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Sedimentary and Palaeoenvironmental Evolution of the Junggar Basin, Xinjiang, Northwest China

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Sedimentary and Palaeoenvironmental Evolution of the Junggar Basin, Xinjiang, Northwest China Palaeobio Palaeoenv (2010) 90:175–186 DOI 10.1007/s12549-010-0038-9 REVIEW Sedimentary and palaeoenvironmental evolution of the Junggar Basin, Xinjiang, Northwest China Weihua Bian & Jens Hornung & Zhenhua Liu & Pujun Wang & Matthias Hinderer Received: 31 March 2010 /Revised: 24 May 2010 /Accepted: 5 July 2010 /Published online: 8 August 2010 # Senckenberg, Gesellschaft für Naturforschung and Springer 2010 Abstract This review paper summarizes the sedimentary first cycle in the Permian and Triassic is characterized by and palaeoenvironmental evolution of the Junggar Basin an Early Permian extensional strike-slip and a Late in Northwest China largely based on hardly accessible Permian to Triassic compressional foreland setting. After Chinese language papers, and complemented by own an Early Permian marine regression, persistent nonmarine field observations and a critical survey of key sediment fluvio-lacustrine conditions were established containing cores from petroleum wells. We have combined this probably the thickest organic-rich mudstone interval in information and updated existing lithofacies and isopach the world, which act as major source rocks of the basin. maps for characteristic time slices of basin evolution and Starting with four depocenters, the basin was unified palaeoenvironmental change. The Junggar Basin was during the Triassic. The preserved total maximum initiated during the late stage of collisional tectonics in thickness of this cycle is about 8,500 m in the southern the southern Central Asian Orogenic Belt (Altaids) since depocenter. During the second intracontinental depres- the Early Permian. According to studies in surrounding sion cycle, subsidence slowed down and the depocenter mountain chains and geophysical surveys, the basement migrated towards the basin center reaching a maximum consists of a collage of oceanic basins, intraoceanic thickness of 6,000 m. The palaeoenvironment was island arcs, and microcontinents of Precambrian to dominated by a large oscillating freshwater lake receiv- Palaeozoic age. The basin fill is subdivided into three ing changing quantities of clastic sediments from the tectonically controlled stratigraphic sequences which are surrounding mountain ranges and forming alluvial fans, separated by two regional angular unconformities. The braid plains, and deltas partly containing coal seams of economic interest. Sedimentary facies, pollen, and palae- This article is a contribution to the special issue “Triassic-Jurassic obotanical plant fossils show an overall aridization trend biodiversity, ecosystems, and climate in the Junggar Basin, Xinjiang, and a shrinking lake cover. During the Neogene cycle, ” Northwest China the depocenter migrated back to the south and the former : : W.-H.W. Bian BianJ.Á HornungJ. HornungM.Á HindererM. Hinderer (*) (*) asymmetric foreland basin was reactivated due to Institut für Angewandte Geowissenschaften, thrusting and rapid uplift of the Tian Shan. The Technische Universität Darmstadt, maximum thickness of these molasse-type deposits Schnittspahnstraße 9, Darmstadt 64287, Germany exceeds 5,000 m. Despite its strong potential, there is e-mail: [email protected] still a lack of high resolution bio- and cyclostratigraphy, sequence stratigraphy, and palaeoclimate studies in the W.W.-H. Bian Bian: P.Á WangP.-J. Wang College of Earth Sciences, Jilin University, Junggar Basin to elucidate local versus regional palaeo- 2199 Jianshe Street, environmental patterns and to better constrain far- Changchun 130061, China distance tectonic forcing. Z.Z.-H. Liu Liu Keywords Central Asian Orogenic Belt (CAOB) . Junggar Northwest Branch, Research Institute of Petroleum Exploration and Development (RIPED), Basin . Lake sediments . Lithofacies . Palaeoenvironment . PetroChina, China Basin evolution 176 Palaeobio Palaeoenv (2010) 90:175–186 Introduction terms have been proposed to describe the specific nature of the basin such as "broken foreland basin" (Dickinson The Junggar Basin in the Xinjiang Uygur Autonomous and Snyder 1978), "collisional successor basin" (Graham Region of Northwest China is one of the most prominent et al. 1993), and "walled sedimentary basin" (Carroll et al. walled sedimentary basins in western China, surrounded 2010). The latter emphasizes the long-lasting closed by active mountain ranges but with little internal geomorphology of this basin type with internal drainage deformation and an exceptionally long history of subsi- caused by dominantly contractional intraplate deformation dence and impoundment of sediments (Carroll et al. and being an integral part of the growth of the Asian 2010). These basins developed since the Late Palaeozoic continent since the Permian. Aridity appears to be a after amalgamation of microcontinents, ocean basins, and necessary condition to defeat orogen-traversing rivers island arcs forming the Altaid orogenic belt, also called the (Sobel et al. 2003). Central Asian Orogenic Belt (CAOB) which represents the Temporal and spatial discrete information on the largest crustal growth in Palaeozoic time (Sengör et al. sedimentary record of the Junggar Basin is mainly based 1993). The sedimentary fill is nonmarine and dominated by on outcrop belts within and in front of the surrounding fluvio-lacustrine sandstones and mudstones. Most basins mountain ranges that dominantly expose sedimentary facies were repeatedly covered by large lakes and house substan- proximal to the source areas (Hendrix et al. 1992; Fang et tial economic resources of coal, oil shale, petroleum, and al. 2006; Metcalfe et al. 2009; Hornung and Hinderer evaporite minerals (Zhao et al. 2010). In addition, they 2010). The Permian is characterized by a gradual transition preserve important palaeobiological and continental palae- from deep marine to nonmarine depositional environments. oclimate records. This includes the possibly thickest organic-rich mudstone The Junggar Basin has a total area of 136,000 km2 and is interval in the world approaching 2,000 m and being the presently surrounded by the Zaire Mountains and Halalate major source rocks of the basin (Lawrence 1990; Carroll et Mountains to the west, the Qingelid Mountains and al. 1992). Through the Mesozoic up to the Palaeogene, Karamaili Mountains to the northeast, and the east–west large fluvio-lacustrine deposystems persisted over the trending Boro Horo Mountains (Tian Shan) and Bogda whole basin; however, several episodes of enhanced Mountains to the south (Fig. 1a). The triangle-shaped basin sediment input and changes in humidity and seasonality can be subdivided into four geological units from the north led to strong shift of lateral facies and second to fourth to south namely the Wulungu Depression, Luliang Uplift, order vertical cyclicity (Hendrix et al. 1992; Zhao et al. Central Depression and Piedmont Depression north of the 2010; Fig. 1c). In the Neogene, the southern part of the Tian Shan Mountains (Fig. 1a). The maximum thickness of Junggar Basin experienced rapid subsidence and strong the basin fill since the Permian reaches 14,000 m in the sediment supply by the rising Tian Shan converting the south (Tang et al. 1997). basin into the present asymmetric foreland basin dominated The juvenile Junggar Basin formed at the end of the by coarse-grained molasse deposition (Chen et al. 2002; Carboniferous after final collision of the combined Zhang et al. 1999a; Fig. 1b). Tarim–central Tian Shan Block with the northern Tian The aim of our paper is to complement recent large-scale Shan Block by post-collisional transcurrent tectonics reviews about the Late Palaezoic to Cenozoic tectonic during the Early and Middle Permian and flexural evolution and basin formation of northern China (Xiao et foreland subsidence in the Late Permian when subduc- al. 2009; Carroll et al. 2010) by a review of extensive data tion terminated (Chen et al. 2002; Kuang and Qi 2006; from petroleum exploration within the Junggar Basin, that Wang et al. 2009; Xiao et al. 2009). During the Mesozoic– are documented only in relatively inaccessible Chinese Cenozoic, the Junggar Basin impounded sediments almost language publications or internal reports, and compare the continuously in an intracontinental setting. The basin results with the international literature. Benefiting from margins, however, have been repeatedly deformed in geophysical exploration and petroleum drillings, more and response to successive accretion onto the south Asian more information about the sedimentary accumulation and margin (Hendrix et al. 1992; Carroll et al. 1995). Since basin evolution was obtained (e.g. Chen et al. 2002;Heet Neogene, the Junggar Basin was reactivated as a foreland al. 2005; Luo et al. 2006; Song 2006; Zou et al. 2007; Feng basin due to the collision of the Indian plate with the et al. 2008; Kang 2008; Liu et al. 2008; Qu et al. 2008; Zhu Eurasian plate (Hendrix et al. 1994;Guoetal.2006;Luo et al. 2008; Wu et al. 2009). In particular, we collected well et al. 2006;DeGraveetal.2007). This multiphase basin information from the Xinjiang Oilfield Company including history and its intraplate position make it difficult to cast cutting logs of 150 wells and a stratigraphic framework of the Junggar Basin (and other nonmarine basins across 520 wells and revised existing facies maps. Detailed studies China) into traditional classification schemes that empha- on key wells acted as a control of these generalized facies size plate–boundary interactions. Therefore, different maps and helped to better interpret palaeoenvironments.
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