An Unrecognized Major Collision of the Okhotomorsk Block with East Asia During the Late Cretaceous, Constraints on the Plate Reorganization of the Northwest Paciﬁc

Home , Izanagi Plate, Taihang Mountains, Xuefeng Mountains, Yin Mountains

Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115

Contents lists available at ScienceDirect

Earth-Science Reviews

journal homepage: www.elsevier.com/locate/earscirev

An unrecognized major collision of the Okhotomorsk Block with East Asia during the Late Cretaceous, constraints on the plate reorganization of the Northwest Paciﬁc

Yong-Tai Yang ⁎

CAS Key Laboratory of Crust–Mantle Materials and Environments, School of Earth and Space Sciences, University of Science and Technology of China, Hefei 230026, China article info abstract

Article history: Interactions at plate boundaries induce stresses that constitute critical controls on the structural evolution of Received 28 February 2013 intraplate regions. However, the traditional tectonic model for the East Asian margin during the Mesozoic, invoking Accepted 30 July 2013 successive episodes of paleo-Pacific oceanic subduction, does not provide an adequate context for important Late Available online 8 August 2013 Cretaceous dynamics across East Asia, including: continental-scale orogenic processes, significant sinistral strike- slip faulting, and several others. The integration of numerous documented field relations requires a new tectonic Keywords: model, as proposed here. The Okhotomorsk continental block, currently residing below the Okhotsk Sea in Continental collision Continental transform boundary Northeast Asia, was located in the interior of the Izanagi Plate before the Late Cretaceous. It moved northwest- East Asia ward with the Izanagi Plate and collided with the South China Block at about 100 Ma. The indentation of the Northwest Pacific Okhotomorsk Block within East Asia resulted in the formation of a sinistral strike-slip fault system in South China, Okhotomorsk Block formation of a dextral strike-slip fault system in North China, and regional northwest–southeast shortening and Late Cretaceous orogenic uplift in East Asia. Northeast-striking mountain belts over 500 km wide extended from Southeast China to Southwest Japan and South Korea. The peak metamorphism at about 89 Ma of the Sanbagawa high- pressure metamorphic belt in Southwest Japan was probably related to the continental subduction of the Okhotomorsk Block beneath the East Asian margin. Subsequently, the north-northwestward change of motion direction of the Izanagi Plate led to the northward movement of the Okhotomorsk Block along the East Asian margin, forming a significant sinistral continental transform boundary similar to the San Andreas fault system in California. Sanbagawa metamorphic rocks in Southwest Japan were rapidly exhumed through the several- kilometer wide ductile shear zone at the lower crust and upper mantle level. Accretionary complexes successively accumulated along the East Asian margin during the Jurassic–Early Cretaceous were subdivided into narrow and subparallel belts by the upper crustal strike-slip fault system. The departure of the Okhotomorsk Block from the northeast-striking Asian margin resulted in the occurrence of an extensional setting and formation of a wide magmatic belt to the west of the margin. In the Campanian, the block collided with the Siberian margin, in Northeast Asia. At about 77 Ma, a new oceanic subduction occurred to the south of the Okhotomorsk Block, ending its long-distance northward motion. Based on the new tectonic model, the abundant Late Archean to Early Proterozoic detrital zircons in the Cretaceous sandstones in Kamchatka, Southwest Japan, and Taiwan are interpreted to have been sourced from the Okhotomorsk Block basement which possibly formed during the Late Archean and Early Proterozoic. The new model suggests a rapidly northward-moving Okhotomorsk Block at an average speed of 22.5 cm/yr during 89–77 Ma. It is hypothesized that the Okhotomorsk–East Asia collision during 100–89 Ma slowed down the northwestward motion of the Izanagi Plate, while slab pull forces produced from the subducting Izanagi Plate beneath the Siberian margin redirected the plate from northwestward to north-northwestward motion at about 90–89 Ma. © 2013 Elsevier B.V. All rights reserved.

Contents

1. Introduction...... 97 2. GeologicalsettingoftheOkhotomorskBlockandJapanIslands...... 98 3. Thenewtectonicmodel...... 103 3.1. ThecollisionoftheOkhotomorskBlockwiththeEastAsianmargin...... 103 3.2. Strike-slipmotionoftheOkhotomorskBlock...... 105

⁎ Tel.: +86 0551 63607193. E-mail address: [email protected].

3.2.1. Thesinistraltransformfaultzone...... 105 3.2.2. Effectsinamuchbroaderregion...... 106 3.2.3. Extensionandmagmatismfollowingthetranspressionalregime...... 107 3.3. ThecollisionoftheOkhotomorskBlockwiththeSiberianmargin...... 108 4. EvidencesofArcheanandEarlyProterozoiczircons...... 108 4.1. U–Pbdatingofdetritalzircons...... 108 4.2. Newinterpretations...... 109 5. EvolutionoftheSanbagawaHPmetamorphicbelt...... 109 6. Discussions...... 110 6.1. TheOkhotomorskBlockbeforetheLateCretaceous...... 110 6.2. Constraints on the plate reorganization of the Northwest PaciﬁcduringtheCNS...... 110 6.3. The Okhotomorsk–EastAsiacollisionandtheEarlyCretaceousandCenozoicextensionaleventsinEastChina...... 111 7. Conclusions...... 112 Acknowledgments...... 112 References...... 112

1. Introduction Tectonic Line (MTL) (Taira et al., 1983; Takagi, 1986; Otsuki, 1992), Tanakura Tectonic Line (TTL) (Taira et al., 1983; Otsuki, 1992), and Cen- Reconstructing tectonic processes operating along the East Asian tral Sikhote-Alin Fault (CSAF) (Zonenshain et al., 1990), etc. (Figs. 1 and margin (Figs. 1 and 2) during the Cretaceous is important for under- 2). Moreover, a series of small NE–SW trending pull apart basins devel- standing the geologic evolution of East Asia, especially in extensive oped in Southeast China during the Late Cretaceous (Charvet et al., intraplate regions, and for constraining plate reconstructions of the 1994; Lapierre et al., 1997; Ma et al., 2009). Structural studies indicated paleo-Pacific Ocean (Engebretson et al., 1985; Lithgow-Bertelloni and that Japan Islands (Taira et al., 1983; Kanaori, 1990; Otsuki, 1992)and Richards, 1998; Smith, 2003; Norton, 2007; Seton et al., 2012), particu- South Korea (Hwang et al., 2008) are subdivided into many blocks by larly during the Cretaceous Normal Superchron (CNS) (125–84 Ma), a strike-slip faults and the Late Cretaceous igneous rocks are mainly dis- time of no magnetic reversals. It is generally accepted that the East tributed around these faults. However, the current oceanic subduction Asian margin has experienced successive oceanic subduction with model is unable to reconcile these ubiquitous strike-slip features with occasional oceanic ridge collision since the Paleozoic (Isozaki, 1996; the subhorizontal internal structure of the crust in SW Japan, as imaged Maruyama et al., 1997; Isozaki et al., 2010). However, a series of geolog- by seismic data (Ito et al., 2009)(Fig. 2c). Because of this, the idea ical events occurred in East Asia during the early Late Cretaceous are of strike-slip-fault-controlled tectonics in Japan (Taira et al., 1983; poorly explained by this successive oceanic subduction model. Kanaori, 1990; Otsuki, 1992)(Fig. 4) has been completely abandoned Many thermochronologic, structural, and stratigraphic studies have (Isozaki et al., 2010). indicated that a continental-scale NW–SE shortening event occurred Other features unaccounted for in the traditional tectonic model in East Asia during the early Late Cretaceous (Charvetetal.,1994; include: ubiquitous thrusting features, high metamorphic pressure and Lapierre et al., 1997; Ratschbacher et al., 2003), which was intervened fast exhumation of Sanbagawa high-pressure metamorphic rocks, and cer- between two widespread extensional episodes in the Early Cretaceous, tain geochemical characteristics of granites in SW Japan (Fig. 2), which and in the latest Cretaceous–Cenozoic, respectively (Watson et al., are best explained by episodic collision and underthrusting of micro- 1987; Ren et al., 2002). During this period, major mountains and basins continents (Charvet, 2013). Although various relatively small-scale conti- were rapidly uplifted and exhumed, including: the Nanling Mountains nental collisional events during the Late Jurassic–Cretaceous have been (NL) (Chen, 2000), Wuyi Mountains (WY) (Chen, 2000), Yellow proposed at the proto-Japan margin (Jolivet et al., 1988; Otsuki, 1992; Mountains (Y) (Zheng et al., 2011), Xuefeng Mountains (XF) (Yan et al., Charvet, 2013) and at the SE China margin (Charvet et al., 1994; Lapierre 2011), Sichuan Basin (SB) (Shen et al., 2009), Qinling–Dabie mountain et al., 1997; Ratschbacher et al., 2003), they were possibly inadequate in belts (QL and DB) (Grimmer et al., 2002; Ratschbacher et al., 2003; scale to produce the aforementioned regional deformations or they were Enkelmann et al., 2006; Cui et al., 2012), Jiaolai Basin (JB) (Zhang et al., not consistent with the deformation time of the early Late Cretaceous. 2003), Luxi Uplift (LU) (Wang et al., 2008), Bohai Bay Basin (BBB) In addition, as the Izanagi and Kula plates in the paleo-Pacific (Xu et al., 2001; Zhu et al., 2012), Taihang Mountains (TH) (Xu et al., Ocean have been wholly subducted and ages of the Pacificseafloor 2001), Lüliang Mountains (LL) (Li and Song, 2010), Ordos Basin (OB) formed during the CNS are unable to be precisely defined, detailed (Zhang et al., 2011), Yan–Yin mountain belts (YIN and YAN) (Wu plate reorganization of the Pacific Ocean in this period has still remained and Wu, 2003a,b), Changbai Mountains (CB) (Li et al., 2010), Songliao uncertain. The prevailing model (Engebretson et al., 1985), on the basis Basin (SLB) (Feng et al., 2010), and Great Xing'an Mountains (GX) (Li of hotspots, magnetic anomalies, and fracture zones in the north Pacific et al., 2011) in China; East Gobi Basin (EGB) in Mongolia (Graham Basin, suggested that the Izanagi Plate moved north-northwestward et al., 2001; Johnson, 2004); Sikhote-Alin Fold Belt (SAFB) in Russia to northward relative to the Eurasian Plate at a speed of more than (Zonenshain et al., 1990) and Sanjiang-Middle Amur Basin (SMAB) in 20 cm/yr between 135 and 85 Ma (Fig. 4). Smith (2003, 2007) the China–Russia border region (Kirillova, 2003); Gyeongsang (GB) suggested that the E–WorientedIzanagi–Pacific ridge was located just and other basins in South Korea (Choi and Lee, 2011); and Ryoke meta- to the north of Australia during 130–100 Ma and rapidly moved north- morphic belt in Japan (Kamp and Takemura, 1993; Okudaira et al., ward to a location beside NE Asia between 100 and 84 Ma. Primarily 2001), etc. (Figs. 1–3). Furthermore, the uplift of northeast-striking using fracture zone and magnetic isochron data of the PacificBasin, mountain ranges in East Asia appears to have blocked moist ocean air Norton (2007) proposed that a significant reorganization occurred at into the interior of the continent, resulting in the deposition of red clas- the boundary between the Farallon and Izanagi plates at about 90 Ma, tic sediments and eolian sands in China and Mongolia during the Late followed by a total change of about 35° from northwestward at about Cretaceous (Chen, 2000; Hasegawa et al., 2009; Ma et al., 2009). 90 Ma to northward at 71 Ma in the direction of Pacific–Izanagi motion. The East Asian margin was characterized by large-scale sinistral The global plate dynamics model (Lithgow-Bertelloni and Richards, strike-slip movements during the early Late Cretaceous. Major examples 1998) also suggested a rapidly north-northwestward to northward- include the Lishui Fault (LF) (Chen, 2000), Changle-Nanao Fault (CNF) moving Izanagi Plate during the CNS. However, a recent global plate (Charvetetal.,1994), Tanlu Fault (TLF) (Zhang et al., 2003), Median motion model (Seton et al., 2012) proposed that the Izanagi Plate Earth-Science Reviews 126 (2013) 96–115

Fig. 1. Topographic and tectonic map of East Asia, with an inset of the enlarged Nanling Mountains at the lower right. Mountain belts, CB: Changbai Shan; DB: Dabie Shan; DL: Dalou Shan; GX: Great Xing'an Mountains; LL: Lüliang Shan; LU: Luxi Uplift; NL: Nanling Mountains; QL: Qinling Mountains; SAFB: Sikhote-Alin Fold Belt; TH: Taihang Shan; WY: Wuyi Shan; XF: Xuefeng Shan; Y: Yellow Shan; YAN: Yan Shan; YIN: Yin Shan. Basins, BBB: Bohai Bay Basin; EGB: East Gobi Basin; GB: Gyeongsang Basin; HB: Hengyang Basin; JB: Jiaolai Basin; JHB: Jianghan Basin; MB: Mayang Basin; OB: Ordos Basin; SB: Sichuan Basin; SLB: Songliao Basin; SMAB: Sanjiang-Middle Amur Basin; SYB: Subei-Yellow Sea Basin. Strike-slip faults, CNF: Changle-Nanao Fault; CSAF: Central Sikhote-Alin Fault; LF: Lishui Fault; MTL: Median Tectonic Line; SF: Shangyi-Gubeikou-Pingquan Fault; SKTL: South Korean Tectonic Line; TF: Taiyingzhen-Lengkou-Shangying Fault; TLF: Tanlu Fault; TTL: Tanakura Tectonic Line; ZLF: Ziyun-Luodian Fault. moved in a westward direction during the Cretaceous and the Izanagi– (Pavlenkova et al., 2009) and currently resides below the Okhotsk Paciﬁc ridge intersected the East Asian margin in a sub-parallel ori- Sea (Fig. 1). Because there is another small continental block in the entation during the early Eocene. Onshore geological records, such Okhotsk–Chukotka volcanic belt called the Okhotsk Massif or Okhotsk as orogenic uplift events, major faulting events, basin stratigraphy, Terrane (Zonenshain et al., 1990; Stone et al., 2003), the present metamorphism, and magmatism, probably provide important infor- study follows Parfenov and Natal'in (1986) and uses the name of mation for assessing how widespread plate motion changes were Okhotomorsk Block for the continental block below the Okhotsk Sea. during the CNS (Matthews et al., 2012). The consolidated basement of the Okhotomorsk Block is covered by A new tectonic model is proposed here for the evolution of the East the Late Cretaceous–Cenozoic sediments 1–12 km thick and has not Asian margin during the Late Cretaceous. This model links various, been encountered by drilling (Chekhovich et al., 2009). The Sredinny seemingly isolated, geologic events, explains many controversial Massif in Kamchatka (Fig. 1) has been thought to be the eastern geologic problems in East Asia, and provides a much-needed context part of the block (Parfenov and Natal'in, 1986; Jolivet et al., 1988; for plate reconstruction of the paleo-Paciﬁc Ocean during the CNS. Bindeman et al., 2002). As the high-grade metamorphosed massif contains abundant Archean to Early Cretaceous detrital zircon cores 2. Geological setting of the Okhotomorsk Block and Japan Islands which underwent the ubiquitous episode of 77 Ma overgrowth (Figs. 3 and 5a), it was interpreted as a product of regional metamorphism The Okhotomorsk Block (Parfenov and Natal'in, 1986; Şengör and and migmatization of a siliciclastic sedimentary protolith during the Natal'in, 1996), also called the Okhotsk Block (Jolivet et al., 1988; Late Cretaceous (Bindeman et al., 2002). The collisional event of the Otsuki, 1992), has a continental crust of over 20 km in thickness Okhotomorsk Block with the Siberian margin north of the Okhotsk Sea Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115 99 (a)

(b)

(c)

Fig. 2. (a) Basement geologic map of Japan Islands (modiﬁed from Taira et al., 1983; Isozaki, 1996; Taira, 2001; Isozaki et al., 2010; Wakita, 2013). (b) Detailed geologic map of Shikoku (after Taira et al., 1988; Aoki et al., 2011, 2012). (c) Cross section across SW Japan (after Ito et al., 2009). occurred by the end of the Cretaceous, causing the cessation of magmatic terrane to Asia and moved northward with the Izanagi Plate or the Kula activity in the Okhotsk-Chukotka arc (Parfenov and Natal'in, 1986; Plate in the Mesozoic (Parfenov and Natal'in, 1986; Jolivet et al., Jolivet et al., 1988; Bindeman et al., 2002; Chekhovich et al., 2009) 1988; Otsuki, 1992). Before its collision with Siberia, it collided with (Figs. 1 and 3). Seismic tomographic data (Bijwaard et al., 1998; NE Japan during the Late Jurassic-Early Cretaceous (Jolivet et al., 1988), Gorbatov et al., 2000) show a high-velocity zone dipping to the north- or moved along the trench to the east of Japan during the Early Creta- west to a depth of 660 km beneath the northern Sea of Okhotsk, indicat- ceous (Otsuki, 1992)(Fig. 4). Others argued that the block was an ex- ing subduction of the Okhotomorsk Block beneath the Siberian margin. pelled fragment as a result of the scissor-like closure of the Mongol– It was also suggested that the Okhotomorsk Block collided with Sakhalin Okhotsk Ocean during the Early Mesozoic (Şengör and Natal'in, 1996; Island during the Paleogene, forming westward convergent structures Bindeman et al., 2002)(Fig. 1). in NE Japan and Sakhalin (Otsuki, 1992; Maruyama et al., 1997; Taira, The geological units of Japan Islands are classiﬁed by origin of forma- 2001)(Fig. 1). However, debates have been arisen over the origin of tion mainly into the Paleozoic non-accretionary belts (Hida, Oki, South the Okhotomorsk Block before its collision with Siberia during the Late Kitakami, and Kurosegawa), accretionary complexes of Carboniferous Cretaceous. Some researchers suggested that the block was an exotic to Paleogene age, and the Cretaceous Sanbagawa high-pressure 100 Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115

Fig. 3. A brief summary of events occurred in East Asia during the Late Cretaceous, including: exhumation, sedimentation, deformation, accretion, mylonitization, and magmatism. The collision of the Okhotomorsk Block within East Asia resulted in the onset of rapid cooling and exhumation in South China, North China, East Mongolia, South Korea, and SW Japan at about 100–96 Ma. The collision and subsequent strike-slip movement of the Okhotomorsk Block resulted in the hiatus of accretionary activity in SW Japan from the late Cenomanian to the Santonian (about 96–83 Ma). The oblique movement of the Okhotomorsk along the NE-striking Asian margin during 89–83 Ma caused a rapid exhumation of Sanbagawa HP metamorphic rocks and mylonitization along the MTL in SW Japan, and rapid uplifting and compressive deformation in NE Japan, SE Russia and NE China. After the Okhotomorsk Block passed the NE-striking Asian margin at about 83 Ma, an extensional setting occurred in SW Japan, leading to the formation of the Izumi Basin to the west of the MTL. At about 79 Ma, the Okhotomorsk Block collided with the Siberian margin, resulting in the cessation of arc magmatism in the Okhotsk-Chukotka volcanic belt. At about 77 Ma, the Izanagi oceanic lithosphere began to subduct beneath the Okhotomorsk from the south, causing magmatism, regional metamorphism, and accumulation of the late Campanian marine clastic sediments along the southern and eastern margins of the Okhotomorsk. metamorphic belt (Taira et al., 1983; Isozaki, 1996; Taira, 2001; Isozaki arc or microcontinent) which moved with the Izanagi plate and collided et al., 2010; Wakita, 2013)(Fig. 2a). The Hida and Oki belts consist with proto-Japan in the Late Jurassic–Early Cretaceous (Otsuki, 1992; mainly of Paleozoic sedimentary and metamorphic rocks which were Kato and Saka, 2003; Charvet, 2013)(Fig. 4). The hundreds-kilometer deposited along the Asian continental margin during the Middle-Late long and several-kilometer wide Kurosegawa Belt in SW Japan consists Paleozoic time and were subjected to metamorphism during the of a series of lenses of Paleo-Mesozoic granitic, metamorphic, and shal- Carboniferous–Early Triassic, forming the core of the Phanerozoic growth low marine sedimentary rocks surrounded by serpentinite (Taira et al., of Japan Islands (Isozaki, 1996; Isozaki et al., 2010; Wakita, 2013). The 1983; Maruyama et al., 1984; Wakita, 2013). It separates the Chichibu South Kitakami Belt in NE Japan consists of Paleo-Mesozoic igneous Belt into the North Chichibu Belt, an Early-Middle Jurassic accretionary and metamorphic rocks, and shallow marine continental shelf deposits complex, and the South Chichibu Belt, a Middle Jurassic–earliest Creta- of Silurian to Jurassic age (Isozaki, 1996; Wakita, 2013). It was interpreted ceous accretionary complex (Hada et al., 2001; Ishida et al., 2003)(Fig. as a tectonic outlier of the South China Block continental margin 2). The Chichibu Belt and the intervening Kurosegawa Belt as a whole (Isozaki, 1996), while others deﬁned it as an exotic landmass (island thrust over the Cretaceous Shimanto accretionary complexes above Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115 101

(a) 140-130 Ma (b) 130-115 Ma

Fig. 4. Tectonic sketch map of Japan in (a) 140–130 Ma, (b) 130–115 Ma, (c) 115–85 Ma, and (d) 85–53 Ma (after Otsuki, 1992). the Butsuzo Tectonic Line (BTL) (Kato and Saka, 2003; Ito et al., 2009; Paleogene age (Isozaki, 1996; Isozaki et al., 2010)(Fig. 2a). The Ryoke Charvet, 2013)(Fig. 2). A number of models have been proposed for high-temperature metamorphic belt to the north of the MTL was a prod- the origin of the Kurosegawa Belt. It was interpreted as a strike-slip mo- uct of plutonometamorphism of the Jurassic accretionary complex during bile zone along which basement rocks of continental margin or island the mid-Cretaceous (Nakajima, 1994; Suzuki and Adachi, 1998; Wakita, arc were tectonically sliced and transported (Taira et al., 1983), an exot- 2013).TheRyokeBeltisunconformablycoveredbytheLateCretaceous ic landmass which collided with proto-Japan in the Late Jurassic–Early elongate clastic basin, Izumi Group, while under them there is a major Cretaceous (Maruyama et al., 1984; Otsuki, 1992; Charvet, 2013) upper crustal-scale half-graben, the Seto Subsurface Prism (SSP) (Ito (Fig. 4a), or a far-travelled klippe-like tectonic outlier of the South et al., 2009)(Fig. 2c). The Cretaceous Shimanto accretionary prism is sep- China Block continental margin (Isozaki, 1996). arated from the Jurassic–earliest Cretaceous accretionary prism by the Nearly 80% of basement rocks in Japan consist of ancient accretionary BTL and has two sub-belts, the Lower Cretaceous sub-belt to the north complexes which young oceanward from Carboniferous–Triassic to and the Upper Cretaceous sub-belt to the south (Taira et al., 1988) 102 Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115 (a)

(b)

(c)

Fig. 5. Age distribution pattern of detrital zircons in (a) Sredinny Massif, Kamchatka, (b) SW Japan, with locations in Fig. 2 except the sample KRB-1, and (c) Taiwan. Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115 103

(Fig. 2b). The Lower Cretaceous sub-belt consists of Neocomian to towards Eurasia during the Jurassic–Early Cretaceous (Otsuki, 1992) Cenomanian clastics (Figs. 2band3)andistightlyfolded.Taira et al. (Fig. 4a). The South Kitakami Belt and Kurosegawa Belt collided with (1988) suggested that this sub-belt was probably a transform fault zone proto-Japan at about 140 Ma (Otsuki, 1992; Charvet, 2013), but at the along the Asian margin before the accretion of the southern sub-belt same time the Okhotomorsk Block moved northward along the trench during the Campanian. The Upper Cretaceous sub-belt is composed of at the East Asian margin (Otsuki, 1992). However, the model proposed Late Jurassic–Early Cretaceous basalt, nannofossil-bearing limestone, here suggests that the Okhotomorsk Block arrived at the East Asian and radiolarian chert; Cenomanian–Santonian pelagic shale, hemipelagic margin at about 100 Ma much later than the South Kitakami Belt and shale, and acidic tuff; and Campanian trench clastic rocks (Taira et al., the Kurosegawa Belt did at about 140 Ma (Otsuki, 1992; Charvet, 1988; Taira, 2001). The Early Cretaceous pillow lavas and nannofossils 2013), and it first collided with the South China Block during the early formed at equatorial latitude, but the Campanian turbidite units were Late Cretaceous. deposited approximately at their present latitude, suggesting that the At about 100 Ma, the Okhotomorsk Block moved with the Izanagi oceanic crust moved north at least 3000 km in the mid-Cretaceous and Plate in a direction of N35°W (Norton, 2007) and collided with the was rapidly subducted and accreted along the Asian margin during the South China Block at the East Asian margin (Fig. 6). Between 100 and Campanian time (Taira et al., 1988; Taira, 2001)(Figs. 2band3). 89 Ma, the northwestward-advancing Okhotomorsk Block caused the The Sanbagawa Belt (Fig. 2a), extending SW–NE for more than formation of a sinistral strike-slip fault system in the southern South 800 km from Central to SW Japan, is composed of rocks subjected China Block (Fig. 7a). An Early Eocene reconstruction of SE Asia shows to high-pressure type metamorphism of pumpellyite–actinolite facies that before opening of the South China Sea there was a large concavity through blueschist transition facies, to epidote–amphibolite and eclogite at the Asian margin to the southeast of Taiwan (Hall, 2002)(Fig. 1), facies (Aoki et al., 2011). It has been traditionally defined to be a typical which, according to the new model, corresponds to the southern oceanic subduction-related high-pressure metamorphic belt whose indenter corner formed during the collision. Topographically, there are protolith was a Jurassic–Early Cretaceous accretionary prism accumu- three NW-trending linear low-lying lines across the Nanling Mountains lated in a shallow part of the trench (Isozaki and Itaya, 1990; Isozaki, (NL) (Fig. 1). A series of small pull-part basins were formed beside them 1996; Maruyama et al., 1997; Isozaki et al., 2010; Aoki et al., 2011). and filled with red clastic sediments interbedded with basalts of 96 Ma However, recently, it was recognized that protoliths of many metamor- (Chen, 2000; Shu et al., 2004; Ma et al., 2009)(Fig. 3). The Ziyun– phic rocks in the traditional Sanbagawa Belt formed as an accretionary Luodian Fault (ZLF) to the south of the Sichuan Basin (Fig. 1) was a complex after 90–80 Ma and suffered a progressive metamorphism major normal fault during the Paleozoic–Triassic (Ma et al., 2009). It during about 80–60 Ma (Aoki et al., 2011; Itaya et al., 2011). They were separated from the Sanbagawa Belt and were named as the 500 km Shimanto metamorphic belt (Aoki et al., 2011)(Fig. 2b). 100 Ma Zircon U–Pb dating of the meta-sandstone (QM) intercalated with eclogite of the Sanbagawa Belt in central Shikoku yields an age of 132– 112 Ma for rims which grown around older cores mainly of the latest Jurassic–earliest Cretaceous age (Okamoto et al., 2004)(Figs. 2band 5b). This study has become a major basis for the suggestion that the peak metamorphism of the Sanbagawa Belt in eclogite facies occurred Eurasia during 120–110 Ma (e.g. Isozaki et al., 2010; Aoki et al., 2011; Itaya et al., 2011). However, based on a garnet–omphacite Lu–Hf isochron Izanagi Plate age of 89–88 Ma for the Sanbagawa Belt in Shikoku, Wallis et al. (2009) suggested a peak metamorphism exceeding 1.8 GPa at about 89 Ma and an extreme rapid exhumation of at least 2.5 cm/yr during

89–85 Ma. Before the belt was exposed at about 50 Ma, it experienced GB a much slower exhumation at middle crustal levels. In addition, interest- ingly, the Sanbagawa Belt was imaged by seismic data to be a several-kilometer wide, gently north-dipping belt which extends from the upper crust to a depth of about 30 km to the south of the MTL (Ito et al., 2009)(Fig. 2c). Presumed location of Although the Sanbagawa Belt has long been ascribed as an oceanic the Kurosegawa Belt subduction-related high-pressure metamorphic belt, Charvet (2013) proposed that the oceanic subduction model is unable to explain the high peak metamorphic pressure of 2.9 to 3.8 GPa of the Higashi–Akaishi peri- Okhotomorsk dotite body in the Sanbagawa Belt (Enami et al., 2004; Ota et al., 2004) (Fig. 2b), which was most likely formed in a collisional orogen. According to Guillot et al. (2009), the maximum pressures recorded in exhumed metamorphic rocks formed in the accretionary-type subduction scenario vary from 0.7 to 2.0 GPa. In addition, it was suggested by Charvet (2013) that the fast exhumation of at least 2.5 cm/yr of the Sanbagawa Belt during 89–85 Ma (Wallis et al., 2009) could not be achieved in the accretionary-type subduction setting in which the exhumation rates gen- Izanagi motion direction Continental-oceanic Magma invasion erally range between 1 and 5 mm/yr (Guillot et al., 2009). (Norton, 2007) convergent boundary and eruption

3. The new tectonic model Undifferentiated Successive nonmarine Marine sedimentation nonmarine basins sedimentation on continent 3.1. The collision of the Okhotomorsk Block with the East Asian margin and erosion areas

Fig. 6. Paleogeographic map of East Asia at about 100 Ma. GB: Gyeongsang Basin. The It was suggested that the Okhotomorsk Block, South Kitakami Belt, Okhotomorsk Block moved with the Izanagi Plate in a direction of N35°W and collided and Kurosegawa Belt all derived from the Izanagi Plate and migrated with the South China Block at the East Asian margin. 104 Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115

(a) basins (Fig. 7a). The southernmost major fault, along the main valley of the Pearl River, propagated northwestward, forming the ZLF on the Paleozoic weak zone. The collisional event produced a dextral strike-slip fault system from JapantoNorthChina(Fig. 7a). Paleographic reconstructions of Japan show that prior to large-scale sinistral strike-slip faulting in NE Japan in the mid-Cretaceous there was a large concavity at the continental margin between SW and NE Japan (Otsuki, 1992)(Fig. 4b), which may correspond to the northern indenter corner. A major dextral strike- slip fault may have initiated at the corner and propagated northwestwards through the Changbai Mountains to the northern margin of the North China Block, creating the big bend at the northeastern end of the Jiao-Liao-Ji Belt (Zhao et al., 2005). Due to the resistance of the Amurian Microcontinent to the northwestward propagation of this fault, dextral strike-slip movement occurred along the E–W-striking marginal fault of the North China Block. Another northwest-trending dextral strike-slip fault belt may have originated from the Korean Peninsula and propagated to the southern Yan Mountains, where major dextral strike-slip faults were active during the Cretaceous, such as Shangyi-Gubeikou-Pingquan Fault (SF) and Taiyingzhen- Lengkou-Shangying Fault (TF) (Ma, 2002; Zhang et al., 2001, 2004) (Figs. 1 and 7a). Westward movement of the fault belt along the SF and the Precambrian suture zone of the Khondalite Belt (Zhao et al., 2005) bent the Trans-North China Orogen. Due to the transpressional movement of these dextral strike-slip faults, the Changbai (CB) (Li et al., 2010), Yan (Wu and Wu, 2003a), and Yin (Wu and Wu, 2003b) (b) mountains underwent regional transpressional uplift (Fig. 3). The early Late Cretaceous basaltic rocks were found in the Yan Mountains and its adjacent areas (Chen and Chen, 1997; Xu et al., 2001), which were possibly related to the strike-slip motion of the dextral strike- slip fault system. The resistance of the Amurian Microcontinent to the northwestward motion of the North China Block produced compressional stresses to the north of the North China Block, leading to the formation of signiﬁcant angular unconformities between the Lower and Upper Cretaceous sequences in the East Gobi Basin (Graham et al., 2001; Johnson, 2004), and several other basins in the China– Mongolia border region (Meng et al., 2003)(Figs. 3 and 7a). To the west of the indenting Okhotomorsk Block, between aforementioned sinistral and dextral strike-slip fault systems, the indentation was mainly accommodated by NW–SE-directed crustal shortening (Fig. 7). Mountain ranges peaking between 3500 m and 4000 m above sea level rapidly formed in SE China (Chen, 2000), resulting in a retreat of sea water from SE China at 99 ± 3 Ma after the Early Cretaceous transgression (Hu et al., 2012)(Figs. 3, 6 and 7a). Thermochronological ages from the Ryoke Belt (RB) basement in Kyushu, SW Japan suggest that several kilometers of uplift and denudation occurred approximately during 100–80 Ma (Kamp and Takemura, 1993)(Fig. 3). The accretion-

Fig. 7. (a) Paleogeographic map of East Asia during 100–89 Ma. (b) Schematic cross ary activity in SW Japan was halted between the late Cenomanian and section of AB with location in (a). Mountain belts, CB: Changbai Mountains; DB: Dabie the Santonian (Taira et al., 1988; Hara and Kimura, 2008)(Figs. 2band Mountains; DL: Dalou Mountains; LL: Lüliang Mountains; LU: Luxi Uplift; NL: Nanling 3). An orogenic exhumation event ended siliciclastic sedimentation in Mountains; QL: Qinling Mountains; TH: Taihang Mountains; WY: Wuyi Mountains; XF: the Gyeongsang (GB) and other basins in South Korea (Choi and Lee, Xuefeng Mountains; Y: Yellow Mountains; YAN: Yan Mountains; YIN: Yin Mountains. 2011; Zhang et al., 2012)(Fig. 3). Therefore, in front of the indenter, Basins, BBB: Bohai Bay Basin; EGB: East Gobi Basin; GB: Gyeongsang Basin; HB: Hengyang Basin; JB: Jiaolai Basin; MB: Mayang Basin; OB: Ordos Basin; SB: Sichuan Basin; SYB: NE-striking mountain belts with a width of over 500 km extended Subei-Yellow Sea Basin. Strike-slip faults, SF: Shangyi-Gubeikou-Pingquan Fault; TF: from SE China to SW Japan and South Korea (Fig. 7a). To the west of Taiyingzhen-Lengkou-Shangying Fault; ZLF: Ziyun-Luodian Fault. RB: Ryoke Belt. The in- these mountain belts, conglomerates, sandstones, and red mudstones dentation of the Okhotomorsk Block within East Asia resulted in the formation of a sinis- of alluvial fan, ﬂuvial, eolian, and brackish lacustrine environments tral strike-slip fault system in South China and a dextral strike-slip fault system in North China, and regional NW–SE shortening and orogenic exhumation in East Asia. were deposited above a regional Cenomanian unconformity in the Subei-Yellow Sea Basin (SYB), Jianghan Basin (JHB), and other small basins (Charvet et al., 1994; Chen, 2000; Ma et al., 2009; Hu et al., became a sinistral transpressional fault in the Late Mesozoic (Zhang 2012). To the northeast of the ZLF in the South China Block, the Xuefeng et al., 2009)andgranitesof93–91 Ma were found in the Dachang area Mountains (XF), Dalou Mountains (DL), and eastern Sichuan Basin (SB) along the fault (Cai et al., 2006)(Figs. 1 and 3). It is suggested here were intensely deformed and uplifted (Fig. 7a). Detrital zircon geochro- that during the indentation, several sinistral strike-slip faults initiated nologic studies suggested that the Xuefeng Mountains became an im- at the indenter corner and propagated northwestwards into the Nanling portant topographic high and divide between the Hengyang Basin to Mountains, resulting in transpressional uplifting of the NW-striking its east and the Mayang Basin to its west since the Late Cretaceous range belts, small-scale magmatism, and formation of small pull-part (Yan et al., 2011). The eastern Sichuan Basin and the Dalou Mountains Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115 105 are composed of a series of NE–SW-trending folds in which the Lower (a) Cretaceous rocks are the youngest strata (Ma, 2002; D.P. Yan et al., 89-79 Ma 500 km 2003; Liu et al., 2012). Fission track analyses indicate that they underwent a rapid exhumation during the early Late Cretaceous (Hu et al., 2006; Shen et al., 2009)(Fig. 3). In Central China, the Qinling– Dabie (QL and DB) mountain belts experienced a rapid cooling associated Siberia with dextral strike-slip faulting and NW–SE shortening during 100– 70 Ma (Grimmer et al., 2002; Ratschbacher et al., 2003; Enkelmann et al., 2006; Cui et al., 2012)(Fig. 3). Structural studies indicated that the Jiaolai Basin (JB) and its neighboring areas in the eastern North China Block underwent a NW–SE Izanagi Plate compression between 100 and 90 Ma (Zhang et al., 2003), possibly SAFB causing a rapid uplifting and denudation event in the Luxi Uplift (LU) GX

(Wang et al., 2008) and the Bohai Bay Basin (BBB) (Xu et al., 2001; SLB CSAF Zhu et al., 2012)(Figs. 3 and 7a). Sediments were transported from regions within the uplifted North China Block and deposited in the Subei–

Yellow Sea Basin (SYB) (Ma et al., 2009). The Taihang Mountains (TH), CB TTL Okhotomorsk the Lüliang Mountains (LL), and the central syncline in the Trans-

North China Orogen were folded and uplifted (Xu et al., 2001; Ma, A

2002; Li and Song, 2010)(Figs. 3 and 7a). Further to the west, structural TLF SKTL B studies suggested that the Ordos Basin experienced a NW–SE compres- SYB sion during 100–90 Ma and rapid uplifting changed the basin into an erosional area during the Late Cretaceous (Yang et al., 2005; Zhang et al., 2011)(Figs. 3 and 7a).

It is suggested here the remnant ocean between the Okhotomorsk LF Block and the East Asian margin was possibly closed in a scissor-like manner in 100–96 Ma (Fig. 6). Collision possibly ﬁrst occurred beside F CN SE China, and then beside SW Japan. The onset of rapid cooling and exhumation in various areas in South China occurred at about 100 Ma (e.g. Chen, 2000; Grimmer et al., 2002; Enkelmann et al., 2006; Hu et al., 2006; Shen et al., 2009; Yan et al., 2011; Zheng et al., 2011; Cui et al., (b) A K B 2012; Hu et al., 2012)(Fig. 3). However, most areas in the North China Block including basins in South Korea (Choi and Lee, 2011)begantoun-

South China Okhotomorsk k dergo orogenic uplift at about 96–95 Ma and the hiatus of accretionary 0

3 activity in SW Japan was from the late Cenomanian to the Santonian MTL – (about 96 83 Ma) (Taira et al., 1988; Hara and Kimura, 2008)(Fig. 3). Sanbagawa Belt 50 km 3.2. Strike-slip motion of the Okhotomorsk Block

Izanagi motion direction Continental-oceanic Strike-slip fault At about 90–89 Ma, the Okhotomorsk Block, which had not been (Norton, 2007) convergent boundary completely sutured with the South China Block, began to move northward with the north-northwestward-moving Izanagi Plate (Figs. 7a Undifferentiated Successive nonmarine Nonmarine sedimentation nonmarine basins sedimentation above an unconformity and 8a). The starting time of the northward motion of the Okhotomorsk and erosion areas at about 90–89 Ma is mainly constrained by the rapid exhumation of Magma invasion Sanbagawa high-pressure metamorphic rocks in SW Japan during Marine sedimentation Mountains Highlands and eruption 89–85 Ma (Wallis et al., 2009). This suggestion is consistent with the on continent proposal that a rapid change of the motion direction of the Izanagi Fig. 8. (a) Paleogeographic map of East Asia during 89–79 Ma. (b) Schematic cross section Plate occurred from N35°W at about 90 Ma to N15°W at about 84 Ma of AB with location in (a). Mountain belts, CB: Changbai Mountains; GX: Great Xing'an (Norton, 2007), and consistent generally with the model of a rapidly Mountains; SAFB: Sikhote-Alin Fold Belt. Basins, SLB: Songliao Basin; SYB: Subei-Yellow northward-moving Izanagi–Paciﬁc ridge between 100 and 84 Ma Sea Basin. Strike-slip faults, CNF: Changle-Nanao Fault; CSAF: Central Sikhote-Alin Fault; (Smith, 2003, 2007). The most intense volcanism in the Okhotsk- K: Kurosegawa Belt; LF: Lishui Fault; MTL: Median Tectonic Line; SKTL: South Korean Tectonic Line; TLF: Tanlu Fault; TTL: Tanakura Tectonic Line. The Okhotomorsk Block Chukotka arc of NE Asia began at 89 Ma (Tikhomirov et al., 2012) moved northward along the East Asian margin due to the change from N35°Wto (Figs. 1 and 3), possibly resulted from the onset of orthogonal subduc- N15°W in Izanagi motion direction. The northeastward oblique motion of the tion of the Izanagi Plate below the Siberian margin. High-resolution Okhotomorsk Block along the transform zone at the Asian margin resulted in rapid exhu- mantle tomographic data show a high-velocity zone at 900 km depth mation of Sanbagawa high-pressure metamorphic rocks through the ductile shear zone at below the Yellow Sea and SE China (Huang and Zhao, 2006)(Fig. 7a), the lower crust and upper mantle level, and formation of an upper crustal strike-slip fault system of several tens of kilometers wide. which may correspond to the remnant of the oceanic slab detached from the Okhotomorsk.

3.2.1. The sinistral transform fault zone mantle level, and an upper crustal strike-slip fault system several tens The oblique motion of the Okhotomorsk Block along the NE-striking of kilometers wide (Fig. 8b). Asian margin to the south of the northern indenter corner during about The deﬁnition of the vertical ductile shear zone at the lower crust 89–83 Ma was achieved through displacement of a signiﬁcant sinistral and upper mantle level is based on the following evidences. (1) Seismic transform fault zone between the Eurasian Plate and the Okhotomorsk data show that the Sanbagawa Belt is a several-kilometer wide, gently Block (Fig. 8). The transform fault zone is composed of a several- north-dipping belt to the south of the MTL (Ito et al., 2009)(Fig. 2c). kilometer wide ductile shear zone at the lower crust and upper (2) According to P–T estimates of the Iratsu eclogitic body and 106 Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115

Higashi–Akaishi peridotite body (Fig. 2b), a sandwiched thermobaric Charvet, 2013)(Fig. 4a). Taira et al. (1983) interpreted this belt as a structure was proposed for the exhumation of the Sanbagawa Belt strike-slip mobile zone through which lateral displacement of over (Ota et al., 2004). The highest-grade rocks were tectonically thinned 1000 km occurred and numerous tectonic blocks totally unrelated to as a slice by ductile deformation and were exhumed rapidly from the Jurassic–Early Cretaceous accretionary complex were delivered about 90 km depth to mid-crustal levels. (3) Sanbagawa metamorphic into Japan. A recent paleomagnetic study (Uno et al., 2011)reporteda rocks were exhumed at a rate of at least 2.5 cm/yr during 89–85 Ma difference in paleolatitude (14° ± 3°) for the Kurosegawa Belt between (Wallis et al., 2009),whichismuchhighercomparedtomost the Early Cretaceous and the present, implying a northward translation ultrahigh-pressure and high-pressure units formed in continental-type of ~1500 ±300 km from the position of the South China Block to its subduction scenarios (Guillot et al., 2009). (4) Sanbagawa metamorphic present position during the mid-Cretaceous. Integrating all the informa- rocks were raised to the mid-crustal level at about 85 Ma (Ota et al., tion together, it is suggested here that a relatively small terrane possibly 2004; Wallis et al., 2009), suggesting that the rapidly exhuming collided with the South China Block during the Late Jurassic–earliest pathway ended at the mid-crustal level. (5) The pervasive, nearly Cretaceous (Maruyama et al., 1984; Otsuki, 1992; Charvet, 2013) strike-parallel, retrograde stretching lineation in the Sanbagawa Belt (Fig. 6). During the Early Cretaceous, shallow marine sediments were suggests a gently rising eastward trajectory along a sinistral strike-slip deposited above this block (Hada et al., 2001; Ishida et al., 2003)and margin of Asia (Wintsch et al., 1999; Wallis et al., 2009). (6) A mylonite accretionary complexes were accumulated to its east. When the zone, several hundreds to a thousand meters wide, was found along the Okhotomorsk Block moved obliquely along the NE-striking Asian MTL in the Ryoke metamorphic belt near the Takato area (Takagi, 1986) margin during 89–83 Ma, the block was possibly located beside the (Fig. 2a). Asymmetric microstructures and the attitude of stretching main strike-slip fault of the transform boundary. Upper crustal rocks lineations in the mylonite zone suggest that sinistral strike-slip shearing on the block were tectonically sliced and transported laterally along with a minor vertical-slip component occurred during the mid- the main strike-slip fault for over 1000 km (Taira et al., 1983; Uno Cretaceous mylonitization (Takagi, 1986; Otsuki, 1992)(Fig. 3). (7) A et al., 2011). The ubiquitous serpentinite both in the Kurosegawa Belt fault zone less than 10 km wide was also found in the lower crust just (Taira et al., 1983) and along the San Andreas Fault (e.g. Moore and below the San Andreas Fault in Northern California (Henstock et al., Rymer, 2007; Holdsworth et al., 2011) further supports that rock lens 1997), the best modern example of continental transform faults. (8) Nu- of the Kurosegawa Belt were transported along the main strike-slip merical models of deformation at a continental transform boundary fault through which serpentinite was migrated from the upper mantle (Roy and Royden, 2000; Platt and Behr, 2011)suggestanarrowductile level. shear zone 50 m to 7 km wide at the lower crust and upper mantle level. 3.2.2. Effects in a much broader region At the upper crustal level, a series of sinistral strike-slip faults possi- Velocity data from the western United States indicate that the plate bly constituted a large flower structure several tens of kilometers wide boundary right-lateral motion extends at least 1000 km to the west of at the East Asian transform margin (Fig. 8b). The numerical model the San Andreas Fault, with strain rate and total displacement decreasing (Roy and Royden, 2000) suggests that at a continental transform bound- away from the transform fault zone (Platt and Becker, 2010; Parsons and ary a network of interacting strike-slip faults form in the upper crust and Thatcher, 2011). Similarly, the effect of the oblique sinistral motion of these faults have a spatial connection to the narrow lower crustal shear the Okhotomorsk Block along the NE-striking Asian margin reached a zone. The strike-slip faults subdivided the accretionary complexes broader region to the west of the transform margin (Fig. 8a). Several successively accumulated along the East Asian margin during the major sinistral strike-slip faults formed or reactivated, including the Jurassic–Early Cretaceous into narrow, long, and subparallel belts, Lishui Fault (LF) (Chen, 2000), Changle-Nanao Fault (CNF) (Charvet such as the Early-Middle Jurassic North Chichibu Belt, the Middle et al., 1994), and Tanlu Fault (TLF) (Zhang et al., 2003). A series of Jurassic–earliest Cretaceous South Chichibu Belt, and the Neocomian– small NE–SW trending pull apart basins developed in Southeast China Cenomanian Shimanto sub-belt (Taira et al., 1983, 1988; Hada et al., intheLateCretaceous(Charvet et al., 1994; Lapierre et al., 1997; Ma 2001; Ishida et al., 2003)(Fig. 2). Transpressional stresses produced et al., 2009). E–W trending stretching lineations formed throughout folded structures in these narrow belts (Taira et al., 1988). This pattern the Ryoke metamorphic belt in SW Japan, associated with a top-to- is very similar to that of the San Andreas fault system in California, the-west sense of shear (Adachi and Wallis, 2008; Okudaira et al., which is several tens of kilometers wide and composed of a series of 2009)(Fig. 2a). Japan Islands (Taira et al., 1983; Kanaori, 1990; Otsuki, faults subparallel to the San Andreas Fault (Hill et al., 1990; Meade 1992) and South Korea (Hwang et al., 2008) were subdivided into and Hager, 2005; Platt and Becker, 2010). It is reminded here that the many blocks by strike-slip faults along which the Late Cretaceous fault system might have been partially eroded during the exhumation magmatism mainly occurred. of the Sanbagawa and Ryoke metamorphic belts from the middle crustal It is presumed here that the northern indenter corner resisted level in the latest Cretaceous–Paleogene (Okudaira et al., 2009; Wallis the motion of the Okhotomorsk Block (Figs. 7aand8a). An intense et al., 2009)(Fig. 2). compression occurred between the Okhotomorsk and the region to There possibly was a vertical main strike-slip fault in the East Asian the north of the indenter corner. Counterclockwise rotation, sinistral transform boundary, which connected the lower crustal shear zone strike-slip faulting, and rapid uplifting occurred in NE Japan (Itoh et al., and accommodated a high percentage of the relative movement 2000), forming the major TTL which may have extended through the between the Eurasian Plate and the Okhotomorsk Block (Fig. 8b). Its Tatar Strait and several other strike-slip fault zones (Otsuki, 1992) role in the East Asian transform margin is similar to that of the San (Figs. 2a, 4b, c, and 8a). The rapid uplifting in central Hokkaido and Andreas Fault in the San Andreas transform boundary between the southern Sakhalin caused a change of depositional environment from Pacific and North America plates (Hill et al., 1990; Meade and Hager, deep marine to shallow marine and non-marine in these areas (Ando, 2005; Platt and Becker, 2010). The formation of the narrow and long 2003; Hasegawa et al., 2003)(Fig. 3). The major sinistral strike-slip Kurosegawa Belt in SW Japan (Fig. 2) was probably related to the fault, CSAF, had a displacement of about 200 km, and folding and large scale left-lateral offset of the main fault (Fig. 8b). The Kurosegawa thrusting occurred in the SAFB (Zonenshain et al., 1990). Sea water Belt is composed of lenses of Ordovician–Early Cretaceous granitic, retreated from the Sanjiang-Middle Amur Basin and the SAFB in the metamorphic, and shallow marine sedimentary rocks surrounded by late Turonian (Kirillova, 2003)(Figs. 3, 7a, and 8a). At the Turonian– serpentinite or bounded by faults (Taira et al., 1983; Maruyama et al., Coniacian boundary (about 88 Ma), the Songliao Basin experienced a 1984; Hada et al., 2001; Wakita, 2013)(Fig. 2). It was defined as an long subaerial exposure and weathering, forming a major angular exotic landmass which collided with the East Asian margin during the unconformity within the Upper Cretaceous sequences (Feng et al., Late Jurassic–Early Cretaceous (Maruyama et al., 1984; Otsuki, 1992; 2010)(Figs. 3 and 8a). Fission track analyses indicate that the Great Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115 107

Xing'an Mountains began to undergo a rapid cooling at about 90 Ma (Li (Otsuki, 1992; Nakajima, 1994; Suzuki and Adachi, 1998). Granitoids et al., 2011)(Figs. 3 and 8a). occupy about 70–80% of the Ryoke metamorphic belt (Okudaira et al., 2009), suggesting a close correspondence between the SSP 3.2.3. Extension and magmatism following the transpressional regime which underwent the most intense extension (Ito et al., 2009)and When the southwestern end of the Okhotomorsk Block passed the the magmatism during the Late Cretaceous (Fig. 2). Late Cretaceous NE-striking Asian margin to the south of the northern indenter corner bimodal volcanism in SE China appears to have been produced by at about 83 Ma (Figs. 8aand9a), the long and subparallel accretionary intracontinental extension and rifting, not subduction (Charvet et al., belts and the Kurosegawa Belt in the upper crustal fault system and the Sanbagawa metamorphic belt in the shear zone at lower crust and (a) upper mantle levels were left behind in SW Japan. The space left by the departed lithosphere of the Okhotomorsk was rapidly ﬁlled by subduction of oceanic lithosphere to its south, forming the highly- deformed Shimanto accretionary prism in SW Japan during the early Campanian (Taira et al., 1988)(Fig. 9b). Easing of the transpressional regime led to relaxation of areas to the west of the continental margin. The MTL and Sanbagawa rocks began to dip gently to the northwest and normal faulting commenced to northwest of the MTL (Fig. 9b). The Seto Subsurface Prism developed (Ito et al., 2009)andreceived marine sedimentation of the Izumi Group after about 83 Ma (Noda and Toshimitsu, 2009)(Figs. 2, 3, and 9b). The deep subduction of the Shimanto accretionary prism beneath the Asian margin resulted in the formation of Shimanto HP metamorphic rocks at the latest Cretaceous (Aoki et al., 2011)(Fig. 9b). Charvet (2013) suggested that a continental block called Shimanto Block collided with SW Japan during 80-60 Ma. This suggestion is inconsistent with the geological fact that a wide Upper Cretaceous accretionary prism formed along the Japanese margin during the Campanian-Maastrichtian (Taira et al., 1988; Taira, 2001) (Fig. 2b). The suggested collisional and compressive event (Charvet, 2013) was contradictory to the extensional setting shown by the formation of the Seto Subsurface Prism (Ito et al., 2009) and the deposition of the Izumi Group (Noda and Toshimitsu, 2009) to the northwest of the MTL during the latest Cretaceous (Fig. 2c). During the Late Cretaceous, especially between 90 and 75 Ma, intense magmatism occurred in a belt hundreds of kilometers wide extending from SE China (Charvet et al., 1994; Lapierre et al., 1997)and Taiwan (Yui et al., 2009; Wintsch et al., 2011), through South Korea (Zhang et al., 2012)andSWJapan(Otsuki, 1992; Nakajima, 1994; (b) Suzuki and Adachi, 1998), to the SAFB, in Russia (Zonenshain et al., 1990)(Fig. 1). Traditionally the Late Cretaceous igneous rocks are con- sidered as products of continental arcs related to oceanic subduction (Nakajima, 1994; Isozaki, 1996; Maruyama et al., 1997; Isozaki et al., 2010). However, it is suggested here that the oblique motion of the Okhotomorsk Block along the NE-striking Asian margin was possibly an important trigger for this magmatic event. As mentioned above, the plate boundary sinistral motion produced a regional effect to the west of the transform fault zone and to the north of the northern indenter corner. Many major and minor strike-slip faults formed, (c) separating big areas into many small blocks (Kanaori, 1990; Hwang et al., 2008). With migration of the Okhotomorsk along the NE-striking Asian margin, areas near the margin gradually relaxed landward and eastward (Figs. 8aand9b). Extensional forces following the transpressional regime may have contributed to the large number of gaps between blocks separated by previously formed faults, creating space to host igneous intrusions. This interpretation is supported by the following evidences. The Late Cretaceous granites in SW Japan generally have a tendency of landward and eastward younging

Fig. 9. (a) Paleogeographic map of East Asia during 79–77 Ma. (b) Schematic cross section of AB with location in (a). (c) Schematic cross section of CD with location in (a). IG: Izumi Group; MTL: Median Tectonic Line; SSP: Seto Subsurface Prism. The Okhotomorsk Block collided with the Siberian margin. At about 77 Ma, the Izanagi oceanic lithosphere began to subduct beneath the Okhotomorsk, causing magmatism, regional metamorphism, and accumulation of accretionary prism along its margin. The departure of the Okhotomorsk Block from the NE-striking Asian margin resulted in the occurrence of an extensional setting (tilting of crustal structures), formation of a wide magmatic belt, and formation of highly-deformed accretionary prism along the margin. 108 Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115

1994; Lapierre et al., 1997). Similarly, volcanism began in the SAFB structures developed (Hourigan and Akinin, 2004; Tikhomirov et al., at the Santonian, after the formation of compressional structures 2012). (Zonenshain et al., 1990)(Fig. 3). After around 83 Ma, the Okhotomorsk Block moved along the north- 4. Evidences of Archean and Early Proterozoic zircons trending Asian margin to the north of the indenter corner (Figs. 8aand 9a). As the continental margin was relatively consistent with the north- 4.1. U–Pb dating of detrital zircons ward motion of the Izanagi Plate, the block moved along the trench, as suggested by Otsuki (1992), and produced little compression to the Abundant Late Archean to Early Proterozoic detrital zircons have margin. Shallow marine sedimentation continuously occurred in central been found in Cretaceous sandstones in Kamchatka (Bindeman et al., Hokkaido and southern Sakhalin until about 79 Ma (Ando, 2003; 2002), SW Japan (Okamoto et al., 2004; Nakama et al., 2010; Aoki Hasegawa et al., 2003) when the Okhotomorsk Block collided with the et al., 2012), and Taiwan (Yui et al., 2012)(Figs. 1 and 5). Different Siberian margin (Figs. 3 and 9a). models have been proposed to explain their possible sources. However, it is found that all these models are not convincing. In Kamchatka, based on U–Pb dating of detrital zircons in metamor- 3.3. The collision of the Okhotomorsk Block with the Siberian margin phic basements of the Sredinny Massif, it was suggested that siliciclastic sediments which contain abundant Archean (2900–2500 Ma), Early At about 79 Ma, the rapidly-moving Okhotomorsk Block began to col- Proterozoic (1700–2100 Ma), Ordovician to Early Jurassic (460–175 Ma), lide with the Siberian margin, north of the Okhotsk Sea (Fig. 9a), resulting and Late Jurassic to Early Cretaceous (150–96 Ma) detrital zircons were in the cessation of arc magmatism in the Okhotsk-Chukotka volcanic deposited at the eastern part of the Okhotomorsk Block during about belt (Tikhomirov et al., 2012)(Figs. 1 and 3). Continental collision 120–96 Ma (Bindeman et al., 2002)(Fig. 5a). A speculative model was ended at about 77 Ma. No significant structural deformations related proposed that the Okhotomorsk formed as a result of the eastward ex- to this relatively short collisional event have been found on the Siberian trusion of subduction–accretion materials during the Triassic closure of margin (Hourigan and Akinin, 2004). A minor intraplate basaltic volca- the Mongol–Okhotsk Ocean (Şengör and Natal'in, 1996; Bindeman nism occurred in the Okhotsk-Chukotka volcanic belt from 77.5 ± et al., 2002)(Fig. 1). The Siberia Craton was interpreted as the source 1.1 Ma to 74.0 ± 1.2 Ma (Hourigan and Akinin, 2004; Tikhomirov et al., area of the Archean, Proterozoic, and Paleozoic zircons found in the 2012), possibly resulted from the asthenospheric rise following the slab Sredinny Massif (Bindeman et al., 2002). Only considering the present detachment from the Okhotomorsk Block (Fig. 9c). The high-velocity area of the Okhotomorsk Block of about 1.5 million square kilometers, zone dipping to the northwest beneath the northern Sea of Okhotsk is without taking into account its reduced area due to the interaction be- possibly the remnant of the oceanic slab detached from the Okhotomorsk tween the Okhotomorsk Block and Eurasia during the Late Cretaceous (Gorbatov et al., 2000)(Fig. 9a). At about 77 Ma, the Izanagi oceanic lith- (Figs. 6–9), it is suggested here that the definition of this giant block osphere began to subduct beneath the Okhotomorsk from the south. This as an accretionary prism is possibly unrealistic. Moreover, a number new subduction caused magmatism, regional metamorphism (Bindeman of paleomagnetic and geological studies suggested that the Mongol– et al., 2002; Chekhovich et al., 2009), and accumulation of the late Campa- Okhotsk Ocean was possibly closed during the Late Jurassic–Early nian marine clastic sediments (Terekhov et al., 2012)alongthesouthern Cretaceous (e.g. Zonenshain et al., 1990; Yin and Nie, 1996; Zorin, 1999; and eastern margins of the Okhotomorsk (Figs.3,and9a, c). Because the Kravchinsky et al., 2002; Cogné et al., 2005; Metelkin et al., 2010). Okhotomorsk had a northwestward motion along the northwest- In SW Japan, U–Pb dating of detrital zircons from the Paleozoic to trending Asian margin to the north of Sakhalin during its final move- Cenozoic sandstones shows that most of Paleozoic, Triassic, Jurassic, ment phase, a semi-closed oceanic basin formed between its south- Early Cretaceous, and Late Cretaceous sandstones (HTE-3, MRB-1, western margin and southern Sakhalin, which was closed during the MTO-1, HU-1, KRM-1, JC6, JC8, QM, NK1, and IZ01) hardly contain the Paleogene (Otsuki, 1992; Maruyama et al., 1997; Taira, 2001)(Fig. 9a). Proterozoic grains (Okamoto et al., 2004; Nakama et al., 2010; Aoki et Northeast-trending troughs formed in the northern Okhotsk Sea, receiv- al., 2012)(Figs. 2 and 5b), indicating that siliciclastic flux from two ing Maastrichtian–Cenozoic sediments about 6 km thick (Chekhovich major cratons (North China Block and South China Block) was very et al., 2009)(Fig. 9a, c). small (Isozaki et al., 2010). It was suggested that the Paleozoic, Jurassic, An issue that needs to be addressed here is why a new oceanic and mid-Cretaceous arc batholith belts abound Japan were the main subduction occurred so fast to the south of the Okhotomorsk Block sources during the Paleo-Mesozoic time (Isozaki et al., 2010; Aoki after a short collision between 79 and 77 Ma (Fig. 9), while a new et al., 2012). However, the Late Archean (2700–2500 Ma) and Early subduction zone did not initiate to the east of the Okhotomorsk Proterozoic (2500–1500 Ma) zircons form a major component in the Block after significant structural deformations in East Asia during the Sanbagawa Belt (sample BK11, 82% of all dated grains), Shimanto accre- Okhotomorsk–East Asia collision in 100–89 Ma (Fig. 7). Geodynamic tionary complex (sample 09405-4, 31% of all dated grains), and meta- models (Toth and Gurnis, 1998; Hall et al., 2003; Baes et al., 2011)indi- morphosed Shimanto accretionary complex (sample BK12, 74% of all cate that a preexisting weakness zone in the lithosphere is required to dated grains), and they are most abundant in the Sanbagawa Belt facilitate the subduction initiation process and subduction can occur if (BK11) (Aoki et al., 2012). the weak zone is moderately compressed. It is suggested here a series Aoki et al. (2012) attributed the occurrence of the Proterozoic zir- of fractures may have been formed at the ocean–continent transition cons in the Sanbagawa Belt to a basal erosion of the overlying Jurassic areas during the Okhotomorsk–East Asia collision and during the accretionary complex in the subduction zone and those in the Shimanto transpressional motion of the Okhotomorsk Block along the East Asian metamorphic belt to another basal erosion of the overlying Sanbagawa margin (Figs. 7aand8a). When the Okhotomorsk Block collided with Belt. They thought these are the only possible mechanisms to explain the Siberia Craton, convergence produced compressive forces along the sudden appearance of the Proterozoic zircons in Japan. However, the preexisting fracture zones to the south and east of the block, bending this interpretation is highly doubtful. First, the model of Aoki et al. the oceanic lithosphere as it entered the trench. Therefore, a self- (2012) is based on a questionable assumption that they only found sustaining subduction zone was rapidly created (Fig. 9c). In addition, the Proterozoic zircons in meta-sandstones of the Sanbagawa metamor- the fast slab detachment from the Okhotomorsk to the north of the phic belt and Shimanto metamorphic belt, and never found them in the block may have also been related to the preexisting fracture zones at coeval nonmetamorphosed accretionary complex and forearc basin the ocean–continent transition areas (Fig. 9c). As a result, after a short sediments. This assumption is inconsistent with their data which collision between 79 Ma and 77 Ma, an intraplate basaltic volcanism show that the Proterozoic zircons make up 31% of all dated grains in occurred on the Siberian margin where no significant compressive 09405-4, a sandstone sample of the nonmetamorphosed Shimanto Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115 109 accretionary complex (Fig. 5b). The second but the most significant (e.g. Isozaki and Itaya, 1990; Aoki et al., 2011; Itaya et al., 2011), it should contradiction between the model and practical data is that U–Pb dating not have contained so abundant Proterozoic zircons. If it had been of detrital zircons from sandstones of the Jurassic accretionary complex deposited just before the Okhotomorsk–East Asia collision as SCY-1 in in SW Japan (e.g. HU-1, KRM-1, and JC6) suggest that they almost do not Taiwan was (Fig. 5c), besides the Proterozoic zircons, it should also contain the Proterozoic zircons delivered from two major ancient have contained some Early Cretaceous zircons. In addition, it is sug- Chinese continents (Isozaki et al., 2010; Nakama et al., 2010; Aoki gested here that the protolith of the meta-sandstone QM is the Early et al., 2012). How could the Sanbagawa Belt get an abundant supply Cretaceous accretionary complex sandstone (e.g. Isozaki and Itaya, of the Proterozoic grains (82% in BK11) in the subduction zone from 1990; Okamoto et al., 2004; Aoki et al., 2011; Itaya et al., 2011)and the overlying Jurassic sediments which almost do not contain the does not have a link to the Okhotomorsk Block (Figs. 2cand5b), mainly Proterozoic grains? because only one Proterozoic zircon was found from many dated zir- In Taiwan (Fig. 1), age distribution patterns of detrital zircons from cons in the sample (Okamoto et al., 2004). the metamorphosed rocks which were originated from the Jurassic– After the Okhotomorsk Block moved away from the NE-striking Cretaceous accretionary complexes show that the mid-Cretaceous Asian margin (Fig. 8), for a short period of several million years, Archean accretionary complex (SCY-1) contains much more abundant Late and Early Proterozoic detrital grains were still a relatively important Archean and Early Proterozoic (2700–1700 Ma) zircons than the Late component in the rapidly accumulated accretionary complexes. They Jurassic–earliest Cretaceous (SCT-5) and Late Cretaceous (SCT-1) accre- mainly came from numerous rock fragments which were broken from tionary complexes (Fig. 5c) (Yui et al., 2012). As zircon age spectra of the the Okhotomorsk Block and were left behind the block. Therefore, Late Jurassic–earliest Cretaceous and Late Cretaceous accretionary com- a certain number of Archean and Proterozoic zircons were detected plexes are similar to those of modern river sediments in the southern in the Late Cretaceous Shimanto accretionary complex in SW Japan part of the South China Block, siliciclastic sediments were evidently (09405-4 and BK12) (Fig. 5b) and in the Late Cretaceous accretionary sourced from the South China Block and deposited in Taiwan along complexinTaiwan(SCT-1)(Fig. 5c). However, because the Okhotomorsk the East Asian margin during the Late Jurassic–earliest Cretaceous and Block left the East Asia margin completely, its influence gradually Late Cretaceous (Yui et al., 2012). The significant increase of the Early disappeared. Few Proterozoic zircons were found in the sample NK1 Proterozoic zircons in the mid-Cretaceous accretionary complex was and Proterozoic zircons are not present in sands accumulated in recent ascribed to the continental uplift and erosion of the North China Block rivers in Japan (KRB-1) (Nakama et al., 2010). during the Triassic South China–North China collision. It is very hard During the Campanian, the Okhotomorsk Block collided with Siberia to understand this interpretation. Why did the Triassic collisional (Fig. 9). As a part of the giant block, siliciclastic sediments accumulated event influence the deposition along the East Asian margin only in the along the eastern Okhotomorsk margin during the Early Cretaceous also mid-Cretaceous not in the Late Jurassic–earliest Cretaceous? Moreover, arrived at Northeast Asia. Part of them is exposed in Kamchatka and the North China Block experienced a regional extensional event during is called the Sredinny Massif (Fig. 1). Therefore, it is very easy to the Early Cretaceous and most previously uplifted areas in the block understand why the Sredinny Massif contains so abundant Archean became sedimentary basins (Zhu et al., 2012; Lin et al., 2013). and Proterozoic zircons (Fig. 5a). Regarding the Ordovician to Early Cretaceous zircons (460–96 Ma) in the Sredinny Massif, it is suggested 4.2. New interpretations here that they were not necessarily delivered from the Okhotomorsk Block itself. They could come from the East Asian margin during the The model of the Okhotomorsk-East Asia collision during 100–89 Ma Okhotomorsk–East Asia collision (Fig. 7). The uplifted accretionary and the Okhotomorsk-Siberia collision during 79–77 Ma (Figs. 6–9) complexes could provide zircons of various Paleozoic–Mesozoic ages provides a possible explanation for the abundant Late Archean to Early to the Okhotomorsk Block (Fig. 5a, b). Proterozoic detrital zircons in the Cretaceous sandstones in Kamchatka, SW Japan, and Taiwan (Fig. 5). First, it is presumed here that the Okhotomorsk Block is composed of the Late Archean and Early Protero- 5. Evolution of the Sanbagawa HP metamorphic belt zoic basement. A process of how old zircons were delivered from the Okhotomorsk to these places is described as follows. There has been a major debate on the age of peak metamorphism of During most of the Early Cretaceous, the exposed Mesozoic arc the Sanbagawa Belt in SW Japan (Fig. 2). It has been generally accepted batholith belts near the Asian margin were the main sources (Isozaki that the peak metamorphism took place around 120 Ma (e.g. Isozaki et al., 2010; Aoki et al., 2012; Yui et al., 2012), sediments accumulated and Itaya, 1990; Aoki et al., 2011; Itaya et al., 2011). One supporting in forearc basins (e.g. JC8) and accretionary complexes (e.g. JC6 and evidence is the whole rock Rb–Sr dating of eight samples in central SCT-5) along the East Asian margin mainly contained the Mesozoic Shikoku, showing an age of 116 ± 10 Ma (Minamishin et al., 1979). zircons (Fig. 5b, c). Another is the U–Pb dating of detrital zircons in a meta-sandstone In a period of several million years before the Okhotomorsk Block (sample QM) intercalated with the Iratsu eclogite in central Shikoku, collided with East Asia (Fig. 6), siliciclastic sediments accumulated which yields a metamorphic age of 130–110 Ma (Okamoto et al., along the East Asian margin had two sources, the Eurasia Plate and the 2004)(Figs. 2band5b). However, it was suggested that these studies approaching Okhotomorsk Block. The exposed Mesozoic arc batholith lack a clear link between the ages and metamorphic history (Endo belts near the Asian margin still provided the Mesozoic zircons, but et al., 2009; Wallis and Endo, 2010). A Lu–Hf dating of the Seba eclogite the approaching of the Okhotomorsk Block suddenly resulted in the in central Shikoku and the Kotsu eclogite in eastern Shikoku provided a significant increase of Archean and Early Proterozoic zircons in accre- peak metamorphic age of 88–89 Ma (Wallis et al., 2009)(Fig. 2b). tionary complexes. The protolith of SCY-1 in Taiwan was possibly Another Lu–Hf dating of the Iratsu eclogite in central Shikoku yielded deposited in this scenario (Fig. 5c). an age of 116 Ma (Endo et al., 2009)(Fig. 2b), compatible to the zircon During the Okhotomorsk–East Asia collision (Fig. 7), the western age (Okamoto et al., 2004). Based on geochronological and petrological Okhotomorsk Block margin which was probably covered by siliciclastic studies of the Iratsu eclogite, Endo et al. (2009) proposed that the sediments accumulated before the Late Cretaceous was subducted eclogite unit experienced a pre-eclogite facies metamorphism at 550– below East Asia. It is proposed here that the protolith of the meta- 650 °C and 1 GPa at about 116 Ma, and an eclogite facies metamor- sandstone sample BK11 of the Sanbagawa Belt is possibly the sandstone phism at 600–650 °C and 2 GPa at about 89 Ma. Furthermore, these deposited along the Okhotomorsk Block margin during the Late Jurassic– authors provided a possible scenario for the evolution of the Sanbagawa Early Cretaceous (Figs. 2band5b). If it had been eroded from the Late Belt that the Iratsu unit was subducted before the Seba unit and they Jurassic–earliest Cretaceous accretionary complex as generally thought became juxtaposed during the prograde eclogite metamorphism. 110 Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115

Based on the geochronological and petrological characteristics of the Paleogene (Otsuki, 1992; Maruyama et al., 1997; Taira, 2001). Prior to Sanbagawa Belt (Okamoto et al., 2004; Endo et al., 2009; Wallis et al., the Late Cretaceous, it may have been as big as either the South 2009), an evolution of the Sanbagawa metamorphic belt in the new China Block or the North China Block (Fig. 10a, b). In addition, abundant tectonic framework (Figs. 6–9)isprovidedhere.DuringtheEarly Late Archean to Early Proterozoic detrital zircons in the Cretaceous Cretaceous, accretionary sediments along the East Asia margin were sandstones in Kamchatka, SW Japan, and Taiwan suggest that the partially eroded and subducted with the Izanagi Plate, and experienced Okhotomorsk Block formed during the Late Archean and Early a pre-eclogite facies metamorphism during 130–110 Ma (Minamishin Proterozoic, with a similar age to the North China Block (Zhao et al., et al., 1979; Okamoto et al., 2004; Endo et al., 2009). During the 2005). Therefore, this giant and old craton merits careful consideration Okhotomorsk–East Asia collision in 100–89 Ma (Fig. 7), the western in future plate reconstructions. Okhotomorsk Block margin was subducted below East Asia. In the sub- It is presumed here that the Okhotomorsk Block was surrounded by duction zone, the crustal rocks offscraped from the Okhotomorsk Block passive margins and located in the interior of the Izanagi Plate before were juxtaposed with those accretionary sediments and oceanic rocks theLateCretaceous(Fig. 10a, b). Van der Meer et al. (2012) suggested which underwent a metamorphism during 130–110 Ma, and were to- that the major intra-oceanic subduction zone Telkhinia separated the gether subducted to the upper mantle level (Endo et al., 2009). At early Mesozoic Panthalassa Ocean into a western realm, the Pontus about 89 Ma, just before the slab breakoff from the Okhotomorsk Ocean, and an eastern realm, the Thalassa Ocean, and several Asian exotic Block, the subducted materials underwent the peak eclogite facies terranes were on the western margin of the overriding Thalassa oceanic metamorphism (Wallis et al., 2009). During 89–85 Ma, Sanbagawa plate (Fig. 10a). However, it is unlikely that the Okhotomorsk Block was high-pressure metamorphic rocks were rapidly exhumed through the located at the margin of the Izanagi Plate, the northwestern part of the ductile shear zone at the lower crust and upper mantle level between Thalassa Ocean (Van der Meer et al., 2012), during the early Mesozoic. the Okhotomorsk Block and East Asia (Fig. 8). In summary, the new tec- The high-velocity zone below the Yellow Sea and SE China (Huang and tonic evolution model of the Sanbagawa Belt involves two metamorphic Zhao, 2006)(Fig. 7a) indicates a remnant of the oceanic slab detached events, a pre-eclogite facies metamorphism of part of Sanbagawa rocks from the Okhotomorsk Block. The Early Cretaceous magmatic arc suites in an oceanic subduction setting during 130–110 Ma, and a progressive extensively distributed in SE China were related to the westward subduc- eclogite metamorphism of Sanbagawa rocks as a whole in a continental tion of the Izanagi oceanic lithosphere (Charvet et al., 1994; Lapierre subduction setting, culminating at about 89 Ma. et al., 1997) before the collision of the Okhotomorsk Block with East Asia. The Sanbagawa metamorphic belt is interpreted as a mingled It is mentioned previously that the protolith of the meta-sandstone product of pre-eclogite-facies metamorphic rocks previously offscraped BK11 of the Sanbagawa Belt was possibly deposited along the during the Early Cretaceous oceanic subduction and rocks detached Okhotomorsk Block margin during the Late Jurassic–Early Cretaceous from the subducting Okhotomorsk crust. The protolith of the meta- (Fig. 5b). A major zircon age peak of 156–181Maisshowninthesample sandstone QM near the Iratsu body is the Early Cretaceous accretionary BK11 (Aoki et al., 2012). It was suggested that substantial volcanic and hy- sandstone (Figs. 2band5b), which together with other subducted drothermal activities took place near the Pacific Plate in the Middle Juras- oceanic rocks underwent a pre-eclogite facies metamorphism during sic when the Pacificjustformed(Bartolini and Larson, 2001; Koppers 130–110 Ma (Okamoto et al., 2004; Ota et al., 2004; Endo et al., 2009; et al., 2003; Tivey et al., 2005)(Fig. 10a, b). The coincidence may imply Utsunomiya et al., 2011). The garnet–granulite relicts in the Iratsu that the group of the Middle Jurassic zircons in the Okhotomorsk Block body suggest a pre-Sanbagawa metamorphism under a geotherm was related to the intense intraplate magmatism in the paleo-Pacific and lith-pressure of a thick crust of 15–30 km (Ota et al., 2004; Ocean during the Middle Jurassic, and the block was not very far away Utsunomiya et al., 2011). They are interpreted here to have been from the triple junction between the Farallon, Phoenix and Izanagi plates. offscraped from the ancient crystalline basement of the Okhotomorsk During the Late Jurassic–Early Cretaceous, owing to the fast expansion Block during the subduction of the Okhotomorsk below East Asia. The of the PacificPlate(Bartolini and Larson, 2001; Smith, 2003), the Izanagi pelitic schists from the surrounding rocks and pelitic gneisses from Plate moved northwestward with continental blocks or island arcs the marginal zone of the Iratsu body are characterized by negative εNd which were in the interior of the plate or at its margins (Engebretson (t) value (~−5), suggesting a source from an old continental crust et al., 1985; Smith, 2003; Norton, 2007; Van der Meer et al., 2012) (Utsunomiya et al., 2011). It is interpreted here that their pelitic (Fig. 10a, b). A series of Asian exotic terranes including the South Kitakami protoliths were deposited along the Okhotomorsk Block margin before Belt, Kurosegawa Belt, and Kolyma–Omolon Block which were on the the Late Cretaceous and were offscraped from the Okhotomorsk Block western margin of the Izanagi Plate collided with the East Asian margin during the continental subduction. They were unlikely sourced from duringtheLateJurassic–earliest Cretaceous (Otsuki, 1992; Stone et al., the South China Block as Utsunomiya et al. (2011) suggested, because 2003; Charvet, 2013). During about 100–89 Ma, the northwestward- U–Pb dating of detrital zircons from the Paleozoic to Cenozoic sand- moving Okhotomorsk Block collided with the East Asian margin stones in SW Japan indicate that siliciclastic flux from two Chinese (Fig. 10c). ancient cratons was very small (Isozaki et al., 2010)(Fig. 5b). In addition, as mentioned above, the meta-sandstone BK11 of the Sanbagawa 6.2. Constraints on the plate reorganization of the Northwest Pacificduring Belt was possibly deposited along the Okhotomorsk Block margin the CNS during the Late Jurassic–Early Cretaceous (Figs. 2band5b). The interpretation for origins of Sanbagawa metamorphic rocks is consistent The new tectonic model (Figs. 6–9) establishes process relationships with the continental collision model suggesting that in continental between onshore geological records and current ideas regarding the collision orogens, ultra-high-pressure rocks may mingle with the low- plate configuration of the paleo-PacificOcean(Engebretson et al., grade metamorphic rocks offscraped in the early stage of subduction, 1985; Smith, 2003; Norton, 2007; Seton et al., 2012). As it is primarily forming tectonic mélanges (Zheng, 2012). based on geological records in East Asia, in turn, the model provides constraints for reconstructing the paleo-PacificduringtheCNS(Fig. 10). 6. Discussions The formation of NW-SE-striking sinistral and dextral strike-slip fault systems and a series of NE-SW-trending compressional struc- 6.1. The Okhotomorsk Block before the Late Cretaceous tures between these systems in East Asia during the indentation phase of 100–89 Ma (Fig. 7a) suggests that the Izanagi Plate moved The area of the Okhotomorsk Block was reduced after collision with approximately northwestward during and just before this period East Asia, compression against NE Japan, and collision with Siberia in the (Fig. 10b, c), consistent with plate constructions of the paleo-Pacific Late Cretaceous (Figs. 6–9), and collision with Sakhalin Island during the Ocean (Smith, 2003; Norton, 2007). It was suggested that a global-scale Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115 111

(a) LateTriassic-Early Jurassic (b) Early Cretaceous

Eurasia SK

NCB KO NCB Thalassa K SCB SCB Telkhinia SK Ocean Thalassa K OK Izanagi Ocean Farallon Pontus Izanagi Tethys Farallon Tethys Ocean OK Pacific

Phoenix Phoenix

Siberia Siberia OK Izanagi Eurasia Eurasia Izanagi NCB NCB

SCB OK SCB

Farallon Pacific Pacific Farallon

Phoenix

Fig. 10. Schematic tectonic reconstruction of the paleo-Pacific Ocean (a) during the Late Triassic–Early Jurassic (modified from Van der Meer et al., 2012), (b) during the Early Cretaceous (modified from Smith, 2003, 2007; Seton et al., 2012; Van der Meer et al., 2012), (c) during 100–89 Ma (modified from Smith, 2003, 2007; Seton et al., 2012), and (d) during 79–77 Ma (modified from Smith, 2003, 2007; Norton, 2007). Yellow zigzag schematically shows the spreading ridge. Red lines with triangles denote subduction zones or presumed subdcution zones. K: Kurosegawa Belt; KO: Kolyma-Omolon Block; NCB: North China Block; OK: Okhotomorsk Block; SCB: South China Block; SK: South Kitakami Belt. plate reorganization event occurred at 105–100 Ma probably resulted 10c, d), indicating an average speed of 22.5 cm/yr. Taking into account from the eastern Gondwanaland subduction cessation (Matthews et al., the low velocities associated with continental collision during the last 2012). However, the compressional records in East Asia (Graham et al., 2 million years, this estimated speed is entirely consistent with esti- 2001; Meng et al., 2003; Zhang et al., 2003; Choi and Lee, 2011) which mates of 23.3–23.8 cm/yr, the speed of the north-northwestward- were used to support the hypothesis of the global-scale event are moving Izanagi Plate during the early Late Cretaceous (Engebretson reinterpreted here as products of the continental collision of the et al., 1985). The rapidly northward-moving Izanagi Plate during the Okhotomorsk Block with East Asia during 100–89 Ma (Fig. 7a). early Late Cretaceous resulted in the large-scale northward motion of The consistence between the onset of the northeastward oblique the Early Cretaceous oceanic crust which was rapidly subducted and ac- motion of the Okhotomorsk Block along the East Asian margin at around creted along the Asian margin during the Campanian time (Taira et al., 89 Ma and a rapid change of about 20° from northwestward to north- 1988; Taira, 2001). northwestward in the direction of Pacific-Izanagi motion between 90 and 84 Ma (Norton, 2007)(Figs. 7a, 8a, and 10c, d) supports the sugges- 6.3. The Okhotomorsk–East Asia collision and the Early Cretaceous and tion that a significant reorganization of the paleo-Pacific Ocean occurred Cenozoic extensional events in East China at around 90 Ma (Norton, 2007). One hypothesis to explore in this regard is that the Okhotomorsk–East Asia collision during 100–89 Ma It is well known that extensional events widely occurred in East slowed down the northwestward motion of the Izanagi Plate China, in the Early Cretaceous, and in the latest Cretaceous–Cenozoic, (Fig. 10c), while slab pull forces, originating from subduction of the respectively (Watson et al., 1987; Ren et al., 2002; Zhu et al., 2012). In Izanagi Plate beneath the Siberian margin, eventually redirected the the last decade, Chinese and Western geologists have paid much atten- Izanagi Plate from northwestward to north-northwestward motion tion to the Early Cretaceous cratonic destruction of the North China (Fig. 10d). In addition, the northward motion of the Okhotomorsk Block and numerous studies have suggested that extensional structures Block during 89–77 Ma implies that the scenario that the Izanagi Plate including metamorphic core complexes (e.g. Wang et al., 2011), exten- moved in a westward direction throughout the Cretaceous (Seton sional basins (e.g. Meng, 2003), and syntectonic plutons (e.g. Wu et al., et al., 2012) is possibly unrealistic. 2005) formed in East China mainly between 140 and 110 Ma (Lin et al., Based on the new tectonic model here, the speed of the 2013). The latest Cretaceous–Cenozoic episode began after 80 Ma with Okhotomorsk Block can be estimated during 89–77 Ma. In the 12 mil- the main extensional period in the Paleogene (Ren et al., 2002). Many lion years, it traveled about 2700 km in a N–S direction (Figs. 7–9, and extensional basins filled with Cenozoic sediments of thousands of 112 Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115 meters developed in East China and have become important oil- structures, triggering intense magmatic activities along the margin. producing regions. 40Ar–39Ar dating of basalts in the lower part of the During 79–77 Ma, the Okhotomorsk collided with Siberia in Northeast Upper Cretaceous Wangshi Formation in the Jiaolai Basin (JB) shows Asia. an age of 73.5 ± 0.3 Ma, indicating the onset of this extensional episode The new tectonic model spatially and temporally connects main in the eastern North China Block (J. Yan et al., 2003)(Fig. 1). It is clear geological events occurred in East Asia during the early Late Cretaceous, that there was a long gap of at least 30 million years between these and establishes process relationships between onshore geological two extensional events (Watson et al., 1987; Ren et al., 2002). records and the plate configuration of the paleo-Pacific Ocean. It pro- Compared to above-mentioned two extensional events, fewer vides a basis for synthesizing diverse aspects of the geological evolution studies, so far, have been given to the early Late Cretaceous evolution of neighboring areas of East Asia during the Late Cretaceous: orogenesis, in East China. The main reason possibly is the lack of objects of study. strike-slip faulting, basin evolution, paleoclimatic change, accretion, There was a magmatic hiatus in East China during the early Late magmatism, metamorphism, etc. In the mean time, it suggests a perfect Cretaceous (Xu, 2001; Menzies et al., 2007). In East China, except in example of ancient continental transform boundaries. Of course, the SE China coast (Fig. 8a) (Charvet et al., 1994; Lapierre et al., 1997), detailed studies in local areas are much needed to test and refine the few igneous rocks formed during the early Late Cretaceous have been model in the future. found. Extensive areas, except the Songliao Basin (SLB), Subei-Yellow Sea Basin (SYB), and Jianghan Basin (JHB), became uplifted and erosion- Acknowledgments al areas during the early Late Cretaceous (Chen, 2000)(Figs. 7aand8a). Moreover, most of the early Late Cretaceous sediments in the Subei- This work was funded by the Projects ZC9850290129 and Yellow Sea Basin and Jianghan Basin have been deeply buried by the WK2080000026. I thank my colleagues Gerald Bryant, Fang Huang, – sediments accumulated in the latest Cretaceous Cenozoic extensional Wei Leng, Johnny MacLean, Yingming Sheng, and Yongfei Zheng for episode (Li and Lü, 2002). Therefore, the evolution of East China in their useful comments. Critical reviews by Jacques Charvet, Cari this period was generally and simply described as a part of a long exten- Johnson, and an anonymous reviewer assisted greatly in improving – sional episode of the Late Mesozoic Cenozoic time related to a succes- the manuscript. sive oceanic subduction of the paleo-Pacific Ocean (e.g. Watson et al., 1987; Ren et al., 2002; Xu, 2007; Zhu et al., 2012). Few studies have discussed the mechanisms of the magmatic hiatus and regional uplifting References in East China during the early Late Cretaceous. Adachi, Y., Wallis, S., 2008. Ductile deformation and development of andalusite micro- The Okhotomorsk–East Asia collision proposed here provides an structures in the Nukata area: constraints on the metamorphism and tectonics of – interpretation for the magmatic hiatus (Xu, 2001; Menzies et al., 2007) the Ryoke belt. Island Arc 17, 41 56. Ando, H., 2003. Stratigraphic correlation of Upper Cretaceous to Paleocene forearc basin and regional uplifting (Charvet et al., 1994; Lapierre et al., 1997; Chen, sediments in Northeast Japan: cyclic sedimentation and basin evolution. Journal of 2000; Ratschbacher et al., 2003)(Figs. 3 and 7a) in East China during Asian Earth Sciences 21, 921–935. the early Late Cretaceous. The new model clearly suggests that the Aoki, K., Maruyama, S., Isozaki, Y., Otoh, S., Yanai, S., 2011. Recognition of the Shimanto HP – metamorphic belt within the traditional Sanbagawa HP metamorphic belt: new per- Early Cretaceous extension and the latest Cretaceous Cenozoic exten- spectives of the Cretaceous–Paleogene tectonics in Japan. Journal of Asian Earth sion in East China was not a successive event, and they were possibly Sciences 42, 355–369. caused by different mechanisms (Cope and Graham, 2007). Further Aoki, K., Isozaki, Y., Yamamoto, S., Maki, K., Yokoyama, T., Hirata, T., 2012. Tectonic erosion fi fi in a Paci c-type orogen: detrital zircon response to Cretaceous tectonics in Japan. studies are needed to nd if there was a direct relationship between Geology 40, 1087–1090. this collisional event along the East Asian margin during the early Late Baes, M., Govers, R., Wortel, R., 2011. Subduction initiation along the inherited weakness Cretaceous and the ending of the Early Cretaceous extensional event in zone at the edge of a slab: insights from numerical models. Geophysical Journal Inter- national 184, 991–1008. East Asia. It is suggested here that the regional uplifting and crustal Bartolini, A., Larson, R.L., 2001. Pacific microplate and the Pangea supercontinent in the thickening in East Asia during the Okhotomorsk-East Asia collision Early to Middle Jurassic. Geology 29, 735–738. in 100–89 Ma (Fig. 7a) probably provided a basis for the latest Bijwaard, H., Spakman, W., Engdahl, E.R., 1998. Closing the gap between regional and – Cretaceous-Cenozoic extension in East China, although they were global travel-time tomography. Journal of Geophysical Research 103, 30055 30078. Bindeman, I.N., Vinogradov, V.I., Valley, J.W., Wooden, J.L., Natal'in, B.A., 2002. Archean not necessarily the main controlling factors. protolith and accretion of crust in Kamchatka: SHRIMP dating of zircons from Sredinny and Ganal massifs. Journal of Geology 110, 271–289. – 7. Conclusions Cai, M., He, L., Liu, G., Wu, D., Huang, H., 2006. SHRIMP zircon U Pb dating of the intrusive rocks in the Dachang tin-polymetallic ore field, Guangxi and their geological significance. (in Chinese with English abstract) Geological Review 52, 409–414. Based on data from stratigraphy, thermochronology, structural Charvet, J., 2013. Late Paleozoic–Mesozoic tectonic evolution of SW Japan: a review— geology, petrology, geochemistry, and geophysics in different parts of reappraisal of the accretionary orogeny and revalidation of the collisional model. Journal of Asian Earth Sciences 72, 88–104. East Asia, a new tectonic model at the East Asian margin during the Charvet, J., Lapierre, H., Yu, Y., 1994. Geodynamic significance of the Mesozoic volcanism early Late Cretaceous is set forth, here. The key elements of this model of southeastern China. Journal of Southeast Asian Earth Sciences 9, 387–396. are the major collision of the Okhotomorsk Block with East Asia during Chekhovich, V.D., Sukhov, A.N., Kononov, M.V., Palandzhyan, S.A., 2009. Geodynamics of fi – – the northwestern sector of the paci c mobile belt in the Late Cretaceous Early 100 89 Ma and the oblique strike-slip motion of the Okhotomorsk Paleogene. Geotectonics 43, 111–132. Block along the NE-striking Asian margin during 89–83 Ma. Collision Chen, P., 2000. Paleoenvironmental changes during the Cretaceous in eastern China. and indentation of the Okhotomorsk Block within the East Asian margin In: Okada, H., Mateer, N.J. (Eds.), Cretaceous Environments of Asia. Elsevier Science, – pp. 81–90. resulted in regional NW SE shortening and orogenic exhumation in Chen, Y.X., Chen, W.J., 1997. Mesozoic volcanic rocks in Western Liaoning Province and its East Asia, and a progressive eclogite metamorphism of Sanbagawa adjacent areas: geochronology, geochemistry, and tectonic setting. Seismology Press, rocks in Southwest Japan. The northeastward oblique motion of the Beijing 279 pp. (in Chinese). Okhotomorsk formed a significant sinistral continental transform Choi, T., Lee, Y.I.L., 2011. Thermal histories of Cretaceous basins in Korea: implications for response of the East Asian continental margin to subduction of the Paleo-Pacificplate. boundary between the Eurasian Plate and Izanagi Plate, similar to the Island Arc 20, 371–385. San Andreas fault system in California. Sanbagawa metamorphic rocks Cogné, J.P., Kravchinsky, V.A., Halim, N., Hankard, F., 2005. Late Jurassic–Early Cretaceous were rapidly exhumed through the several-kilometer wide ductile closure of the Mongol-Okhotsk Ocean demonstrated by new Mesozoic palaeomagnetic results from the Trans-Baikal area (SE Siberia). Geophysical Journal shear zone at the lower crust and upper mantle level, and accretionary International 163, 813–832. complexes were subdivided into narrow and subparallel belts by Cope, T., Graham, S.A., 2007. Upper crustal response to Mesozoic tectonism in western the upper crustal strike-slip fault system. The departure of the Liaoning, North China, and implications for lithospheric delamination. In: Zhai, M.G., Windley, B.F. Kusky T.M., Meng Q. (Eds.), Mesozoic Sub-continental Lithospher- Okhotomorsk from the NE-striking Asian margin led to the occurrence ic Thinning under Eastern Asia. Geological Society, London. Special Publications 280, of an extensional setting and tilting of previously formed crustal 201–222. Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115 113

Cui, J., Liu, X., Dong, S., Hu, J., 2012. U–Pb and 40Ar/39Ar geochronology of the Tongbai Isozaki, Y., Aoki, K., Nakama, T., Yanai, S., 2010. New insight into a subduction related complex, central China: implications for Cretaceous exhumation and lateral extrusion orogen: a reappraisal of the geotectonic framework and evolution of the Japanese of the Tongbai–Dabie HP/UHP terrane. Journal of Asian Earth Sciences 47, 155–170. Islands. Gondwana Research 18, 82–105. Enami, M., Mizukami, T., Yokoyama, K., 2004. Metamorphic evolution of garnet-bearing Itaya, T., Tsujimori, T., Liou, J.G., 2011. Evolution of the Sanbagawa and Shimanto high- ultramafic rocks from the Gongen area, Sanbagawa belt, Japan. Journal of Metamor- pressure belts in SW Japan: insights from K–Ar (Ar–Ar) geochronology. Journal of phic Geology 22, 1–15. Asian Earth Sciences 42, 1075–1090. Endo, S., Wallis, S.R., Hirata, T., Anczkiewicz, R., Platt, J.P., Thirlwall, M., Asahara, Y., 2009. Ito, T., Kojima, Y., Kodaira, S., Sato, H., Kaneda, Y., Iwasaki, T., Kurashimo, E., Tsumura, N., Age and early metamorphic history of the Sanbagawa belt: Lu–Hf and P–Tconstraints Fujiwara, A., Miyauchi, T., Hirata, N., Harder, S., Miller, K., Murata, A., Yamakita, S., from the Western Iratsu eclogite. Journal of Metamorphic Geology 27, 371–384. Onishi, M., Abe, S., Sato, T., Ikawa, T., 2009. Crustal structure of southwest Japan, Engebretson, D.C., Cox, A., Gordon, R.G., 1985. Relative motions between oceanic and revealed by the integrated seismic experiment Southwest Japan 2002. Tectonophysics continental plates in the Pacific Basin. Geological Society of America Special Paper, 472, 124–134. 206, pp. 1–58. Itoh, Y., Amano, K., Danhara, T., 2000. Paleomagnetism, rock magnetism, and fission track Enkelmann, E., Ratschbacher, L., Jonckheere, R., Nestler, R., Fleischer, M., Gloaguen, R., dating of the Kurihashi Granodiorite in northeast Japan: evidence for a Cretaceous Hacker, B.R., Zhang, Y.Q., Ma, Y.S., 2006. Cenozoic exhumation and deformation of hydrothermal event and differential rotation along the eastern Eurasian margin. northeastern Tibet and the Qinling: is Tibetan lower crustal flow diverging around Journal of Geophysical Research 105, 13519–13532. the Sichuan Basin? Geological Society of America Bulletin 118, 651–671. Johnson, C.L., 2004. Polyphase evolution of the East Gobi basin: sedimentary and structural Feng, Z., Jia, C., Xie, X., Zhang, S., Feng, Z., Cross, T.A., 2010. Tectonostratigraphic units and records of Mesozoic–Cenozoic intraplate deformation in Mongolia. Basin Research 16, stratigraphic sequences of the nonmarine Songliao basin, northeast China. Basin 79–99. Research 22, 79–95. Jolivet, L., Cadet, J.P., Lalevée, F., 1988. Mesozoic evolution of Northeast Asia and the Gorbatov, A., Widiyantoro, S., Fukao, Y., Gordeev, E., 2000. Signature of remnant slabs in collision of the Okhotsk microcontinent. Tectonophysics 149, 89–109. the North Pacific from P-wave tomography. Geophysical Journal International 142, Kamp, P.J.J., Takemura, K., 1993. Thermo-tectonichistory of Ryoke Basement in 27–36. Hohi volcanic zone, northeast Kyushu, Japan: constraints from fission track Graham, S.A., Hendrix, M.S., Johnson, C.L., Badamgarav, D., Badarch, G., Amory, J., Porter, thermochronology. Island Arc 2, 213–227. M., Barsbold, R., Webb, L.E., Hacker, B.R., 2001. Sedimentary record and tectonic Kanaori, Y., 1990. Late Mesozoic–Cenozoic strike-slip and block rotation in the inner belt implications of Mesozoic rifting in southeast Mongolia. Geological Society of America of Southwest Japan. Tectonophysics 177, 381–399. Bulletin 113, 1560–1579. Kato, K., Saka, Y., 2003. Kurosegawa Terrane as a transform fault zone in Southwest Japan. Grimmer, J.C., Jonckheere, R., Enkelmann, E., Ratschbacher, L., Hacker, B.R., Blythe, A., Gondwana Research 6, 669–686. Wagner, G.A., Liu, S., Dong, S., 2002. Cretaceous–Tertiary history of the southern Kirillova, G.L., 2003. Late Mesozoic–Cenozoic sedimentary basins of active continental Tan-Lu fault zone: apatite fission track and structural constraints from the Dabie margin of Southeast Russia: paleogeography, tectonics, and coal–oil–gas presence. Shan. Tectonophysics 359, 225–253. Marine and Petroleum Geology 20, 385–397. Guillot, S., Hattori, K., Agard, P., Schwartz, S., Vidal, O., 2009. Exhumation processes in Koppers, A.A.P., Staudigel, H., Duncan, R.A., 2003. High-resolution 40Ar/39Ar dating of the oceanic and continental subduction contexts: a review. In: Lallemand, S., Funiciello, oldest oceanic basement basalts in the western Pacific basin. Geochemistry, Geophysics, F. (Eds.), Subduction Zone Geodynamics. Springer-Verlag, Berlin Heidelberg, Geosystems 4, 8914. http://dx.doi.org/10.1029/2003GC000574. pp. 175–205. Kravchinsky, V.A., Sorokin, A.A., Courtillot, V., 2002. Paleomagnetism of Paleozoic and Hada, S., Ishii, K., Landis, C.A., Aitchison, J., Yoshikura, S., 2001. Kurosegawa Terrane in Mesozoic sediments from the southern margin of Mongol-Okhotsk ocean, far eastern Soutwest Japan: disrupted remnants of a Gondwana-derived terrane. Gondwana Russia. Journal of Geophysical Research 107 (B10), 2253. http://dx.doi.org/10.1029/ Research 4, 27–38. 2001JB000672. Hall, R., 2002. Cenozoic geological and plate tectonic evolution of SE Asia and the SW Lapierre, H., Jahn, B.M., Charvet, J., Yu, Y.W., 1997. Mesozoic magmatism in Zhejiang Pacific: computer-based reconstructions, model and animations. Journal of Asian Province and its relation with the tectonic activities in SE China. Tectonophysics Earth Sciences 20, 353–432. 274, 321–338. Hall, C.E., Gurnis, M., Sdrolias, M., Lavier, L.L., Muller, R.D., 2003. Catastrophic initiation of Li, G., Lü, M., 2002. Atlas of Chinese Petroliferous Basins. (in Chinese) Petroleum Industry subduction following forced convergence across fracture zones. Earth and Planetary Press, Beijing, 492 pp. Science Letters 212, 15–30. http://dx.doi.org/10.1016/S0012-821X(03)00242-5. Li, X., Song, Y., 2010. Meso-Cenozoic uplift and exhumation of the Lüliangshan Mountains: Hara, H., Kimura, K., 2008. Metamorphic and cooling history of the Shimanto accretionary constraint from fission track thermochronology. Acta Geologica Sinica 84, 296–305 complex, Kyushu, Southwest Japan: implications for the timing of out-of-sequence (English Edition). thrusting. Island Arc 17, 546–559. Li,X.,Gong,G.,Yang,X.,Zeng,Q.,2010.Late Cretaceous–Cenozoic exhumation of the Yanji Hasegawa, T., Pratt, L.M., Maeda, H., Shigeta, Y., Okamoto, T., Kase, T., Uemura, K., 2003. area, NE China: constraints from fission track thermochronology. Island Arc 19, Upper Cretaceous stable carbon isotope stratigraphy ofterrestrial organic matter 120–133. from Sakhalin, Russian Far East: a proxy for the isotopic composition of Li, X., Yang, X., Xia, B., Gong, G., Shan, Y., Zeng, Q., Li, W., Sun, W., 2011. Exhumation of the paleoatmospheric CO2. Palaeogeography, Palaeoclimatology, Palaeoecology 189, Dahinggan Mountains, NE China from the Late Mesozoic to the Cenozoic: new 97–115. evidence from fission-track thermochronology. Journal of Asian Earth Sciences 42, Hasegawa, H., Tada, R., Ichinnorov, N., Minjin, C., 2009. Lithostratigraphy and depositional 123–133. environments of the Upper Cretaceous Djadokhta Formation, Ulan Nuur basin, Lin, W., Faure, M., Chen, Y., Ji, W., Wang, F., Wu, L., Charles, N., Wang, J., Wang, Q., 2013. Late southern Mongolia, and its paleoclimatic implication. Journal of Asian Earth Sciences Mesozoic compressional to extensional tectonics in the Yiwulüshan massif, NE China 35, 13–26. and its bearing on the evolution of the Yinshan–Yanshan orogenic belt: Part I: Structural Henstock, T.J., Levander, A., Hole, J.A., 1997. Deformation in the Lower Crust of the San analyses and geochronological constraints. Gondwana Research 23, 54–77. Andreas Fault System in Northern California. Science 278, 650–653. Lithgow-Bertelloni, C., Richards, M.A., 1998. Dynamics of Cenozoic and Mesozoic plate Hill, D.P., Eaton, J.P., Jones, L.M., 1990. Seismicity, 1980–86. In: Wallace, R.E. (Ed.), The San motions. Reviews of Geophysics 36, 27–78. Andreas Fault System, California. United States Geological Survey Professional Paper, Liu, S., Deng, B., Li, Z., Sun, W., 2012. Architecture of basin–mountain systems and their 1515, pp. 115–151. influences on gas distribution: a case study from the Sichuan basin, South China. Holdsworth, R.E., van Diggelen, E.W.E., Spiers, C.J., de Bresser, J.H.P., Walker, R.J., Bowen, L., Journal of Asian Earth Sciences 47, 204–215. 2011. Fault rocks from the SAFOD core samples: implications for weakening at Ma, L.F. (Ed.), 2002. Geological Atlas of People's Republic of China. Chinese Map Publishing shallow depths along the San Andreas Fault, California. Journal of Structural Geology House, Beijing. 33, 132–144. Ma, Y., Chen, H., Wang, G., 2009. Atlas of tectonics and sequence lithofacies Hourigan, J.K., Akinin, V.V., 2004. Tectonic and chronostratigraphic implications of new palaeogeography in South China from Sinian to Neogene. Science Press, Beijing 301 40Ar/39Ar geochronology and geochemistry of the Arman and Maltan-Ola volcanic pp. (in Chinese). fields, Okhotsk–Chukotka volcanic belt, northeastern Russia. Geological Society of Maruyama, S., Banno, S., Matsuda, T., Nakajima, T., 1984. Kurosegawa zone and its bearing America Bulletin 116, 637–654. on the development of the Japanese Islands. Tectonophysics 110, 47–60. Hu, S., Kohn, B.P., Raza, A., Wang, J., Gleadow, A.J.W., 2006. Late Mesozoic and Cenozoic Maruyama, S., Isozaki, Y., Kimura, G., Terabayashi, M., 1997. Paleogeographic maps of the thermotectonic evolution along a transect from the north China craton through the Japanese Islands: plate tectonic synthesis from 750 Ma to the present. Island Arc 6, Qinling orogen into the Yangtze craton, central China. Tectonics 25, TC6009. 121–142. Hu, G., Hu, W., Cao, J., Yao, S., Xie, X., Li, Y., Liu, Y., Wang, X., 2012. Deciphering the Matthews, K.J., Seton, M., Müller, R.D., 2012. A global-scale plate reorganization event at Early Cretaceous transgression in coastal southeastern China: constraints based on 105–100 Ma. Earth and Planetary Science Letters 355–356, 283–298. petrography, paleontology and geochemistry. Palaeogeography, Palaeoclimatology, Meade, B.J., Hager, B.H., 2005. Block models of crustal motion in southern California Palaeoecology 317–318, 182–195. constrained by GPS measurements. Journal of Geophysical Research 110, B03403. Huang, J., Zhao, D., 2006. High-resolution mantle tomography of China and surrounding http://dx.doi.org/10.1029/2004JB003209. regions. Journal of Geophysical Research 111, B09305. Meng, Q.R., 2003. What drove late Mesozoic extension of the northern China–Mongolia Hwang, B.H., Ernst, W.G., McWilliams, M., Yang, K., 2008. Geometric model of conjugate tract? Tectonophysics 369, 155–174. faulting in the Gyeongsang Basin, southeast Korea. Tectonics 27, TC6015. Meng, Q.R., Hu, J.M., Jin, J.Q., Zhang, Y., Xu, D.F., 2003. Tectonics of the late Mesozoic wide Ishida, K., Kozai, T., Park, S.O., Mitsugi, T., 2003. Gravel bearing radiolaria as tracers for extensional basin system in the China–Mongolia border region. Basin Research 15, erosional events: a review of the status of recent research in SW Japan and Korea. 397–415. Journal of Asian Earth Sciences 21, 909–920. Menzies, M., Xu, Y., Zhang, H., Fan, W., 2007. Integration of geology, geophysics and Isozaki, Y., 1996. Anatomy and genesis of a subduction-related orogen: a new view of geochemistry: a key to understanding the North China Craton. Lithos 96, 1–21. geotectonic subdivision and evolution of the Japanese Islands. Island Arc 5, 289–320. Metelkin, D.V., Vernikovsky, V.A., Kazansky, A.Y., Wingate, M.T.D., 2010. Late Mesozoic Isozaki, Y., Itaya, T., 1990. Chronology of Sanbagawa metamorphism. Journal of Metamor- tectonics of Central Asia based on paleomagnetic evidence. Gondwana Research 18, phic Geology 8, 401–411. 400–419. 114 Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115

Minamishin, M., Yanagi, T., Yamaguchi, M., 1979. Rb–Sr whole rock ages of the Sanbagawa Taira, A., Katto, J., Tashiro, M., Okamura, M., Kodama, K., 1988. The Shimanto Belt in metamorphic rocks in central Shikoku. In: Yamaguchi, M. (Ed.), Isotope Geoscience of Shikoku, Japan: evolution of Cretaceous to Miocene accretionary prism. Modern the Japanese Islands (in Japanese). Report for Scientific Research of the Ministry of Geology 12, 5–46. Education of Japan (No. 334054), pp. 68–71. Takagi, H., 1986. Implications of mylonitic microstructures for the geotectonic evolution Moore, D.E., Rymer, M.J., 2007. Talc-bearing serpentinite and the creeping section of the of the Median Tectonic Line, central Japan. Journal of Structural Geology 8, 3–14. San Andreas fault. Nature 448, 795–797. Terekhov, E.P., Mozherovsky, A.V., Tsoy, I.B., Lelikov, E.P., Vashchenkova, N.G., Gorovaya, Nakajima, T., 1994. The Ryoke plutonometamorphic belt: crustal section of the Cretaceous M.T., 2012. Late Mesozoic and Cenozoic volcanosedimentary complexes from the Eurasian continental margin. Lithos 33, 51–66. submarine Vityaz Ridge, the island arc slope of the Kuril–Kamchatka trench, and its Nakama, T., Hirata, T., Otoh, S., Aoki, K., Yanai, S., Maruyama, S., 2010. Paleogeography of evolution. Russian Journal of Pacific Geology 6, 209–216. the Japanese Islands: age spectra of detrital zircon and provenance history of the Tikhomirov, P.L., Kalinina, E.A., Moriguti, T., Makishima, A., 2012. The Cretaceous orogen. (in Japanese with English abstract) Journal of Geography 119, 1161–1172. Okhotsk–Chukotka Volcanic Belt (NE Russia): Geology, geochronology, magma Noda, A., Toshimitsu, S., 2009. Backward stacking of submarine channel-fan successions output rates, and implications on the genesis of silicic LIPs. Journal of Volcanology controlled by strike-slip faulting: the Izumi Group (Cretaceous), southwest Japan. and Geothermal Research 221–222, 14–32. Lithosphere 1, 41–59. Tivey, M.A., Larson, R., Schouten, H., Pockalny, R., 2005. Downhole magnetic measure- Norton, I.O., 2007. Speculations on Cretaceous tectonic history of the northwest Pacific ments of ODP Hole 801C: implications for Pacific oceanic crust and magnetic field and a tectonic origin for the Hawaii hotspot. In: Foulger, G.R., Jurdy, D.M. (Eds.), behavior in the Middle Jurassic. Geochemistry, Geophysics, Geosystems 6, Q04008. Plates, Plumes, and Planetary Processes. Geological Society of America Special http://dx.doi.org/10.1029/2004GC000754. Paper, 430, pp. 451–470. Toth, J., Gurnis, M., 1998. Dynamics of subduction initiation at pre-existing fault zones. Okamoto, K., Shinjoe, H., Katayama, I., Terada, K., Sano, Y., Johnson, S., 2004. SHRIMP U–Pb Journal of Geophysical Research 103, 18,053–18,067. http://dx.doi.org/10.1029/ zircon dating of quartz-bearing eclogite from the Sanbagawa Belt, southwest Japan: 98JB01076. implications for metamorphic evolution of subducted protolith. Terra Nova 16, Uno, K., Furukawa, K., Hada, S., 2011. Margin-parallel translation in the western Pacific: 81–89. paleomagnetic evidence from an allochthonous terrane in Japan. Earth and Planetary Okudaira, T., Hayasaka, Y., Himeno, O., Watanabe, K., Sakurai, Y., Ohtomo, Y., 2001. Cooling Science Letters 303, 153–161. and inferred exhumation history of the Ryoke metamorphic belt in the Yanai district, Utsunomiya, A., Jahn, B.M., Okamoto, K., Ota, T., Shinjoe, H., 2011. Intra-oceanic island arc southwest Japan: constraints from Rb–Sr and fission-track ages of gneissose granitoid origin for Iratsu eclogites of the Sanbagawa belt, central Shikoku, southwest Japan. and numerical modeling. Island Arc 10, 98–115. Chemical Geology 280, 97–114. Okudaira, T., Beppu, Y., Yano, R., Tsuyama, M., Ishii, K., 2009. Midcrustal horizontal shear Van der Meer, D.G., Torsvik, T.H., Spakman, W., van Hinsbergen, D.J.J., Amaru, M.L., 2012. zone in the forearc region of the mid-Cretaceous SW Japan arc, inferred from strain Intra-Panthalassa Ocean subduction zones revealed by fossil arcs and mantle struc- analysis of rocks within the Ryoke metamorphic belt. Journal of Asian Earth Sciences ture. Nature Geoscience 5, 215–219. 35, 34–44. Wakita, K., 2013. Geology and tectonics of Japanese islands: a review—the key to under- Ota, T., Terabayashi, M., Katayama, I., 2004. Thermobaric structure and metamorphic standing the geology of Asia. Journal of Asian Earth Sciences 72, 75–87. evolution of the Iratsu eclogite body in the Sanbagawa belt, Central Shikoku, Japan. Wallis, S.R., Endo, S., 2010. Comment on ‘Metamorphic P–T–time history of the Lithos 73, 95–126. Sanbabawa belt in central Shikoku, Japan and implication for retrograde metamorphism Otsuki, K., 1992. Oblique subduction, collision of microcontinents and subduction of during exhumation’ by Aoki et al. (Lithos 113 (2009) 393-407). Lithos 116, 195–196. oceanic ridge: their implications on the Cretaceous tectonics of Japan. Island Arc 1, Wallis, S., Anczkiewicz, R., Endo, S., Aoya, M., Platt, J.P., Thirlwall, M., Hirata, T., 2009. 51–63. Movements, ductile deformation and geochronology of the Sanbagawa belt, SW Parfenov, L.M., Natal'in, B.A., 1986. Mesozoic tectonic evolution of NE Asia. Tectonophysics Japan: tectonic significance of 88–89 Ma Lu–Hf eclogite ages. Journal of Metamorphic 127, 291–304. Geology 27, 93–105. Parsons, T., Thatcher, W., 2011. Diffuse Pacific–North American plate boundary: 1000 km Wang, X., Zhong, D., Wang, Y., 2008. Geometry, kinematics and thermochronology study of dextral shear inferred from modeling geodetic data. Geology 39, 943–946. of the Late Mesozoic movement of NW-trending faults, Western Shandong. (in Pavlenkova, N.I., Pilipenko, V.N., Verpakhovskaja, A.O., Pavlenkova, G.A., Filonenko, V.P., Chinese with English abstract) Acta Geologica Sinica 82, 1258–1273. 2009. Crustal structure in Chile and Okhotsk Sea regions. Tectonophysics 472, 28–38. Wang, T., Zheng, Y., Zhang, J., Zeng, L., Donskaya, T., Guo, L., Li, J., 2011. Pattern and kine- Platt, J.P., Becker, T.W., 2010. Where is the real transform boundary in California? matic polarity of late Mesozoic extension in continental NE Asia: perspectives from Geochemistry, Geophysics, Geosystems 11, Q06012. http://dx.doi.org/10.1029/ metamorphic core complexes. Tectonics 30, TC6007. http://dx.doi.org/10.1029/ 2010GC003060. 2011TC002896. Platt, J.P., Behr, W.M., 2011. Deep structure of lithospheric fault zones. Geophysical Watson, M.P., Hayward, A.B., Parkinson, D.N., Zhang, Z.M., 1987. Plate tectonic history, Research Letters 38, L24308. http://dx.doi.org/10.1029/2011GL049719. basin development and petroleum source rock deposition onshore China. Marine Ratschbacher, L., Hacker, B.R., Calvert, A., Webb, L.E., Grimmer, J.C., McWilliams, M.O., Ireland, and Petroleum Geology 4, 205–225. T.,Dong,S.,Hu,J.,2003.Tectonics of the Qinling (Central China): tectonostratigraphy, Wintsch, R.P., Byrne, T., Toriumi, M., 1999. Exhumation of the Sanbagawa blueschist belt, geochronology, and deformation history. Tectonophysics 366, 1–53. SW Japan, by lateral flow and extrusion: evidence from structural kinematics and Ren, J., Tamaki, K., Li, S., Zhang, J., 2002. Late Mesozoic and Cenozoic rifting and its dynamic retrograde P–T–t paths. In: Ring, U., Brandon, M.T., Lister, G.S., Willett, S.D. (Eds.), setting in eastern China and adjacent areas. Tectonophysics 344, 175–205. Exhumation Processes: Normal Faulting, Ductile Flow and Erosion. Geological Society, Roy, M., Royden, L.H., 2000. Crustal rheology and faulting at strike-slip boundaries: 2. London, Special Publications, 154, pp. 129–155. Effects of lower crustal flow. Journal of Geophysical Research 105, 5599–5613. Wintsch, R.P., Yang, H.J., Li, X.H., Tung, K.A., 2011. Geochronologic evidence for a cold arc– http://dx.doi.org/10.1029/1999JB900340. continent collision: the Taiwan orogeny. Lithos 125, 236–248. Şengör, A.M.C., Natal'in, B.A., 1996. Palaeotectonics of Asia: fragments of a synthesis. In: Wu, Z., Wu, Z., 2003a. Low-temperature thermochonological analysis of the uplift history Yin, A., Harrison, M. (Eds.), The Tectonic Evolution of Asia. Rubey Colloquium, of the Yanshan Mountain and its neighboring area. (in Chinese with English abstract) Cambridge University Press, Cambridge, pp. 486–640. Acta Geologica Sinica 77, 399–406. Seton, M., Müller, R.D., Zahirovic, S., Gaina, C., Torsvik, T., Shephard, G., Talsma, A., Gurnis, Wu, Z., Wu, Z., 2003b. Uplift history of the Daqing Mountain since the Late Cretaceous. (in M., Turner, M., Maus, S., Chandler, M., 2012. Global continental and ocean basin Chinese with English abstract) Acta Geoscientia Sinica 24, 205–210. reconstructions since 200 Ma. Earth-Science Reviews 113, 212–270. Wu, F.Y., Lin, J.Q., Wilde, S.A., Zhang, X., Yang, J.H., 2005. Nature and significance of the Shen, C.B., Mei, L.F., Xu, S.H., 2009. Fission track dating of Mesozoic sandstone and its Early Cretaceous giant igneous event in eastern China. Earth and Planetary Science tectonic significance in the Eastern Sichuan Basin, China. Radiation Measurements Letters 233, 103–119. 44, 945–949. Xu, Y.G., 2001. Thermo-tectonic destruction of the Archean lithospheric keel beneath Shu,L.,Deng,P.,Wang,B.,Tan,Z.,Yu,X.,Sun,Y.,2004.Lithology, kinematics and geo- the Sino-Korean Craton in China: evidence, timing and mechanism. Physics and chronology related to Late Mesozoic basin-mountain evolution in the Nanxiong– Chemistry of the Earth 26, 747–757. Zhuguang area, South China. Science in China, Series D: Earth Sciences 47, Xu, Y.G., 2007. Diachronous lithospheric thinning of the North China Craton and forma- 673–688. tion of the Daxin'anling-Taihangshan gravity lineament. Lithos 96, 281–298. Smith, A.D., 2003. A reappraisal of stress field and convective roll models for the origin Xu, J., Gao, Z., Sun, J., Song, C., 2001. A preliminary study of the coupling relationship be- and distribution of Cretaceous to recent intraplate volcanism in the PacificBasin. tween basin and mountain in extensional environments—a case study of the Bohai International Geology Review 45, 287–302. Bay Basin and Taihang Mountain. (in Chinese with English abstract) Acta Geologica Smith, A.D., 2007. A plate tectonic model for Jurassic to recent intraplate volcanism in the Sinica 75, 165–174. Pacific Ocean basin. Geological Society of America Special Paper 430, 471–496 Yan, D.P., Zhou, M.F., Song, H.L., Wang, X.W., Malpas, J., 2003. Origin and tectonic signifi- (http://dx.doi.org/10.1130/2007.2430(23)). cance of a Mesozoic multi-layer over-thrust system within the Yangtze Block (South Stone, D.B., Minyuk, P., Kolosev, E., 2003. New paleomagnetic paleolatitudes for the China). Tectonophysics 361, 239–254. Omulevka terrane of northeast Russia: a comparison with the Omolon terrane and Yan, J., Chen, J., Xie, Z., Zhou, T., 2003. Mantle xenoliths from Late Cretaceous basalt in the eastern Siberian platform. Tectonophysics 377, 55–82. eastern Shandong Province: new constraint on the timing of lithospheric thinning Suzuki, K., Adachi, M., 1998. Denudation history of the high T/P Ryoke metamorphic belt, in eastern China. (in Chinese with English abstract) Chinese Science Bulletin 48, southwest Japan: constraints from CHIME monazite ages of gneisses and granitoids. 2139–2144. Journal of Metamorphic Geology 16, 23–37. Yan, Y., Hu, X., Lin, G., Santosh, M., Chan, L.S., 2011. Sedimentary provenance of the Taira, A., 2001. Tectonic evolution of the Japanese island arc system. Annual Review of Hengyang and Mayang basins, SE China, and implications for the Mesozoic topo- Earth and Planetary Sciences 29, 109–134. graphic change in South China Craton: evidence from detrital zircon geochronology. Taira, A., Saitoh, Y., Hashimoto, M., 1983. The role of oblique subduction and strike-slip Journal of Asian Earth Sciences 41, 494–503. tectonics in evolution of Japan. In: Hilde, T.W.C., Uyeda, S. (Eds.), Geodynamics of Yang, Y., Li, W., Ma, L., 2005. Tectonic and stratigraphic controls of hydrocarbon systems the Western Pacific–Indonesian Region. Geodynamic Series American Geophysical in the Ordos basin: a multicycle cratonic basin in central China. American Association Union, 11, pp. 303–316. of Petroleum Geologists Bulletin 89, 255–270. Y.-T. Yang / Earth-Science Reviews 126 (2013) 96–115 115

Yin, A., Nie, S., 1996. A Phanerozoic palinspastic reconstruction of China and its neighbor- Chinese with English abstract) International Journal of Geomechanics 15, ing regions. In: Yin, A., Harrison, T.M. (Eds.), The Tectonic Evolution of Asia. Cambridge 178–189. University Press, Cambridge, pp. 442–485. Zhang, Y., Shi, W., Dong, S., 2011. Changes of Late Mesozoic tectonic regimes around the Yui, T.F., Okamotoa, K., Usukia, T., Lan, C.Y., Chub, H.T., Liou, J.G., 2009. Late Triassic–Late Ordos Basin (North China) and their geodynamic implications. Acta Geologica Sinica Cretaceous accretion/subduction in the Taiwan region along the eastern margin of 85, 1254–1276. South China—evidence from zircon SHRIMP dating. International Geology Review Zhang, Y.B., Zhai, M., Hou, Q.L., Li, T.S., Liu, F., Hu, B., 2012. Late Cretaceous volcanic rocks 51, 304–328. and associated granites in Gyeongsang Basin, SE Korea: their chronological ages and Yui, T.F., Maki, K., Lan, C.Y., Hirata, T., Chu, H.T., Kon, Y., Yokoyama, T.D., Jahn, B.M., Ernst, tectonic implications for cratonic destruction of the North China Craton. Journal of W.G., 2012. Detrital zircons from the Tananao Metamorphic Complex of Taiwan: Asian Earth Sciences 47, 252–264. implications for sediment provenance and Mesozoic tectonics. Tectonophysics Zhao, G.C., Sun, M., Wilde, S.A., Li, S.Z., 2005. Late Archean to Paleoproterozoic evolution of 541–543, 31–42. the North China Craton: key issues revisited. Precambrian Research 136, 177–202. Zhang, C., Song, H., Wang, G., Yan, D., Sun, W., 2001. Mesozoic dextral strike-slip structural Zheng, Y.F., 2012. Metamorphic chemical geodynamics in continental subduction zones. system in middle segment of intraplate Yanshan Orogenic Belt, northern China. Chemical Geology 328, 5–48. (in Chinese with English abstract) Earth Science. Journal of China University of Zheng, Y., Yuan, W., Wang, D., Jiang, G., Zhu, D., Wang, C., Jia, Y., 2011. Exhumation history Geosciences 26, 464–472. of the Huangshan granite pluton, southern Anhui Province: new insights from Zhang, Y., Dong, S., Shi, W., 2003. Cretaceous deformation history of the middle Tan-Lu ﬁssion-track analysis. Science in China, Series D: Earth Sciences 54, 528–539. fault zone in the Shandong Province, eastern China. Tectonophysics 363, 243–258. Zhu, G., Jiang, D., Zhang, B., Chen, Y., 2012. Destruction of the eastern North China Craton Zhang, C., Wu, G., Wang, G., Zhang, W., Song, H., 2004. Northwest trending tectonic belt in in a backarc setting: evidence from crustal deformation kinematics. Gondwana the middle Yanshan Orogenic Belt of northeast Hebei Province, North China: Research 22, 86–103. tectonic evolution and geochronology. Science in China, Series D: Earth Sciences 47, Zonenshain, L.P., Kuzmin, M.I., Natapov, L.M., 1990. Geology of the USSR: a plate tectonic 896–911. synthesis. Geodynamic Series American Geophysical Union 21, 1–242. Zhang,R.Q.,Zhou,Y.,Wang,X.W.,Li,S.J.,Li,S.,2009.Structural features and tectonic Zorin, Y.A., 1999. Geodynamics of the western part of the Mongolia–Okhotsk collisional evolution of the Wei-Zi-Luo Fault Zone in southwestern Guizhou Province. (in belt, Trans-Baikal region (Russia) and Mongolia. Tectonophysics 306, 33–56.