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Magnetostratigraphy and Depositional History of the Miocene Wushan

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Magnetostratigraphy and Depositional History of the Miocene Wushan Journal of Asian Earth Sciences 44 (2012) 189–202 Contents lists available at ScienceDirect Journal of Asian Earth Sciences journal homepage: www.elsevier.com/locate/jseaes Magnetostratigraphy and depositional history of the Miocene Wushan basin on the NE Tibetan plateau, China: Implications for middle Miocene tectonics of the West Qinling fault zone ⇑ Wang Zhicai a,b, , Zhang Peizhen b, Carmala N. Garzione c, Richard O. Lease d,1, Zhang Guangliang b, Zheng Dewen b, Brian Hough c, Yuan Daoyang b, Li Chuanyou b, Liu Jianhui b, Wu Qinglong b a Institute of Earthquake Engineering, Shandong Earthquake Administration, Jinan 250014, China b Institute of Geology, China Earthquake Administration, National Laboratory of Earthquake Dynamics, Beijing 100029, China c Department of Earth and Environmental Sciences, University of Rochester, Rochester, NY 14627, USA d Department of Earth Science, University of California, Santa Barbara, CA 93106, USA article info abstract Article history: Based on field mapping, section measurement and magnetostratigraphy, 1700 m of sedimentary rocks Available online 19 July 2011 have accumulated in the Wushan basin between 16 Ma and 6 Ma. Basin geometry, sedimentation characteristics and the early syn-depositional deformation along the northern margin of the basin indi- Keywords: cate that formation of the Wushan basin was related to tectonic deformation along the West Qinling fault Middle Miocene zone during the middle Miocene. A series of basins of similar age to the Wushan basin were generated Wushan basin along and to the south of the West Qinling fault zone while basalts also erupted in this region at this time. West Qinling fault zone We suggest that the middle Miocene (16 Ma) may represent a change in kinematics and deformation Tibetan plateau style in the region along and to the south of the West Qinling fault zone. At this time, there was a tran- Magnetostratigraphy sition from NNE–SSW compressional deformation, that dominated the region since the late Paleogene, to the development of WNW–ESE and/or E–W trending strike-slip movement and associated transpression- al and transtensional activity that continues today. The Miocene Wushan basin may have developed in association with transpression along the West Qinling fault zone. Whether this transition was related to the onset of strike-slip along the east Kunlun fault and related deformation transfer, lower crustal flow, or removal of mantle lithosphere, the middle Miocene provides direct evidence for a change in the kine- matic style along the plateau margin. Ó 2011 Elsevier Ltd. All rights reserved. 1. Introduction (Yin et al., 2007, 2008a,b; Yin and Harrison, 2000; Yin et al., 2002) based on a number of lines of evidence, including: (1) the exhuma- The northeastern Tibetan plateau, which is bounded to the tion rates along the East Kunlun fault and the Altyn Tagh fault accel- south by the east Kunlun fault, and to the north by the Altyn Tagh erated in Eocene to early Oligocene (40 ± 10 Ma) (Jolivet et al., 2001); and Qilian-Haiyuan faults (Fig. 1), is an actively deforming part of (2) crustal thickening occurred along the northern and southern the Tibetan plateau (Molnar and Tapponnier, 1975; Meyer et al., margin of the Qaidam basin at 49 Ma (Yin et al., 2002) or between 1998; Tapponnier et al., 2001; Yin and Harrison, 2000). This region 50 and 65 Ma (Yin et al., 2007, 2008a,b); (3) clockwise rotation of is characterized by a series of Cenozoic basins and bordering 24° occurred in Xining–Minhe basin at 41 Ma (Dupont-Nivet mountain ranges controlled or sliced by strike-slip faults and re- et al., 2004, 2008); and (4) reverse faulting and associated mountain lated thrust faults, together providing archives of tectonic defor- uplift in the West Qinling region initiated at 45–50 Ma (Clark et al., mation and environmental change. 2010). However, the tectonic deformation that finally established Studies of Cenozoic basins and mountain ranges indicate that the modern NE Tibetan plateau initiated in the late Miocene deformation of the NE Tibetan plateau began in the late Paleogene (8 Ma) (Song et al., 2001; Yuan et al., 2003; Zheng et al., 2003; Fang et al., 2003; Molnar, 2005; Zhang et al., 2006; Jiang et al., 2007; Lin ⇑ Corresponding author at: Institute of Earthquake Engineering, Shandong et al., 2010) and lasted until the Pliocene and Quaternary (Li et al., Earthquake Administration, Jinan 250014, China. Tel.: +86 13853166836; fax: +86 1979). In recent years, evidence for early and middle Miocene defor- 053188515212. mation has been identified in this region. For instance, the eastern E-mail address: [email protected] (Z. Wang). 1 Laji shan experienced thrusting and became the main source of sed- Present address: Institut für Geowissenschaft, Universität Tübingen, 72074 Tübingen, Germany. iments for the Xunhua basin to the south at 22 Ma (Lease et al., 1367-9120/$ - see front matter Ó 2011 Elsevier Ltd. All rights reserved. doi:10.1016/j.jseaes.2011.06.009 190 Z. Wang et al. / Journal of Asian Earth Sciences 44 (2012) 189–202 Fig. 1. Tertiary geological map highlighting faults of the West Qinling fault zone. Faults, WQNFZ: the West Qinling fault zone, RYSF: the Riyueshan fault, LJSF: the Lajishan fault, MXSF: the Maxianshan fault, DCMX: the Dangchang-Minxian fault, XLF: the Lixian fault. Basins, XN: Xining basin, LNT: Lintan basin, LNX: Linxia basin, XH: Xunhua basin, TB: tianshui basin, NY: Nanyang basin, NDS: Niudingshan basin, XL: Xihe–Lixian basin, GJ: Ganjia basin, TR: Tongren basin, GD: Guide basin. Small circles labeled with ‘‘T’’ point the location of thermochrological thansects (by Lease et al., 2011, and Clark et al., 2010). This figure is based on Geological map of 1:1500000 Tibetan plateau and revised according to field observation. The inset shows the map location in which the Altyn Tagh fault (ATF), the east Kunlun fault (EKF), the West Qinling fault zone (WQNFZ), and the Haiyuan fault (HYF) are indicated. EQ: the East Qinling orogen, WQ: the West Qinling Orogen, QL: the Qilian Orogen, KL: the Kunlun Orogen, SPGZ: the Songpan-Ganzi terrane. 2011), the West Qinling range became a more pronounced source of terrane (Ratschbacher et al., 2003; Zhang et al., 2004; Zheng et al., sediment to the Linxia basin by 14 Ma (Garzione et al., 2005), and 2010)(Fig. 1). mountains to the south of the West Qinling fault zone show acceler- The West Qinling fault zone forms the northern boundary of the ated exhumation rates between 18 and 17 Ma (Clark et al., 2010). West Qinling orogenic belt and consists of several nearly parallel Therefore, the Cenozoic deformation history is rather complicated, faults (Fig. 1, Figs. 2 and 3). Thrust faults have developed on both and may consist of two or more stages (Harrison et al., 1992; sides of the fault zone (Figs. 2 and 3). Slip on the northern frontal Tapponnier et al., 2001; Yue et al., 2003). As for the kinematics of faults have thrusted pre-Cenozoic rocks and strata of the West major faults in this region, it seems that the strike-slip motion for Qinling northward and have formed the southern borders for major faults like the east Kunlun fault and the Haiyuan fault started several Cenozoic basins, such as Linxia, Xunhua, and Longxi basins, relatively late except for the long term left-lateral motion of the and the southern frontal faults dip northward and mark the north- Altyn Tagh fault (Yin and Harrison, 2000). The onset of strike-slip ern border of the Tange basin (Wang et al., 2006). An active, left- motion for the East Kunlun is at ca. 15 Ma (Jolivet et al., 2003), and lateral strike-slip fault is recognized in the middle part of the West the Haiyuan fault probably initiated in late Miocene or Pliocene time Qinling fault zone (Figs. 2 and 3), and its late Quaternary slip rate is (Burchfiel et al., 1991; Zhang et al., 1988, 1990). estimated to be 2 mm/yr (Li, 2005). However, this active strike- Based on the previous observations of long-term Cenozoic short- slip fault is not traceable to the west of the Taohe River (Fig. 1). ening in this region, this study focuses on the Miocene deformation To the north of the West Qinling fault zone, the Qilian block is a history of the West Qinling fault zone by exploiting the sedimenta- Paleozoic orogenic belt dominated by lower Proterozoic gneiss, tion history and magnetostratigraphy of the Wushan basin (Fig. 1). amphibolite, marble and schist and early Paleozoic metasediments The West Qiling fault zone is a significant structure on the NE that include phyllite, low-grade metamorphosed limestone and Tibetan plateau. It now marks part of the geomorphologic and siltstone. Most of the region is now covered by Cretaceous and topographic boundary of the NE margin of the Tibetan plateau Cenozoic red beds and loess, but early Paleozoic and Proterozoic and it also acts as the boundary for several Cenozoic basins rock and strata are commonly exposed in mountainous regions, (Fig. 1). Evidence of thrusting beginning in Paleogene time (Clark for instance, in the Laji Shan (Wang et al., 1997; Garzione et al., et al., 2010), together with documentation of active left-lateral 2005; Lease et al., 2007) (Fig. 1). To the south of the West Qinling strike-slip motion (Li, 2005) suggest that the West Qinling fault fault zone, Cenozoic, late Paleozoic, and Mesozoic strata are ex- zone has been active in the deformation process of the NE Tibetan posed, including Devonian, Carboniferous, Permian and Triassic plateau throughout Cenozoic time, and thus it played a role in the terrigenous metasediments and carbonates, such as sandstone, evolution of adjacent Cenozoic basins. However, the questions of siltstone, slate, and marine limestone (Fig.
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