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Cenozoic Magnetostratigraphy of the Xining Basin, NE Tibetan Plateau

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Cenozoic Magnetostratigraphy of the Xining Basin, NE Tibetan Plateau Earth-Science Reviews 190 (2019) 460–485 Contents lists available at ScienceDirect Earth-Science Reviews journal homepage: www.elsevier.com/locate/earscirev Cenozoic magnetostratigraphy of the Xining Basin, NE Tibetan Plateau, and T its constraints on paleontological, sedimentological and tectonomorphological evolution ⁎ Xiaomin Fanga,b, , Yahui Fanga,b, Jinbo Zana, Weilin Zhanga, Chunhui Songc, Erwin Appeld, Qingquan Mengc, Yunfa Miaoe, Shuang Daic, Yin Lua,d, Tao Zhanga a CAS Center for Excellence in Tibetan Plateau Earth Sciences and Key Laboratory of Continental Collision and Plateau Uplift, Institute of Tibetan Plateau Research, Chinese Academy of Sciences, Beijing 100101, China b College of Resources and Environment, University of Chinese Academy of Sciences, 19A Yuquan Road, Beijing 100049, China c School of Earth Sciences & Key Laboratory of Western China's Environmental Systems (MOE), Lanzhou University, Lanzhou 730000, China d Department of Geosciences, University of Tübingen, Hölderlinstr. 12, 72074 Tübingen, Germany e Key Laboratory of Desert and Desertification, Cold and Arid Regions Environmental and Engineering Institute, Chinese Academy of Sciences, Lanzhou 730000,China ARTICLE INFO ABSTRACT Keywords: The Xining Basin is well known for its thick and continuous sequence of fine-grained Cenozoic sediments. In Cenozoic magnetostratigraphy addition, it contains important Xiejia fauna which define the Xiejian Stage of the early Miocene in the standard Xiejia fauna Chinese land mammal zonation, and it also provides detailed histories of eolian dust deposition which document Eolian dust deposition the aridification of Asia, monsoon evolution and the initiation of the Yellow River in relation to the upliftof Xining Basin Tibetan Plateau. However, the results of magnetostratigraphic dating of the fossil-bearing sequence has yielded NE Tibet uplift conflicting ages for the fauna and stratigraphy, hindering the use of the sequence for addressing majorpa- leoenvironmental and paleoclimatic issues. Here, we review the paleontological, lithological and magnetos- tratigraphic record of the Xining Basin and provide a new, long and continuous high-resolution magnetos- tratigraphy from the basin center. The results show that the observed magnetic polarity zones from the various sections at different sites in the basin exhibit similar magnetic polarity patterns which can be readily correlated, in terms of both magnetic polarity zonation and lithofacies; in addition, they show that the sedimentary se- quence of the basin was sub-continuously deposited from ~54 Ma to 4.8 Ma. The magnetostratigraphic corre- lations confirm previous constraint of the Xiejia fauna in the late Oligocene at ~25 Ma, challenging thecurrent Chinese mammal land zonation for the early Miocene, and we suggest that it provides a superior record of eolian dust deposition and river incision in the late Pliocene than previous studies. There is a close match of the climatic proxy records of the Xiejia section, dated by magnetostratigraphy, with the global climatic record which cor- roborates the paleomagnetic correlations. The evolution of the sedimentary environment provided by the li- thofacies demonstrates a complete cycle of basin formation and termination, which records the eastern Qilian Shan experienced three main phases of uplifts: slow episodic uplifts at ~54 Ma and 22.5 Ma and a late rapid episodic uplifts at 8–7 Ma and since 4.8–3.6 Ma. This tectonic uplift in the NE Tibetan Plateau was mostly nearly synchronous responses to the initial and continuing collision of India and Asia since ~50 ± 5 Ma. 1. Introduction et al., 1996a,b; Li and Fang, 1999)(Fig. 1). It is especially important in relation to the standard Chinese land mammal zones (CLMZ) of the The Xining Basin (XB) lies in a critical transition zone, in terms of early Miocene Xiejian Stage (equivalent to the Aquitanian Stage of the both tectonics and landforms, between the NE Tibetan Plateau and the European marine fossil zones or the Agenian Stage (MN 1–3) of the Loess Plateau, and in climatic terms between the Asian monsoon- European land mammal zones (ELMZ)) (Li and Qiu, 1980; Li et al., dominated region and the dry, westerly-influenced Asian interior (Li 1981, 1984; Qiu et al., 1981; Qiu and Qiu, 1990; Deng et al., 2006). It ⁎ Corresponding author at: CAS Center for Excellence in Tibetan Plateau Earth Sciences and Key Laboratory of Continental Collision and Plateau Uplift, Institute of Tibetan Plateau Research, Chinese Academy of Sciences, Beijing 100101, China E-mail address: [email protected] (X. Fang). https://doi.org/10.1016/j.earscirev.2019.01.021 Received 1 September 2017; Received in revised form 17 January 2019; Accepted 23 January 2019 Available online 25 January 2019 0012-8252/ © 2019 Elsevier B.V. All rights reserved. X. Fang et al. Earth-Science Reviews 190 (2019) 460–485 Fig. 1. (a)DEM image showing the location of the Xining Basin with respect to the geomorphologic and tectonic framework of the NE Tibetan Plateau. (b) Distribution of the Cenozoic stratigraphy of the Xining Basin and locations of the sections referenced in the text (modified from Dai et al., 2006). GJS: Guanjiashan; TS: Tashan and drilling site; 1: Xiejia section; 2: Tashan section; 3: East Xining-Shuiwan-Guanjiashan section; 4: Mojiazhuang section; 5: Bingling Shan section; 6: Yagou section; HW: Houwan section; CJB: Caijiabao section; DDL: Dadunling loess section. 461 X. Fang et al. Earth-Science Reviews 190 (2019) 460–485 Fig. 2. Cross sections a-b and c-d showing the relationships between the Cenozoic stratigraphy and tectonics. c-c′ indicates the East Xining-Shuiwan-Guanjiashan composite sections with its extension upward to the Houwan and Caijiabao sections for the top sequences. Topographic surface outlines are taken from DEM topographic data and 1:50,000 topographic maps. See Fig. 1 for the locations of cross-sections. Numbers in circles indicate the mammalian fauna listed in Table 1. develops the continuous sequence of predominantly fine-grained sedi- great potential for providing high resolution paleoclimatic records ments spanning the early Eocene to the Pliocene (QBGM, 1991; Dai documenting Asian aridification and monsoon evolution, the uplift of et al., 2006; Fang et al., 2015; Yang et al., 2017)(Fig. 2). Thus, it has NE Tibet and the origin and incision of the Yellow River (Li et al., 462 X. Fang et al. Earth-Science Reviews 190 (2019) 460–485 1996a,b; Lu et al., 2004; Dupont-Nivet et al., 2007; Lin et al., 2001; tectonosedimentary and geomorphologic (river incision) framework of Licht et al., 2014; Fang et al., 2015; Nie et al., 2015). The sequences are the XB. We hope that this work will provide the basis for future studies especially important for studying the time interval from the Oligocene of the deformation and uplift of the NE Tibetan Plateau and will help to the early Miocene, which marks a critical transition in both climatic unravel the paleontological and environmental evolution of the region, change and tectonomorphological evolution on both regional and as well as the record of Asian aridification and monsoonal climate global scales, and marked the shift from a greenhouse to an icehouse change provided by the unusually continuous, fine-grained sedimentary Earth (Zachos et al., 2008). The interval is also important in terms of sequence. changes in global planetary wind systems and regional monsoons in Asia (Liu et al., 1998; Sun and Wang, 2005; Guo et al., 2008), as well as 2. Geographic and geologic setting for crustal thickening, extrusion and the growth and uplift of the Ti- betan Plateau, and the associated large-scale reorganization of fluvial The XB is in the eastern extension of the Qilian Shan (Mts.) at the systems (Tapponnier et al., 2001; Molnar, 2005; Zheng et al., 2013). northeastern corner of the Tibetan Plateau (Fig. 1). Its dimensions are However, intense tectonic deformation and broad uplift have also given about 100 × 80 km and the basin surface elevations are mainly be- risen to widespread erosion and development of unconformities in the tween about 2000 and 3000 m. It is confined by the Daban Shan (Mts.), Oligocene-to-early Miocene stratigraphy in Asia. These themes high- Laji Shan (Mts.) and Riyue Shan (Mts.) to the north, south and west, light the importance of the continuous Oligocene-to-Pliocene fine- respectively, while the eastern side is open to the Minhe Basin (Fig. 1b). grained sedimentary record of the Xining Basin as an archive of in- The Huang Shui (River), a tributary of the Huang He (Yellow River), formation on paleontological, climatic and tectonic evolution, which is originates in the Riyue Shan and Daban Shan and flows from west to reflected by increasing regional and global research attention (e.g., Li east, incising the basin center. Up to 16 terraces have developed as a et al., 1996a,b; Horton et al., 2004; Lu et al., 2004, 2007; Dai et al., result, upon which thick (up to 200 m) eolian loess was deposited (Li 2006; Deng et al., 2006; Dupont-Nivet et al., 2007, 2008a,b; Xiao et al., et al., 1996a,b; Lu et al., 2004, 2007; Zhang et al., 2017)(Figs. 1 and 2). 2010, 2012; Abels et al., 2011; Long et al., 2011; Hoorn et al., 2012; Chi Climatically, the XB is now dominated by an arid/semiarid con- et al., 2013; Licht et al., 2014, 2016; Zhang and Guo, 2014; Fang et al., tinental climate with mean annual temperature (MAT) of 5–6 °C and 2015; Zan et al., 2015; Han et al., 2015; Zhang et al., 2017; Yang et al., mean annual precipitation (MAP) of 350–500 mm. Rainfall is mainly 2017). from June to August, following a typical monsoon pattern. The Xiejia (XJ) fauna was initially discovered in the XB (Li and Qiu, The collision of the Qaidam Block and minor Qilian Blocks with the 1980; Li et al., 1981; Qiu et al., 1981) and was later classified as the North China Block during the Caledonian Orogeny terminated the standard Chinese land mammal stage of the early Miocene (Li et al., Qilian Ocean and initiated the Paleozoic Qilian orogen, forming the 1984; Qiu and Qiu, 1990; Deng et al., 2006).
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