subduction complex along the northeastern boundary of the NorthChina block. These data indicate that Phanerozoic subduction along the margin of the North Chinablock and the collision between the North and South China blocks contributed to formation of theDabie-Sulu-Hongseong-Odesan-Higo-Yanji belt. P-T estimations reveal that there was a decrease ingeothermal gradients and an increase of exhumation rates from east to west along the belt duringcollision. These gradients resulted in preservation of UHT metamorphism in the Odesan area inKorea and the Higo area in Japan, high-pressure (HP) metamorphism in the Hongseong belt, andultra high-pressure (UHP) metamorphism in the Dabie-Sulu belt.

Introduction

THE TRIASSIC Dabie-Sulu collision belt between theNorth China and South China blocks was identifiedby the discovery of ophiolites and UHP metamor-phism (Fig. 1; e.g., Wang et al., 1989; Zhai andCong, 1996; Zhai and Liu, 1998), and is distin-guished as containing the world’s largest belt ofUHP metamorphic rocks. There are currently sev-eral debates concerning the tectonic relationshipbetween Korea, China, and Japan, with a number ofdifferent tectonic models proposed to describe thisrelationship (Fig. 2; Yin and Nie, 1993; Ernst andLiou, 1995; Chang, 1996; Zhang, 1997). It is impor-tant to know where the Dabie-Sulu belt continuesand which belts in Korea and Japan it may be con-

temporaneous with in order to obtain a better under-standing of the tectonic processes that led toformation and exhumation of these distinctive UHProcks.

Yin and Nie (1993) argued that collision betweenthe North and South China blocks began by theindentation of the northeastern South China blockinto the southeastern North China block in the LatePermian and continued until the Late Triassic. Intheir model, the collision belt was suggested toextend to the Imjingang belt in Korea and thedextral Honam shear zone in Korea was regarded asa contemporaneous counterpart of the Triassic sinis-tral Tanlu fault in China (Fig. 2A). These faultstogether accommodated the northward extrusion ofthe South China block between them. However, theydid not give any evidence of collision from theImjingang belt. Moreover, the Honam shear zone1Corresponding author; e-mail: ocwhan@chonbuk.ac.kr

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cannot be a counterpart of the Tanlu fault because itbegan to form in the Middle Jurassic instead of theTriassic (Cho et al., 1999; Lee et al., 2003b). Ree etal. (1996) reported late Permian (249 Ma) metamor-phism (8.9–11.5 kbar and 640-815°C) from theImjingang belt as evidence for HP metamorphismrelated to collision. However, as shown in Figure 3,these P-T conditions do not represent HP metamor-phism as claimed. Chang (1996) also interpreted theImjingang belt as an extension of the collision belt,and the Okcheon belt (also transliterated as theOgcheon belt) in South Korea as a continuation ofthe Huanan failed rift in South China. Zhang (1997)proposed a different model in which the Dabie-Sulucollision zone extends to the Yanji zone through theImjingang belt, and he further argued that the colli-sion started from the east during the early Permian

and propagated westward until the late Triassic (Fig.2B). These models also simply suggested that theImjingang belt is the extension of the collision beltinto Korea, without giving any evidence for collisionfrom the belt. Ernst and Liou (1995) regarded theDabie-Sulu collision zone as not only crossing someparts of Korea, but also extending to the Sangunterrain in Japan (Fig. 2C). On the other hand, Ishi-watari and Tsujimori (2003) suggested an extensionof the collision belt from China to Japan directlywithout passing through Korea (Fig. 2D).

The discrepancies among these different tectonicmodels arose mainly from a lack of hard data con-cerning the nature of the late Paleozoic to Triassicsubduction complexes and potential collision beltsin Korea. Recently late Paleozoic to Triassic eclo-gite-facies metamorphism has been identified from

FIG. 1. Simplified tectonic map of northeastern Asia showing the localities for Permo-Triassic eclogites and spinel/sapphirine granulite. Abbreviations: GB = Gyeongsang Basin; GM = Gyeonggi Massif; HB = Hida belt; HMB = Hidamarginal belt; IB = Imjingang belt; ISWJ = Inner zone of Southwest Japan; NM = Nangrim Massif; OK = Oki belt; OMB =Okcheon metamorphic belt; PB = Pyeongnam Basin; TB = Taebacksan basin; YM = Youngnam Massif.

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the Hongseong area in the southwestern Gyeonggimassif, Korea (Oh et al., 2003, 2004a, 2005), farsouth of the previously proposed suture, in theImjingang belt. Late Paleozoic igneous activity andUHT metamorphism related to continental collisionare also reported from the Odesan area in the east-ern part of Gyeonggi massif, Korea (Oh et al, 2006a).Besides the new important findings in Korea, therehas been substantial progress in elucidating anunderstanding of the tectonic history of East China,and several new discoveries have been made fromPaleozoic and Triassic HP metamorphic belts inJapan. This paper proposes a new model to describethe tectonic relationships between Korea, China,and Japan based on these new data.

Tectonic Relation betweenKorea and China

Geology of Eastern China

East China consists of two major Precambriancratons, the North China and the South Chinablocks (Fig. 1). The South China block is in turndivided into the Yangtze and the Cathaysia blocks.Radiometric dating of two ophiolite suites in theeastern part of the suture between the Yangtze andCathaysia blocks gives Sm-Nd ages of 1034 and1020 Ma (Chen et al., 1991). Late Mesoproterozoicsuture zones have been also reported from the north-western and northern margins of the Yangtze block.Li (1984) reported an ophiolitic mélange in westernSichuan (the northwestern margin) that contains

FIG. 2. Tectonic models showing previously proposed tectonic relationships between Korea, China, and Japan. A.Tectonic model suggested by Yin and Nie (1993). B. Tectonic model suggested by Zhang (1997). C. Tectonic modelsuggested by Ernst and Liou (1995). D. Tectonic model suggested by Ishiwatari and Tsujimori (2003).

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gabbro and diabase with a whole-rock Rb-Sr iso-chron age of 1006 ± 59 Ma. Zircon ages of 1304 and1004 Ma have been determined from quartz-kerato-phyres along the northern margin of the Yangtzeblock (Huang, 1993). Li et al. (1995) proposed thatthe late Mesoproterozoic continental collision beltsin and around the South China block correspondedto one of the central Grenvillian sutures of Rodiniathat brought together Australia, Yangtze andCathaysia-Laurentia at ca. 1000 Ma.

The tectonostratigraphy and paleomagnetic fea-tures of the southern North China block differ fromthose of the South China block and suggest that theNorth China block became a part of Rodinia at ca.1000 Ma, when the southern border of the NorthChina block lay adjacent to Siberia (Zhai et al.,2003). These data indicate that the South and NorthChina blocks became parts of the Rodinia supercon-tinent independently at ca. 1000 Ma (Fig. 4).

The breakup of Rodinia was probably initiatedby a ca. 820 Ma mantle plume (e.g., Park et al.,

1995; Li et al., 1999). The Kangdian Rift in thesouthwestern border of the South China block andthe Nanhua Rift along the boundary between theYangtze and Cathaysia blocks formed as a result ofbreakup of Rodinia (Fig. 4; Zhou et al., 2002). The800–700 Ma intrusion ages of granitic gneisses inthe northern border of the South China block arealso associated with rifting of the South China blockfrom Rodinia. The separation of the South Chinablock from Rodinia must have occurred after 750Ma (Li et al., 1995). Likewise, on the southernborders of the North China block, rather weakmagmatic activity and metamorphism at ca. 800–600 Ma has been identified (Kröner et al., 1993; C.Zhang et al., 1996), which Zhai et al. (2003) relateto the rifting of the North China block from Rodinia.

Following the break-up of Rodinia during thelate Neoproterozoic, several microcontinents andimmature island arcs amalgamated through collisionand accretion to form Gondwana during the Pan-African orogeny (ca. 520 Ma; Stern, 1994;

FIG. 3. Inferred metamorphic conditions and P-T paths for the Bibong eclogite in the Hongseong area (Oh et al.,2005) and the Samgot amphibolite in the Imjingang belt (Ree et al., 1996). Thick and thin solid lines represent P-Tpaths of the Bibong eclogite and the Taohong eclogites in the Sulu belt (Yao et al. 2000), respectively. The petrogeneticgrid used is that of Oh and Liou (1998). Abbreviations: BS = blueschist facies; GS = greenschist facies; EA = epidote-amphibolite facies; AM = amphibolite facies; EG = eclogite facies; HG = high-pressure granulite facies; LG = low-pressure granulite facies; IB = P-T condition for amphibolite in the Imjingang belt.

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Maruyama et al., 1997; Li and Powell, 2001; Kuskyet al, 2003). The South and North China blocksprobably converged with each other during the EarlyCambrian and lay close to Australia by the Middleand Late Cambrian (Palmer, 1974; Burrett andRichardson, 1980). Metcalfe (1996) proposed thatthe Paleo-Tethys Ocean opened in the Devonian,moving the North and South China blocks north-ward, and the Paleo-Tethys Ocean between twoblocks disappeared in the Middle Triassic bysubduction of all oceanic crust. The presence of450–400 Ma ophiolites (Li et al., 1991), arc-related470–435 Ma metamorphism (Kröner et al., 1993),and ca. 210–330 Ma eclogites (Cong et al., 1992;

Zhang and You, 1993) in the Qinling-Dabie-Sulucollision belt indicate that opening of the Paleo-Tethys had started in the mid-Ordovician instead ofthe Devonian.

Most models for the Qinling-Dabie-Sulu belthave assumed that the collision zone between theNorth and South China blocks included only onecollisional suture, but recent work has revealed amore complex situation involving at least twosutures and three tectonic plates (G. W. Zhang et al.,1996; Li et al., 2006). According to these models,the Qinling-Dabie-Sulu belt includes the NorthChina block, the Qinling-Dabie microblock (includ-ing the Qaidam, West Qinling, South Qinling, and

FIG. 4. A. Configuration of the mid-Proterozoic supercontinent of Rodinia revised after Li and Powell (2001) andZhai et al. (2003). B. Relative positions of East Gondwana, Yangtze, Cathaysia, and Laurentia based on paleomagneticdata at ~1.0 Ga (revised after Li et al., 1995). C. Late Proterozoic breakup of Rodinia revised after Li and Powell (2001).D. Rifting zone between East Gondwana, South China, and Laurentia at about 720 Ma (revised after Li et al., 1995).Abbreviations: PRC = Priest River Complex; BB = Belt Basin; NCB = North China block; SCB = South China block; Sib= Siberian block.

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Dabie blocks from west to east), and the South China(Yangtze) block. The early Paleozoic saw northwardsubduction of the Qaidam block beneath the NorthChina block, forming an active margin on the south-ern margin of the latter. The North China blockcollided with the Qaidam-Dabie micro-block in theDevonian, producing the Shangxian-Danfengsuture, then the South China block in the Permo-Triassic, forming the Mianxian-Lueyang suture(Meng and Zhang, 2000; Liu et al., 2004; Li, et al.,2006, and references therein). This latter collisionstarted in the east and propagated westward (Zhaoand Coe, 1987; Zhang, 1997) until 209 Ma (Ames etal., 1993). The latter collision resulted in exposureof UHP rocks from approximately 100 km depth inthe Dabie Shan and westward extrusion of theQaidam block (e.g., Okay and Sengor, 1993; Yin andNie, 1993; Hacker et al., 2000; Ratschbacher et al.,2000, 2003), and caused uplift of a large plateau(the Huabei Plateau) in the eastern North Chinablock. The Tanlu fault was initiated in the latePermian (258–248 Ma) as a result of this collisionand continued until the late Triassic (231–213 Ma)(Yin and Nie, 1993).

The Sulu belt in the Shandong Peninsula at theeastern end of the Qinling-Dabie-Sulu belt, containsultramafic rocks, metabasites, and marble that formlenses within the Jiaonan granitic gneisses (Wang etal., 1989; Zhang et al., 1994; Ames et al., 1996;Rowley et al., 1997; Kato et al., 1997). Intrusionages of granitic gneiss and metabasites fall between700-800 Ma (Ames et al., 1996). Metabasites in theSulu area were metamorphosed to coesite-bearingUHP eclogites during 208–245 Ma by the Permianto Triassic collision between the South China andthe North China blocks (Li et al., 1993; Ye et al.,2000). The eclogites underwent an almost isother-mal decompression due to fast uplift as shown inFigure 3, first being retrograded to granulite-faciesconditions followed by amphibolite-facies metamor-phism (Zhang et al., 1995; Banno et al., 2000; Yao etal., 2000). During the retrogression, symplectic tex-tures formed and clinopyroxene compositions wereconverted from omphacite through sodic augite toaugite.

Geology of southern Korea

The southern part of the Korean Peninsula con-sists of the Gyeonggi and Yeongnam Precambrianmassifs and two Phanerozoic belts (the Imjingangand Okcheon belts) (Fig. 1). The Imjingang beltconsists of metasediments of Devonian–Carbonifer-

ous age (Ri and Ri, 1990, 1994). The Okcheon beltis subdivided into the northeastern Taebacksanbasin and the southwestern Okcheon metamorphicbelt. The Okcheon metamorphic belt consists ofnon-fossiliferous, low- to medium-grade metasedi-mentary and metavolcanic rocks. By contrast, theTaebaeksan basin consists of fossiliferous, non- orweakly metamorphosed sedimentary rocks of Paleo-zoic to early Mesozoic age.

Ultramafic rocks, metabasites, and marbles arepreserved as lensoid bodies within granitic gneiss inthe Hongseong area, in the southwestern part of theGyeonggi massif of South Korea (Choi et al., 1998)as they are in the Sulu belt (Fig. 5A). SHRIMP U-Pbzircon intrusion ages of the granitic gneisses have anarrow age range falling between 812 and 822 Ma(Cho, 2001). Metabasites in the Bibong area in thesoutheast Hongseong region are eclogites or showrelics of eclogite-facies mineral assemblages (Oh etal. 2003, 2005). Guo et al. (2004) and Kim et al.(2006) obtained a ca. 230 Ma metamorphic age anda ca. 800 Ma intrusion age from the Bibong eclogitesusing SHRIMP zircon age dating. A metamorphicage of ca. 230 Ma was also obtained from the rims ofzircon in granitic gneiss of the Hongseong area(Cho, 2001). The eclogite experienced an isothermaldecompressional P-T path, indicating fast uplift(Fig. 1). During the decompression, symplectiteformed around garnet (Fig. 5B) and such simplectiteis also observed in the other metabasite lenses in theHongseong area. These geologic settings and P-Tpaths are very similar to those in the Sulu belt.Metabasite boudins in the ultramafic bodies in theBaekdong area in the west Hongseong region aremetamorphosed under transitional P-T conditionsbetween the eclogite and high-pressure granulitefacies during 297–268 Ma (Oh et al., 2004a). Theseresults led Oh et al. (2004a, 2005) to suggest thatthe Hongseong area is an extension of the Dabie-Sulu collision belt in China. They also argued thatcollision between the North and South China blocksprobably occurred earlier in Korea than in China.The finding of a gravity anomaly crossing the WestSea between Korea and China by Choi et al. (2006)supports the suggestion.

The Late Permian to TriassicCollision Belt in Korea

The Odesan area is located in the eastern part ofthe Gyeonggi Massif in Korea, and consists mainlyof migmatitic and porphyroblastic gneisses (Fig. 6).

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FIG. 6. Simplified tectonic map of Northeast Asia and geologic map of Odesan area after Oh et al. (2006b). Abbre-viations: HS = Hongseong area; ODS = Odesan area. Other abbreviations are the same as those used in Figures 1 and 5.

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Mangerite forms stocks intruding the migmatiticgneiss. The mangerite is porphyritic, containingalkali feldspar phenocrysts up to 3 cm long (Fig.7A), in a matrix consisting of orthopyroxene, clino-pyroxene, amphibole, biotite, plagioclase, quartz,apatite, and zircon (Fig. 7B). Oh et al. (2006b)showed that the mangerites differ from mangeritesformed in a typical within-plate tectonic setting intheir high Mg# and Sr concentrations and negativeNb and Ta anomalies. Their LILE enrichments andnegative Ti-Nb-Ta anomalies are probably inher-ited from a pre-collision subduction event, indicat-ing a convergent margin origin for the mangerites.Together with the geochemical data, the U-Pb zir-con age of 257 Ma from the mangerites implies thatthe Hongseong collision belt extends into the Ode-san area. The Hongseong collision belt, consistingmainly of late Proterozoic granitic gneiss, is termi-

nated by NNE-striking faults, and does not con-tinue across the east side of the fault where earlyProterozoic granitic gneiss crops out. The rocks inand around the fault seem to show sinistral strike-slip movement senses (Fitches, 2004), suggestingthat the collision belt moved to the north on the eastside of the sinistral fault. A ca. 240 Ma hornblende-gabbro is present in the Yangpyeong area (So et al.,1989), and possibly formed as a consequence ofcollision, suggesting that the Odesan area may havebeen connected to the Yangpyeong area. The sug-gested Odesan-Yangpyeong belt lies to the north ofthe Hongseong belt, supporting the idea that theeastern part of the collision belt in Korea may bemoved toward the north along the expected sinistralstrike-slip fault (Fig. 8). The fault may continue tothe eastern end of the Imjingang belt where anothersinistral strike-slip fault with a strong NNE-striking

FIG. 7. A. The porphyritic texture of mangerite. B. Photomicrograph showing the orthopyroxene (Opx) + clinopyrox-ene (Cpx) + amphibole (Amp) + plagioclase (Pl) + K-feldspar (K-feld) + quartz (Qtz) assemblage of mangerite. C. Theassemblage of garnet, sillimanite (Sil), spinel (Spl), and cordierite (Crd). D. BSE image showing assemblage of spinel +cordierite + corundum (Crn), and corundum, cordierite, and sillimanite inclusions in spinel in spinel granulite.

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mylonitic foliation terminates the belt (Jeon andKwon, 1999). Although not connected, severalNNE-striking faults are identified along the lineconnecting the two sinistral faults in eastern partsof the Hongseong and Imjingang belts (Fig. 8;KIGAM, 2001). The expected fault suggests thatsinistral strike-slip faults may have formed inKorea in a manner similar to the Tanlu fault inChina during the collision of the North and SouthChina blocks.

The proposed collision belt can also be sup-ported indirectly by the following four aspects. Firstis the concentration of most Permo-Triassic ages inSouth Korea within the Gyeonggi massif and itsneighboring two belts (the Okcheon metamorphicbelts and Imjingang belt). Permo-Triassic metamor-phic and igneous ages are obtained from graniticgneiss and metabasites in the Gyeonggi gneiss com-plex (So et al., 1989; Cho et al., 1996, 2001; Cho,2001; Cho and Kim, 2003; Sagong et al., 2003; Guoet al., 2004; Oh et al., 2004a, 2005, 2006a; Kim etal., 2006). Approximately 300–260 Ma metamor-phic ages are reported from the Okcheon metamor-phic belt (Kim et al., 2001; Cheong et al., 2003;Kim, 2005) and 255–249 Ma metamorphic ages,from the Imjingang belt (Cho et al., 1996, 2001; Reeet al., 1996). The concentration of Permo-Triassicmetamorphic ages in and around the GyeonggiMassif might result from a very strong Permo-Trias-sic tectono-metamorphic event, such as the collisionof the North and South China blocks in the Gyeonggimassif.

The second line of evidence includes the inter-mediate-pressure (IP) metamorphism in both theImjingang and Okcheon metamorphic belts duringPermo-Triassic time with increasing metamorphicgrade toward the collision zone in both belts (north-ward in the Okcheon metamorphic belt and south-ward in the Imjingang belt). In the Okcheonmetamorphic belt, the metamorphic grade increasestoward the northwest from the biotite zone to thestaurolitie zone (Oh et al., 1995, 2004b; Kim et al.,2001; Cheong et al., 2003; Kim, 2005). TheOkcheon metamorphic belt is located 50 km southfrom the Hongseong-Odesan collision belt. Thesedata suggest that the IP metamorphism in theOkcheon metamorphic belt arose from compressioncaused by a distal collision event (Oh et al., 2004b).This suggestion is supported by the widespreadBarrovian type IP metamorphism formed in areaswithin 150 km from the collision boundary in theHimalayan collision belt (Liou et al., 2004; Patrick,

1996). In the Himalaya, the metamorphic gradeincreases towards the collision boundary duringBarrovian IP metamorphism. The Imjingang beltalso underwent Barrovian type IP metamorphismduring the Late Permian (ca. 250–260 Ma; Jeon andKwon, 1999; Cho et al., 2001) and the metamorphicgrade increases toward the south. As the Hong-seong-Odesan collision belt is located to the south ofthe Imjingang belt, the Permo-Triassic metamor-phism in the Imjingang belt also might be a productof an intermediate-pressure metamorphism duringcollision in the area peripheral to the collision zone,as in the Okcheon metamorphic belt. Therefore, thereversed direction of increasing metamorphic gradein both belts towards the Hongseong-Odesan beltduring Permo-Triassic IP metamorphism supportsthe existence of the collision belt within the Gyeo-nggi massif located between the two belts.

Sr, Nd, and Pb isotopic compositions of Cenozoicbasalts analyzed from the islands of Baengnyongdo,Jeongok, Ganseong, and Jeju of Korea (Park et al.,2005), provide the third piece of evidence. Theirlocations are shown in Figure 8A. The Cenozoicbasalts in Jeju Island located south of the Hong-seong-Odesan collision belt show similar isotopiccharacters to those in the South China block,displaying DMM-EM2 mixing, whereas the otherbasalts located to the north of the belt have isotopiccharacters similar to those in the North Chinablocks revealing mixing between DMM and EM1.Park et al. (2005) suggested that the subcontinentallithosphere mantle boundary between the North andSouth China blocks should continue to South Korea,and the Korean continental collision zone may crossthe peninsula through the region between the northand south basalt groups of Korea.

The fourth line of evidence comes from the lateProterozoic igneous and metamorphic eventsrelated to rifting in the northern and southernGyeonggi massif, the Imjingang belt, and Okcheonmetamorphic belt. Igneous ages of ~700 and 800Ma on the northern border of the South China block(Ames et al., 1996; Xue et al., 1997) and ratherweak magmatic activity and metamorphism of ca.800–600 Ma on the southern border of the NorthChina block (Kröner et al., 1993; C. Zhang et al.,1996), correspond to the rifting of the North andSouth China blocks from Rodinia. Along the Hong-seong-Odesan collision belt, the Gyeonggi massifcan be subdivided into northern and southernGyeonggi massifs. A similar age pattern to that inthe borders of the North and South China blocks

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FIG. 8. A. Simplified tectonic map of northeast Asia. B. Simplified geologic map of South Korea showing the Hong-seong-Yangpyeong-Odesan belt, the distribution pattern of Grenvillian ages, Late Proterozoic rifting ages from Rodinia,collision related Paleozoic-Triassic ages and Permian to Cretaceous granitoids (modified from Oh, 2006). The locationsof Pb analysis of Cenozoic basalt are also shown in (A). Abbreviations: OB = Okcheon Belt, Grt = garnet; Zr = zircon; Mo= monazite; Amp = amphibole; WR = whole-rock; Rim = rim age; Ih = inheritance age. The same abbreviations inFigures 1 and 5 are used.

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is seen in the northern and southern Gyeonggimassifs. Igneous and metamorphic ages of 861–742 have been determined in the northern andsouthern parts of the Gyeonggi massif (Kwon et al.,1995; Cho, 2001; Lee et al., 2003a; Guo et al.,2004; Kim et al., 2006). The 742 Ma alkaline A-type granitoid in the northern Gyeonggi massif(Lee et al., 2003a), 756 Ma bimodal volcanism inthe Okcheon metamorphic belt (Lee et al., 1998),and 800 Ma igneous activity in the Imjingnag belt(800 Ma; Cho et al., 2001) occurred as a result ofrifting. These data indicate that the 861–742 Maages in and around the Gyeonggi massif representthe separation of the northern and southern Gyeo-nggi massif from the Rodinian supercontinent asthe southern and northern margins of the North andSouth China blocks, respectively.

Tectonic Relation betweenKorea and Japan

In this section we compare the geology of theHongseong-Odesan belt and surrounding terrains inKorea with possibly correlative belts in Japan. Thegeology of southwestern Japan is characterized bythe Hida and Oki metamorphic belts, and a series ofaccretionary complexes developed at a continentalmargin during early Paleozoic times (e.g., Tsujimoriet al., 2000b; Fig. 9). The Oki metamorphic beltforms the northernmost geotectonic unit of south-west Japan with the Hida belt (Arakawa et al.,2001). The metamorphic rocks in the belt have aCarboniferous–Permian protolith age, a ca. 250 Mametamorphic age, and detrital zircon with Precam-brian ages (up to 3000 Ma) derived from Precam-

FIG. 9. Map showing the geologic and tectonic subdivisions of southwestern Japan (modified after Tsujimori, 2002).The timing of accretion generally gets younger oceanward. Abbreviations: MTL = Median Tectonic Line; I.S.T.L = Itoi-gawa-Shizuoka tectonic time.

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brian basement (Suzuki and Adachi, 1994). Okiamphibolites display a chemical affinity similar tocontinental basalts. The Hida belt is composed ofthe Hida gneiss and Unazuki schist. Their protolithswere suggested to have formed in a continentalshelf-platform setting (Hiroi, 1978, 1983; Sohma etal. 1990). Major and trace element characteristics ofthe igneous rocks in the Hida belt indicate theiremplacement in a continental margin or continentalarc environment (Arakawa et al., 2000). The Hidagneiss experienced two periods of regional meta-morphism: the first at ~350 Ma under granulite-facies conditions, and the second at 240–220 Maunder amphibolite-facies (IP type metamorphism)conditions (Arakawa et al., 2000). The Unazukischist also experienced IP metamorphism. Detritalzircons with Precambrian ages in the Hida gneisses(Sano et al., 2000) point to the Hida belt being con-nected to Precambrian basement, while structuralstudies have shown that the belt and its cratonicmargin were thrust onto the Permian–Jurassicaccretionary complexes as a large nappe (Komatsuand Suwa, 1986; Komatsu et al., 1993).

In the southwestern part of Japan, four HP meta-morphic belts are dispersed in sub-horizontalnappes, in which the older nappes typically occupythe uppermost structural positions. These beltsinclude the ca. 450–400 Ma Oeyama belt, the ca.330–280 Ma Renge belt, the ca. 220–170 Ma Suobelt, and the ca. 90–60 Ma Sambagawa belt (Tsuji-mori et al., 2000b). Ophiolitic peridotite bodieswithin the Oeyama belts are cut by gabbro anddolerite intrusions that display a MORB-like chem-istry. A preliminary Sm-Nd intrusion age of about560 Ma for the gabbro (Hayasaka et al., 1995) indi-cates that the ophiolite formed in the Cambrian. TheFuko Pass metacumulate, which exhibits HP meta-morphism, is exposed as a fault-bounded sheet inthe Oeyama peridotite body. Nishina et al. (1990)obtained hornblende K-Ar ages of 426–413 Ma fromthe metacumulate, which implies that subduction atthe paleo-Pacific margin began in the Silurian(Tsujimori, 1999).

The Carboniferous (330–280 Ma) regional HPRenge metamorphic belt (e.g., Tsujimori and Itaya,1999) is dismembered and is now distributedsporadically throughout the inner zone of southwest-ern Japan (Fig. 9). The Renge belt consists of HPschists of a variety of metamorphic grades includingblueschist-facies metamorphic rocks and glau-cophane-bearing eclogites (Tsujimori and Itaya,1999; Tsujimori et al., 2000a). The Hida marginal

belt is characterized by a serpentinite mélange withhigh-P/T–type Renge blueschists and various frag-ments of Paleozoic accretionary complexes (Tsuji-mori, 2002). The northern area of the Hida marginalbelt is divided into eclogitic and non-eclogitic units.Preliminary phengite 40Ar-39Ar and K-Ar ages fromthe eclogitic unit are 343–348 Ma (Tsujimori et al.,2001), suggesting that the Hida marginal belt repre-sents an eastern extension of the suture zone in east-central China (Tsujimori, 2002; Tsujimori et al.,2006). Permian accretionary complexes (the Aki-yoshi, Maizuru, and Ultratamba belts) form a majorcomponent of the inner zone of southwestern Japan.These geologic settings indicate that the inner partof southwestern Japan was a continental marginwhere a subduction/accretionary complex formedfrom the early to late Paleozoic. Based on these data,the inner part of southwestern Japan is interpretedas an extension of Dabi-Sulu belt formed along theeastern margin of the North China block (Oh, 2006).

The Higo terrain in west-central Kyushu Islandis located at the southernmost end of the inner zoneof southwest Japan (Fig. 9) and consists, from northto south, of the Manotani, Higo, and Ryuhozanmetamorphic complexes, all intruded by the Higoplutonic complex (Karakida, 1992). The highest-grade part in the Higo metamorphic complexpreserves granulite-facies metamorphism (~7.2kbar and ~870°C). In addition, sapphirine- orspinel-bearing granulites preserved as blocks inperidotite intrusions show UHT-metamorphic condi-tions of ~9.0 kbar and ~950°C (Osanai and Kagami,1998; Osanai et al., 2006). The main metamorphicage of the complexes is Permo-Triassic (~250 Ma;Osanai and Kagami, 1998). The Higo metamorphiccomplex has been traditionally considered to be thewestern end of the Ryoke metamorphic belt or partof the Kurosegawa–Paleo Ryoke terrane. However,recent detailed studies including determination ofPermo-Triassic ages (~250 Ma) from this complexsuggest that the Dabie-Sulu collisional belt in Chinacould be extended to the Higo metamorphic com-plex through Korea (Osanai et al., 2006).

In the Odesan area (the eastern part of theGyeonggi Massif on the Korea Peninsula) spinelgranulite adjacent to a late Paleozoic collision-related mangerite intrusion contains the UHTassemblage Spl + Crd + Crn. Spinel and cordieritecompositions indicate peak metamorphic P-T condi-tions of 914–1157°C and 9.0–10.6 kbar (Oh et al.,2006a). Metamorphic zircon overgrowths in thespinel granulite and enclosing migmatitic gneiss,

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dated by SHRIMP U-Pb methods, yield Permo-Triassic ages of 245 ± 10 and 248 ± 18 Ma respec-tively, consistent with the metamorphism being aproduct of the late Paleozoic collision between theNorth and South China blocks within South Korea(Oh et al., 2006a). The age and P-T conditions ofspinel granulite in the Odesan area are similar tothose of sapphirine- or spinel-bearing granulite inthe Higo terrane (250 Ma, >950°C at 8–9 kbar).There is a close association between UHT metamor-phism and continent-continent collision (Osanai etal., 2004; Tamashiro et al., 2004). Therefore, theoccurrence of Late Permian (around 250 Ma) UHTmetamorphic rocks in both the Odesan and Higoareas is good evidence to support the continuation ofthe Dabie-Sulu collision zone into the inner part ofsouthwestern Japan through the Hongseong-Odesancollision zone as suggested by Oh (2006).

Discussion

In the early Paleozoic, three Tethyan oceanbasins opened northward with rifting of three conti-nental slivers from eastern Gondwana (Metcalfe,1996). During these events, the North and SouthChina blocks moved northward with other micro-blocks such as Qaidam, Qinling, and Dabie blocks,and Tethys was consumed by subduction. An activemargin formed along the southern and easternboundaries of the North China block from theOrdovician, and a passive margin developed alongthe northern margin of the South China block (Fig.10A). The Qaidam and North Qinling micro-blockslocated between North and South China blocks col-lided with the southern boundary of the North Chinablock during the Devonian. After the collision,North Qinling became the new southern margin ofthe North China block and a new active marginformed along the new margin. Finally, the North andSouth China blocks collided during the Permo-Triassic (Figs. 10C–10D). Subduction and collisionalong the southern and eastern boundary of theNorth China block formed the Ordovician to Per-mian accretionary complex and a HP belt now occu-pying the southern and eastern borders of the NorthChina block. This complex is represented by ophio-lites, arc complexes, and eclogites in and around theQinling-Dabie-Sulu and Hongseong belts, and alsoby Ordovician–Carboniferous HP metamorphicbelts and accretionary complexes in Japan (Fig. 11).The Hida and Oki belts in Japan were an Ordovi-cian–Carboniferous continental margin of the North

China block (Isozaki, 1997; Arakawa et al., 2000,2001).

The 297–268 Ma HP metamorphism in theHongseong area and 257 Ma collisional mangeritein the Odesan area in Korea indicate that the colli-sion started in the Early to Middle Permian in Korea(Fig. 10B). This confirms suggestions that suturingof the North and South China blocks started duringthe Permian in the east and propagated westward(Zhao and Coe, 1987; Zhang, 1997). During the ini-tial stage of collision, subduction was still occurringin China and Japan along the borders of the NorthChina block as represented by the Permian subduc-tion complexes in the Dabie-Sulu collision zone andthe inner zone of southwest Japan (Akiyoshi,Maizuru, and Ultratamba belts). This configurationindicates that the eastern border of the South Chinablock corresponded with the eastern margin of SouthKorea. At the same time, the Carboniferous–Permian subduction complex in the Yanji belt on thenortheastern border of the North China block (Sao etal., 1995) can be correlated with the Renge subduc-tion complex in the Hida marginal belt, and areparts of a Dabie-Sulu-Hongseong-Higo-Hida-Yanjibelt, encircling the south and east borders of theNorth China block (Fig. 11).

The sinistral movement of the Tanlu fault wasinitiated at 258–248 Ma as a result of westwardpropagation of the collision between the North andSouth China blocks. It continued until the LateTriassic (231–213 Ma) (Figs. 10C and 10D). Aboutthe same time (230–210 Ma) a NE-striking dextralshear zone developed in the Hida marginal, Aki-yosh, and Maizuru belts along the inner zone ofsouthwestern Japan (Takagi and Hara, 1994, Otoh etal., 2003; Otoh and Yanai, 1996). Considering therotation of Japan during the opening of East Sea, theoriginal trend of the Triassic dextral strike-slip faultin Japan may have been N-S. In the tectonic recon-struction of Yin and Nie (1993), the dextral Honamshear zone formed as a western counterpart of thesinistral Tanlu fault when the eastern part of theSouth China block moved northward by about 500km during the collision. On the other hand, theTriassic dextral shear zone in southwest Japan wasregarded as an eastward extension of dextral Honamshear zone in Korea (Yanai et al., 1985). However,the Honam shear zone started to develop in theMiddle Jurassic (Cho et al., 1999; Lee et al., 2003b)and therefore it cannot be a counterpart of the Tanlufault or an extension of the Triassic dextral shearzone in southwest Japan. The Triassic dextral shear

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FIG. 10. The collision process between South and North China blocks (modified from Oh, 2006). A. An active marginwas formed by subduction around the North China block during the mid-Paleozoic; at the same time, a passive marginwas developed around the northern boundary of the South China block. B. The collision started in Korea during thePermian. C. It propagated into the Shandong Peninsula, producing the sinistral Tanlu fault and dextral fault in the Hidabelt along the way. During the collision, the western portion of the North and South China blocks moved southward, alongwith Japan, while the Shandong and Korea peninsulas moved northward. D. The collision terminated during the Triassic.E. After regional intrusion of Jurassic granitoids in Korea Peninsula, the Hida belt was thrust over the inner zone ofsouthwest Japan, while additional Jurassic and Cretaceous accretionary complexes added to Japan. Abbreviations: NCB= North China block; SCB, South China block; QB = Qinling block; YB = Yangtze block; CB = Cathaysia block: BY =Bureya; NK = Northern Korea; SK = Southern Korea; HB = Hida belt; ISWJ = Inner zone of Southwest Japan.

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zone in the inner zone of southwest Japan is likely tobe paired with the Tanlu fault. Along the fault, theKorean Peninsula moved northward, while theOrdovician–Carboniferous subduction complex inJapan moved southward. More studies will beneeded to confirm the dextral fault between Koreaand Japan (Figs. 10C and 10D).

As mentioned elsewhere in this paper, 1034–935Ma Sm-Nd ages have been reported from ophiolitesin the suture zone between the Yangtze and theCathaysia blocks in the South China block (Chen etal., 1991). The suture zone in the South China blockwas reactivated as a rift at 820–750 Ma duringthe breakup of Rodinia (Li et al., 1999). Similarpatterns are observed in and around the Okcheonmetamorphic belt; 1198–960 Ma ages have beenobtained from gneisses and granite around theOkcheon metamorphic belt (Lee et al., 1992, 1994;Sagong et al., 2003; Kim et al., 2005) and rift-related 756 Ma bimodal volcanism occurred in theOkcheon metamorphic belt (Lee et al., 1998; Fig. 8).The igneous and metamorphic ages of ~2100–1400

Ma in the Yeongnam massif (Oh et al., 2000) can becorrelated with 1900–1400 Ma ages from theCathaysia block reported by Li et al. (1995). Thesedata indicate that the Okcheon metamorphic beltcan be correlated with the suture zone between theYangtze and Cathaysia blocks that was subsequentlyreactivated as a failed rift (Figs. 4 and 11). Giventhat the Dabie-Sulu collision belt is now correlatedwith the Hongseong-Odesan belt, the South Gyeo-nggi massif and Yeongnam massif in South Koreacan be matched with the Yangtze and Cathaysiablocks in China, respectively, whereas the NorthGyeonggi massif is matched with the Sino-Koreanblock (North China block; Fig. 11).

Across the Dabie-Sulu-Hongseong-Odesan belt,the metamorphic conditions of peak and retrogrademetamorphism change systematically from east towest. The pressure and temperature for peak meta-morphism increases and decreases, respectively,from the Odesan area to the Dabie area, resulting inUHT metamorphism in the Odesan and Higo areas,HP metamorphism in the Hongseong area, and UHP

FIG. 11. Tectonic map of northeastern Asia showing the tectonic relationships between Korea, China, and Japan,along with the distribution of Permian–Triassic eclogites, collisional igneous activity, and UHT rocks (revised from Oh,2006). Abbreviations: HG = Higo area. Other abbreviations are the same as those used in Figures 1 and 6.

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metamorphism at the Dabie and Sulu areas (Fig. 12;Liou et al., 1996; Oh et al., 2005; Oh et al., 2006a).The metamorphic condition for the first-stage retro-grade metamorphism decreases from UHT metamor-phic conditions in the Odesan area throughgranulite facies in the Hongseong area to mainlyamphibolite facies in the Sulu and Dabie areas. As aresult, the P-T paths of the four areas are as shownin Figure 12, which represent an increase in geo-thermal gradient and a decrease of the uplift ratefrom west to east. This difference may be mainlyrelated to an increasing distance between the Northand South China blocks before collision toward thewest, which increased the amounts of subductedoceanic crust in the west.

The largest amount of subducted oceanic crust inthe west, the Dabie and Sulu areas, caused thestrongest pulling force, resulting in the deepest sub-duction of the South China block to UHP conditiondepths, while the oceanic and continental crusts inthe east part, in the Hongseong area, could reachonly to HP condition depths. The Tanlu fault in theDabie and Sulu areas facilitated subduction of moreoceanic crust to deeper depth. The buoyancy forceincreases as the subduction depth increases, and

stronger buoyancy causes faster uplift. As a result,the time span between subduction and upliftincreased to the east, resulting in more time ofthermal relaxation and higher geothermal gradientsduring the retrograde metamorphic stage. Thedelamination of oceanic curst occurred in the finalstages of continental collision and exposed the sub-ducted continental crust or lower continental crustto the asthenosphere, which supplied high heat flowto them. The slower uplift in the eastern partexposed the subducted continental crust and lowercontinental crust for longer heating times. Through acombination of the most thermal relaxation and mostexposure time to the high thermal gradients from theasthenosphere in the east, the Odesan and Higoareas experienced UHT metamorphism.

Conclusions

1. The Dabie-Sulu collision belt in Chinaextends to the Hongseong-Odesan belt in Korea.

2. The collision between the North and SouthChina blocks started in Korea during the earlyPermian (297–268 Ma). It propagated westwarduntil 258–225 Ma, creating the sinistral Tanlu fault.

FIG. 12. Average P-T paths of eclogites from Dabie and Sulu collision belt in China (Liou et al., 1996), P-T paths ofeclogites from Hongseong belt (Oh et al., 2005), and spinel granulite in Odesan area in Korea (Oh et al., 2006a).

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3. Phanerozoic subduction along the margin ofthe North China block and the collision between theNorth and South China blocks contributed to forma-tion of the Dabie-Sulu-Hongseong-Odesan-Higo-Hida-Yanji belt.

Acknowledgements

This study was supported by a grant from theKorea Science and Engineering Foundation (R05-2004-000-10962-0) and Chonbuk National Univer-sity (2005 Overseas Research Professor Program).We thank Drs. S.W. Kim, V. J. Rajesh (ChonbukNational University), and S. Krishan (Okayama Uni-versity of Science, Japan) for microprobe andgeochemical analysis and important comments andMs. C. S. Kim for preparing the figures.

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