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Late Cretaceous (Campanian) Provenance Change in the Songliao Basin, NE China: Evidence from Detrital Zircon U–Pb Ages from the Yaojia and Nenjiang Formations

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Late Cretaceous (Campanian) Provenance Change in the Songliao Basin, NE China: Evidence from Detrital Zircon U–Pb Ages from the Yaojia and Nenjiang Formations Palaeogeography, Palaeoclimatology, Palaeoecology 385 (2013) 83–94 Contents lists available at SciVerse ScienceDirect Palaeogeography, Palaeoclimatology, Palaeoecology journal homepage: www.elsevier.com/locate/palaeo Late Cretaceous (Campanian) provenance change in the Songliao Basin, NE China: Evidence from detrital zircon U–Pb ages from the Yaojia and Nenjiang Formations Bin Zhao a,b, Chengshan Wang a,b,⁎, Xiaofu Wang c, Zhiqiang Feng d a School of Earth Science and Resources, China University of Geosciences, Beijing 100083, China b State Key Laboratory of Biogeology and Environmental Geology, China University of Geosciences, Beijing 100083, China c Sinopec International Petroleum Exploration and Production Corporation, Beijing, 100029, China d Institute of Exploration and Development of Daqing Oil field Company Ltd, Daqing, 163712, China article info abstract Article history: In order to define the provenance change across the nonconformable boundary between the second and the Received 28 September 2011 third members of the Upper Cretaceous Nenjiang Formation (Campanian) in the north-central area of the Received in revised form 16 February 2012 Songliao Basin, two sandstone samples above (sample a-1 from the fourth member of the Nenjiang) and Accepted 10 March 2012 below (sample z-1 from the first member of the Yaojia Formation) the nonconformity were collected from Available online 18 March 2012 core holes. U–Pb dating was performed on detrital zircons separated from the three sandstone samples. De- trital zircons from sample a-1 have dominant age populations of 100–110 Ma, 190–220 Ma, and ~1800 Ma, Keywords: – Songliao Basin and sample z-1 has dominant ages of 130 150 Ma and ~350 Ma. This paper demonstrates that the prove- Late Cretaceous nance of the fourth member of the Nenjiang Formation is significantly different from the first member of Detrital zircon U–Pb ages the Coniacian Yaojia Formation. The provenance above the nonconformity became much more complex Provenance analysis and the eastern source increased significantly, while the western source sharply declined. The main source Tectonic inversion areas of the fourth member of the Nenjiang Formation are mainly the Zhangguangcai Range, the eastern Less- er Xiang'an Range and the southeast of Songliao Basin. The dominant provenance of the first member of the Yaojia Formation is the northern, the central and the southern Great Xing'an Range. According to the depo- sitional ages and combining the latest seismic stratigraphic profiles in the Songliao Basin, the tectonic inver- sion of the eastern Songliao Basin began between 73 Ma and 87 Ma, which differs from the previous age of 73 Ma. © 2012 Elsevier B.V. All rights reserved. 1. Introduction source area can be defined (Bruguier and Lancelet, 1997; Carter and Steve, 1999). Detrital zircons are able to withstand the effects of weathering, The Songliao Basin is located in northeastern China (119°40′– erosion, abrasion, and thermal alteration, can survive multiple epi- 128°24′E, 42°25′–49°23′N), approximately 750 km in length, 330– sodes of transportation, and possess an inherently stable U–Pb isoto- 370 km wide, with a total area of 260,000 km2. It is a large diamond pic system (Bruguier and Lancelet, 1997; Lee et al., 1997; Cherniak shaped, NNE to SSW trending Meso-Cenozoic sedimentary basin, and Watson, 2000; Kosler and Sylvester, 2003). Study shows that formed on a folded basement (Fig. 1). zircons in basin detrital sediments track the background and the Study suggests that the boundary between the second and third character of the provenance, and also obtain the inner link between members of the Nenjiang Formation (Campanian) of the Songliao the basin subsidence and thermal tectonic events (Carter and Steve, Basin is unconformable. High resolution 3D seismic profiles show that 1999; Fedo et al., 2003; Griffin et al., 2004; Moecher and Samson, it is an angular unconformity (Feng et al., 2010; seismic boundary T06, 2006; Kelty et al., 2008). The detrital sediments come from different Figs. 2, 3). In addition, sediments of member three prograded from provenances and different ages, so zircons deposited in the basin east to west into the centre of the Sangliao Basin (Fig. 2-b) suggesting might have several peak ages. Although rocks of the same ages may an eastern provenance supply to the eastern Songliao Basin. In contrast be present in different areas around the basin, which may make this sediments of the older member two were sourced from the western approach unfeasible, detrital zircons are clues to the exposed geolog- margin. This change is extremely important for it may relate to the ical setting and tectonic evolution around the basin, and the sediment tectonic inversion of the Songliao Basin in Late Cretaceous, which was driven by subduction of the Pacific plate beneath the Eurasian plate (Gao and Cai, 1997; Feng et al., 2010). ⁎ Corresponding author at: School of Earth Science and Resources, China University of Geosciences, Beijing 100083, China. Tel.: +86 10 82321612; fax: +86 10 82322171. Geophysical and sedimentary geological evidence demonstrate the E-mail address: [email protected] (C. Wang). tectonic inversion and the Late Cretaceous provenance of the Songliao 0031-0182/$ – see front matter © 2012 Elsevier B.V. All rights reserved. doi:10.1016/j.palaeo.2012.03.017 84 B. Zhao et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 385 (2013) 83–94 Fig. 1. Geologic and tectonic sketch map of the Songliao Basin region, modified after Zhou et al. (2009a) and Meng et al. (2010). 1. Xra Moron–Changchun suture zone; 2. Jiayin– Mudanjiang suture zone; 3. Nenjiang–Kailu Fault; 4. Dunhua–Mishan Fault; 5. Yitong–Yilan Fault; 6. Xiguitu–Tayuan Fault; 7. Mongolia–Okhotsk suture zone; 8. Hegenshan–Heihe suture zone. The Central Asian Orogenic Belt (CAOB) is between the North China Craton (NCC) and the Siberian Craton (SC). AA′ is the location of the seismic profile (Fig. 2). A1. The northern Great Xing'an Range. A2. The central Great Xing'an Range. A3. The sourthern Great Xing'an Range. B. The Lesser Xing'an Range. C. The Jiamusi Massif. D. The Zhangguangcai Range. Basin (Gao and Cai, 1997; Himeno et al., 2001; Chen et al., 2009a,b; Feng mineral assemblages (Peng et al., 2010). However the change in the et al., 2010; Peng et al., 2010). The provenance direction has been deter- provenance direction and the source areas above and below the non- mined by the distribution and morphology of the delta and the deposi- conformity has yet to be defined precisely. This paper builds upon the tional facies of the sedimentary strata (Feng et al., 2010) and by heavy previous research and focuses on the tectonic inversion of the Songliao Fig. 2. Uninterpreted (a) and interpreted (b) seismic profile modified after Feng et al. (2010) showing the T06 nonconformity and the progradation of the Nenjiang Formation from east to west across the centre of the Sangliao Basin. B. Zhao et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 385 (2013) 83–94 85 Fig. 3. Upper Cretaceous stratigraphic correlation chart of the Songliao Basin (Huang et al., 1999; Wang et al., 2009). The International Stratigraphic Chart is according to Gradstein et al. (2004). Basin, with attention on detrital zircon geochronology and its prove- al., 1999; Xie, 2000; Wu et al., 2007a)(Fig. 1). The Songnen Massif con- nance implications. Also it explores tectonic controls and processes sists of the Songliao Basin in the central part, the southern Great Xing'an between the Pacific plate and Eurasian plate during that period. Range in the west, the Lesser Xing'an Range in the northeast and the Zhangguangcai Range in the east (Wu et al., 2011). The Great Xing'an 2. Geological setting Range located in the eastern Xing'an Massif and the western Songnen Massif,extendinginanNNEdirection(Fig. 1). The Hegenshan–Heihe The Songliao Basin is surrounded by several continental massifs that fault was the boundary between the Songnen Massif and the Xing'an have complex geological histories. These are the Erguna Massif, the Massif. The Songnen Massif and lesser Xing'an–Zhangguangcai Range Xing'an Massif, the Songnen Massif, the Jiamusi Massif, with each being are separated from the Jiamusi Massif by the Jiayin–Mudanjiang Fault separated by a major fault (Ye and Zhang, 1994; Ye et al., 1994; Li et (Li and Ouyang, 1998; Li et al., 2006; Wu et al., 2004, 2007a).The Erguna Fig. 4. Cathodoluminescence images of selected zircons from Upper Cretaceous strata in the Songliao Basin. Circles indicate analytical sites. Numbers indicate the U–Pb age (206Pb/ 238U age (b1000 Ma) or 207Pb/206Pb age (>1000 Ma)) and analytical spot number. Scale bar is 100 μm. 86 B. Zhao et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 385 (2013) 83–94 Table 1 LA-ICP-MS U–Pb dating results of detrital zircons. Spots Element (ppm) Th/U Corrected Isotopic ratios Corrected Age (Ma) Th U 207Pb/206Pb 1σ 207Pb/235U1σ 206Pb/238U1σ 207Pb/206Pb 1σ 207Pb/235U1σ 206Pb/238U1σ a-101 102.82 194.92 0.5275 0.1150 0.0017 5.7391 0.0908 0.3606 0.0032 1880 16 1937 14 1985 15 a-102 156.28 297.54 0.5252 0.0546 0.0019 0.2289 0.0080 0.0306 0.0004 398 56 209 7 194 2 a-103 220.94 233.80 0.9450 0.0545 0.0020 0.2918 0.0103 0.0393 0.0005 391 55 260 8 249 3 a-104 109.96 345.56 0.3182 0.0534 0.0020 0.2256 0.0084 0.0307 0.0003 347 65 207 7 195 2 a-105 77.99 267.80 0.2912 0.1197 0.0010 6.0856 0.0780 0.3667 0.0037 1952 11 1988 11 2014 17 a-106 212.13 1060.81 0.2000 0.1169 0.0007 5.5430 0.0637 0.3424 0.0038 1909 9 1907 10 1898 18 a-108 126.07 193.68
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