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

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Palaeogeography, Palaeoclimatology, Palaeoecology

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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

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 depositional ages and combining the latest seismic stratigraphic profiles in the Songliao Basin, the tectonic inversion 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

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 0.6509 0.0519 0.0022 0.2508 0.0111 0.0350 0.0005 279 73 227 9 222 3 a-109 269.95 472.44 0.5714 0.0503 0.0046 0.1879 0.0163 0.0271 0.0007 208 207 175 14 172 5 a-110 527.50 347.94 1.5161 0.0525 0.0020 0.2622 0.0100 0.0365 0.0005 307 63 236 8 231 3 a-111 175.72 212.10 0.8285 0.0514 0.0020 0.2925 0.0113 0.0417 0.0006 258 62 260 9 264 4 a-112 81.84 103.83 0.7883 0.0574 0.0041 0.3755 0.0289 0.0476 0.0008 506 139 324 21 300 5 a-113 256.61 834.76 0.3074 0.1552 0.0020 9.5536 0.1592 0.4479 0.0072 2404 13 2393 15 2386 32 a-114 99.82 204.38 0.4884 0.0533 0.0042 0.1228 0.0092 0.0171 0.0005 340 114 118 8 109 3 a-116 264.67 392.76 0.6739 0.0461 0.0050 0.0936 0.0100 0.0147 0.0003 345 164 91 9 94 2 a-117 649.98 1191.06 0.5457 0.0536 0.0013 0.2890 0.0078 0.0397 0.0009 353 27 258 6 251 6 a-118 42.57 50.31 0.8461 0.1148 0.0027 5.8859 0.1517 0.3774 0.0080 1876 21 1959 22 2064 38 a-119 35.96 110.47 0.3255 0.1124 0.0027 5.5982 0.1258 0.3670 0.0070 1838 18 1916 19 2015 33 a-120 227.25 457.17 0.4971 0.0513 0.0018 0.2281 0.0079 0.0329 0.0007 254 41 209 7 208 5 a-121 231.83 289.95 0.7996 0.0508 0.0020 0.2206 0.0086 0.0320 0.0007 233 52 202 7 203 4 a-122 283.74 600.41 0.4726 0.0484 0.0019 0.0890 0.0035 0.0135 0.0002 119 60 87 3 86 1 a-123 280.06 570.28 0.4911 0.0519 0.0012 0.2922 0.0070 0.0409 0.0006 281 30 260 5 259 4 a-125 138.71 163.64 0.8476 0.0549 0.0023 0.2959 0.0119 0.0397 0.0006 409 62 263 9 251 4 a-127 50.92 106.54 0.4779 0.0556 0.0025 0.3710 0.0163 0.0485 0.0007 436 74 320 12 305 4 a-128 118.12 225.71 0.5233 0.1712 0.0021 11.6152 0.2376 0.4877 0.0074 2569 16 2574 19 2561 32 a-129 130.40 306.40 0.4256 0.0512 0.0018 0.2679 0.0089 0.0381 0.0004 250 56 241 7 241 3 a-130 746.22 1309.42 0.5699 0.0496 0.0017 0.0879 0.0030 0.0129 0.0002 177 54 86 3 82 1 a-133 43.60 103.25 0.4223 0.0503 0.0030 0.3041 0.0178 0.0444 0.0006 209 109 270 14 280 4 a-134 384.02 428.75 0.8957 0.0451 0.0021 0.0866 0.0039 0.0141 0.0002 183 72 84 4 90 1 a-135 68.30 130.11 0.5250 0.0533 0.0028 0.2272 0.0111 0.0318 0.0005 340 82 208 9 202 3 a-136 99.89 152.62 0.6545 0.0536 0.0027 0.2473 0.0122 0.0340 0.0005 354 88 224 10 216 3 a-137 37.04 77.22 0.4797 0.0487 0.0026 0.3143 0.0186 0.0463 0.0008 132 103 277 14 292 5 a-138 294.56 514.47 0.5725 0.1302 0.0014 7.0234 0.0961 0.3898 0.0035 2101 12 2114 12 2122 16 a-139 41.37 83.59 0.4949 0.0544 0.0036 0.3984 0.0382 0.0493 0.0010 387 181 341 28 310 6 a-141 122.34 184.62 0.6627 0.0464 0.0122 0.1091 0.0287 0.0171 0.0003 19 431 105 26 109 2 a-143 249.81 391.57 0.6380 0.0465 0.0045 0.2290 0.0217 0.0357 0.0006 24 208 209 18 226 3 a-144 322.61 633.39 0.5093 0.0477 0.0013 0.1983 0.0050 0.0301 0.0002 86 45 184 4 191 1 a-145 116.30 217.99 0.5335 0.0511 0.0021 0.2283 0.0089 0.0327 0.0004 243 70 209 7 207 2 a-146 124.73 213.22 0.5850 0.0547 0.0033 0.2615 0.0155 0.0346 0.0006 400 104 236 12 219 3 a-147 60.33 80.80 0.7468 0.0542 0.0029 0.4669 0.0253 0.0627 0.0007 378 102 389 18 392 4 a-148 95.03 177.05 0.5367 0.0553 0.0034 0.2312 0.0150 0.0303 0.0005 425 113 211 12 192 3 a-149 172.87 470.90 0.3671 0.0504 0.0016 0.2152 0.0068 0.0310 0.0003 213 55 198 6 197 2 a-150 269.34 380.20 0.7084 0.0516 0.0017 0.2951 0.0093 0.0416 0.0004 269 54 263 7 262 3 a-151 106.73 237.20 0.4500 0.0535 0.0032 0.1110 0.0066 0.0153 0.0002 350 108 107 6 98 1 a-152 189.47 255.38 0.7419 0.0532 0.0040 0.0910 0.0068 0.0125 0.0002 335 137 88 6 80 1 a-153 77.07 211.83 0.3638 0.0567 0.0019 0.5507 0.0187 0.0707 0.0011 479 49 445 12 440 6 a-154 158.48 314.50 0.5039 0.1108 0.0012 5.1297 0.0766 0.3346 0.0043 1813 12 1841 13 1861 21 a-155 435.38 594.50 0.7323 0.0492 0.0019 0.1046 0.0043 0.0155 0.0002 155 72 101 4 99 1 a-157 100.89 231.99 0.4349 0.0452 0.0026 0.1151 0.0062 0.0189 0.0003 1813 80 111 6 120 2 a-158 160.74 206.46 0.7786 0.0462 0.0031 0.2088 0.0146 0.0336 0.0008 1866 110 193 12 213 5 a-159 147.64 193.94 0.7613 0.0485 0.0022 0.2753 0.0136 0.0413 0.0008 125 77 247 11 261 5 a-160 263.71 586.85 0.4494 0.1141 0.0024 5.4263 0.1453 0.3475 0.0075 1866 22 1889 23 1922 36 a-161 134.93 250.37 0.5389 0.0524 0.0038 0.1146 0.0088 0.0161 0.0005 301 115 110 8 103 3 a-162 331.42 701.46 0.4725 0.0530 0.0016 0.2195 0.0078 0.0303 0.0008 331 38 202 7 192 5 a-163 281.61 624.29 0.4511 0.0574 0.0013 0.6393 0.0152 0.0817 0.0017 507 23 502 9 506 10 a-164 51.80 47.13 1.0990 0.0469 0.0076 0.1477 0.0236 0.0228 0.0006 45 294 140 21 146 4 a-165 223.89 181.76 1.2318 0.0560 0.0030 0.2411 0.0130 0.0316 0.0007 453 80 219 11 201 4 a-166 216.41 309.75 0.6986 0.1119 0.0014 5.1544 0.0705 0.3350 0.0046 1830 11 1845 12 1863 22 a-167 73.47 508.96 0.1443 0.1331 0.0040 6.9267 0.1742 0.3776 0.0061 2139 54 2102 22 2065 29 a-168 886.12 921.79 0.9613 0.0480 0.0012 0.0878 0.0023 0.0131 0.0001 100 42 85 2 84.1 0.8 a-169 228.31 214.91 1.0624 0.0509 0.0013 0.3106 0.0083 0.0441 0.0005 238 40 275 6 278 3 a-170 1100.02 1031.12 1.0668 0.0494 0.0011 0.1010 0.0023 0.0147 0.0002 169 30 98 2 94 1 a-171 219.53 259.34 0.8465 0.0494 0.0017 0.2524 0.0090 0.0368 0.0005 166 59 229 7 233 3 a-173 201.18 152.70 1.3174 0.0484 0.0017 0.2535 0.0098 0.0377 0.0005 121 67 229 8 239 3 a-175 173.72 266.82 0.6511 0.1387 0.0026 7.1414 0.1102 0.3734 0.0042 2211 34 2129 14 2045 19 a-176 744.17 435.89 1.7073 0.0494 0.0011 0.1909 0.0041 0.0280 0.0002 166 35 177 3 178 1 a-177 738.44 622.25 1.1867 0.0461 0.0023 0.0921 0.0046 0.0145 0.0002 509 110 89 4 93 1 a-178 146.92 370.99 0.3960 0.0484 0.0017 0.1088 0.0045 0.0162 0.0004 120 50 105 4 103 3 a-180 484.75 354.13 1.3688 0.0505 0.0028 0.0869 0.0052 0.0124 0.0002 217 107 85 5 80 1 z-101 613.22 281.64 2.1773 0.0487 0.0015 0.1429 0.0045 0.0213 0.0002 133 55 136 4 136 1 z-102 402.74 454.37 0.8864 0.0507 0.0014 0.1541 0.0044 0.0220 0.0003 226 44 146 4 140 2 z-103 343.24 189.19 1.8142 0.0484 0.0018 0.1543 0.0056 0.0234 0.0003 121 63 146 5 149 2 z-104 103.76 171.32 0.6056 0.0494 0.0030 0.1541 0.0096 0.0227 0.0003 165 115 146 8 145 2 z-105 845.57 673.12 1.2562 0.0500 0.0009 0.2010 0.0039 0.0291 0.0003 194 27 186 3 185 2 z-106 365.88 374.45 0.9771 0.0580 0.0024 0.4482 0.0199 0.0568 0.0010 530 66 376 14 356 6 B. Zhao et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 385 (2013) 83–94 87

Table 1 (continued) 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

z-107 632.07 238.79 2.6469 0.0554 0.0021 0.3718 0.0153 0.0485 0.0007 428 66 321 11 305 4 z-108 832.67 992.53 0.8389 0.0544 0.0012 0.3727 0.0142 0.0521 0.0025 388 50 322 10 327 15 z-109 1267.30 500.17 2.5337 0.0494 0.0012 0.1607 0.0040 0.0236 0.0002 165 40 151 3 150 1 z-111 646.28 577.87 1.1184 0.0554 0.0010 0.3945 0.0071 0.0515 0.0005 427 24 338 5 324 3 z-112 620.67 611.16 1.0156 0.0540 0.0010 0.4091 0.0073 0.0549 0.0006 369 23 348 5 345 3 z-113 408.70 157.60 2.5933 0.0513 0.0021 0.1860 0.0073 0.0265 0.0003 255 72 173 6 168 2 z-114 307.60 195.95 1.5698 0.0492 0.0031 0.1452 0.0091 0.0215 0.0005 157 103 138 8 137 3 z-115 815.34 656.71 1.2415 0.0515 0.0016 0.1528 0.0050 0.0214 0.0003 265 54 144 4 136 2 z-116 673.08 281.67 2.3896 0.0500 0.0014 0.1797 0.0050 0.0260 0.0002 197 48 168 4 165 1 z-117 1252.92 626.37 2.0003 0.0491 0.0011 0.1958 0.0047 0.0287 0.0003 153 35 182 4 183 2 z-118 702.70 314.76 2.2325 0.0515 0.0031 0.1325 0.0072 0.0188 0.0005 265 75 126 6 120 3 z-119 731.83 752.31 0.9728 0.0529 0.0012 0.1643 0.0041 0.0225 0.0002 325 39 154 4 143 1 z-121 1468.67 910.94 1.6123 0.0491 0.0010 0.1574 0.0032 0.0233 0.0003 153 26 148 3 149 2 z-122 1326.50 568.24 2.3344 0.0505 0.0011 0.1564 0.0035 0.0225 0.0003 218 29 148 3 144 2 z-124 1210.04 892.01 1.3565 0.0497 0.0009 0.1568 0.0028 0.0230 0.0003 182 21 148 2 147 2 z-125 338.55 471.62 0.7178 0.0520 0.0012 0.1746 0.0046 0.0244 0.0003 287 36 163 4 155 2 z-126 409.22 334.47 1.2235 0.0500 0.0013 0.1952 0.0053 0.0285 0.0004 194 40 181 5 181 2 z-127 399.39 484.15 0.8249 0.0524 0.0013 0.1751 0.0041 0.0244 0.0004 303 28 164 4 156 2 z-129 1577.68 592.38 2.6633 0.0543 0.0015 0.1731 0.0048 0.0233 0.0003 383 39 162 4 148 2 z-130 913.70 396.04 2.3071 0.0489 0.0015 0.1434 0.0047 0.0214 0.0003 142 48 136 4 137 2 z-131 1276.58 412.42 3.0953 0.0499 0.0015 0.1602 0.0049 0.0234 0.0004 189 43 151 4 149 2 z-132 731.71 449.93 1.6263 0.0504 0.0012 0.1750 0.0042 0.0252 0.0003 215 35 164 4 160 2 z-134 284.38 191.29 1.4866 0.0622 0.0038 0.1945 0.0128 0.0226 0.0003 682 120 180 11 144 2 z-135 1655.75 1028.07 1.6105 0.0510 0.0007 0.1817 0.0028 0.0258 0.0002 241 22 170 2 164 1 z-136 174.84 196.76 0.8886 0.0586 0.0030 0.4518 0.0218 0.0577 0.0015 553 61 379 15 362 9 z-137 382.09 304.77 1.2537 0.0554 0.0024 0.2841 0.0117 0.0372 0.0004 427 71 254 9 235 3 z-138 841.27 603.46 1.3941 0.0489 0.0014 0.1643 0.0053 0.0242 0.0004 142 47 154 5 154 2 z-139 1008.69 485.44 2.0779 0.0509 0.0011 0.1872 0.0044 0.0266 0.0003 237 33 174 4 169 2 z-140 792.27 558.62 1.4183 0.0496 0.0011 0.1652 0.0039 0.0241 0.0003 178 34 155 3 153 2 z-141 1079.58 227.07 4.7543 0.0516 0.0015 0.2103 0.0067 0.0296 0.0004 266 51 194 6 188 2 z-142 157.00 103.54 1.5163 0.1116 0.0013 5.2523 0.0639 0.3427 0.0033 1825 10 1861 10 1900 16 z-143 837.17 648.67 1.2906 0.0506 0.0010 0.1642 0.0035 0.0236 0.0002 221 32 154 3 150 1 z-144 390.82 256.87 1.5215 0.0487 0.0025 0.1473 0.0072 0.0221 0.0003 134 84 140 6 141 2 z-145 580.09 569.39 1.0188 0.0482 0.0010 0.1463 0.0031 0.0222 0.0002 109 33 139 3 141 1 z-146 1436.84 944.24 1.5217 0.0499 0.0011 0.2230 0.0140 0.0321 0.0014 191 74 204 12 204 8 z-147 394.41 303.14 1.3011 0.0487 0.0015 0.1522 0.0045 0.0229 0.0002 134 52 144 4 146 1 z-148 978.94 663.36 1.4757 0.0525 0.0009 0.3735 0.0067 0.0529 0.0016 309 39 322 5 332 10 z-149 370.77 254.21 1.4585 0.0522 0.0013 0.2681 0.0070 0.0376 0.0004 292 40 241 6 238 3 z-151 1154.95 734.41 1.5726 0.0505 0.0009 0.2557 0.0050 0.0368 0.0004 216 26 231 4 233 2 z-152 243.26 203.41 1.1959 0.0495 0.0034 0.1569 0.0107 0.0230 0.0003 172 157 148 9 146 2 z-153 625.90 402.63 1.5545 0.0484 0.0014 0.1271 0.0037 0.0191 0.0002 117 49 121 3 122 1 z-154 833.26 367.27 2.2688 0.0494 0.0012 0.1815 0.0046 0.0266 0.0002 166 43 169 4 169 2 z-155 511.75 530.33 0.9650 0.0556 0.0007 0.4658 0.0059 0.0609 0.0004 436 17 388 4 381 2 z-156 2428.80 1489.38 1.6307 0.0499 0.0049 0.0963 0.0095 0.0140 0.0001 189 224 93 9 89.6 0.8 z-157 369.85 182.12 2.0309 0.0478 0.0028 0.1474 0.0090 0.0225 0.0005 88 97 140 8 143 3 z-158 846.94 786.54 1.0768 0.0498 0.0010 0.1720 0.0035 0.0251 0.0002 186 30 161 3 160 1 z-159 140.03 190.71 0.7342 0.0518 0.0018 0.2252 0.0077 0.0318 0.0003 274 60 206 6 202 2 z-160 398.60 175.37 2.2729 0.0539 0.0023 0.1496 0.0064 0.0203 0.0002 365 76 142 6 130 1 z-161 951.74 614.29 1.5493 0.0505 0.0013 0.2031 0.0056 0.0290 0.0003 220 47 188 5 184 2 z-162 654.46 386.45 1.6935 0.0502 0.0014 0.1551 0.0039 0.0226 0.0002 202 43 146 3 144 1 z-163 768.73 249.30 3.0836 0.0510 0.0019 0.1429 0.0052 0.0205 0.0002 241 67 136 5 131 1 z-166 275.28 311.84 0.8828 0.0599 0.0032 0.4862 0.0258 0.0588 0.0012 598 80 402 18 368 7 z-167 1550.58 1211.14 1.2803 0.0485 0.0009 0.1545 0.0033 0.0230 0.0002 122 37 146 3 147 1 z-168 549.45 539.91 1.0177 0.0487 0.0010 0.2064 0.0045 0.0307 0.0003 133 33 191 4 195 2 z-169 593.10 361.31 1.6415 0.0504 0.0015 0.1600 0.0049 0.0230 0.0002 214 53 151 4 147 1 z-170 134.03 164.75 0.8135 0.0585 0.0013 0.7730 0.0180 0.0956 0.0009 550 34 581 10 589 5 z-171 2459.27 535.44 4.5930 0.0516 0.0020 0.1304 0.0049 0.0183 0.0002 269 67 124 4 117 1 z-172 1413.50 573.34 2.4654 0.0493 0.0015 0.1398 0.0040 0.0208 0.0002 163 46 133 4 133 1 z-173 351.77 243.50 1.4446 0.0491 0.0017 0.1498 0.0053 0.0222 0.0002 153 62 142 5 141 1 z-174 519.61 426.51 1.2183 0.0503 0.0013 0.1611 0.0045 0.0231 0.0002 210 49 152 4 147 1 z-175 1261.31 382.05 3.3014 0.0515 0.0014 0.1652 0.0045 0.0233 0.0002 265 49 155 4 148 1 z-176 523.10 397.61 1.3156 0.0514 0.0014 0.1516 0.0041 0.0214 0.0002 258 48 143 4 136.3 1 z-177 578.98 461.71 1.2540 0.0508 0.0018 0.1633 0.0053 0.0236 0.0002 229 56 154 5 150 1 z-178 398.39 204.43 1.9488 0.0497 0.0020 0.1321 0.0053 0.0193 0.0002 182 76 126 5 123 1 z-179 371.52 190.66 1.9486 0.0497 0.0019 0.1439 0.0054 0.0211 0.0002 182 68 137 5 135 1 z-180 149.68 134.16 1.1157 0.0500 0.0022 0.1941 0.0083 0.0282 0.0004 195 74 180 7 179 2

Massif, located in the northwestern part of NE China, is separated from Heilongjiang block (Zhang et al., 1998). Then in the Permian Period the Xing'an Massif by the Xiguitu–Tayuan Fault. South of the Songliao the North China Craton collided and closed with the Siberian Craton Basin is the North China Craton (NCC). (actually with the Heilongjiang block) along the line of the Xra– The Erguna–Xing'an Massif, Songnen–Zhangguangcai Massif, Muron–Changchun fault, which is called the Xra–Muron–Changchun Jiamusi–Xingkai Massif, and others collided and closed in the suture (Sun et al., 2004a,b). The North China Craton became one of Carboniferous Period, and formed the uniﬁed block called the the important sediment source areas of the south Songliao Basin 88 B. Zhao et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 385 (2013) 83–94

Fig. 5. U–Pb concordia diagrams for detrital zircon grains: sample a-1 (68 grains total) from the fourth member of the Nenjiang Formation; Sample z-1 (72 grains total) from the ﬁrst member of the Yaojia Formation, without the grain z-142 dated at 1825±10 Ma (Table 1).

(Wang et al., 2007; Zhang et al., 2009). The Songnen–Zhangguangcai collected from the fourth member of the Upper Cretaceous (Campa- Massif is separated from the Jiamusi Massif by the Mudanjiang suture nian) Nenjiang Formation in the northern part of the Songliao Basin, zone (Li and Ouyang, 1998; Wu et al., 2004, 2007b; Li et al., 2006). Stud- at the site of “Ao 405 well”, which is southeast of the Gulong Depression ies show that the Jiamusi Massif came from the low latitude area (Wilde in Qijia, at a depth of 452 m. The fourth member of the Nenjiang Forma- et al, 2000, 2001, 2003), and collided with the Asian continental margin tion consists mainly of gray-green mudstone, silty mudstone, mixed between Late Triassic and Early Jurassic (Wu et al., 2007b; Zhou et al., with gray siltstone and fine sandstone, siltstone. Sample z-1 was also 2009a,b). collected from the Songliao Basin at the site of “Zhou 804 Well” south The Songliao Basin was formed and filled in four tectonic stages: of the Sanzhao Depression. Sampling depth was 1383 m from the first mantle upwelling, syn-rift, post-rift thermal subsidence, and tectonic in- member of the Upper Cretaceous (Coniacian–Santonian) Yaojia Forma- version (Gao and Cai, 1997). The youngest tectonic inversion phase pre- tion, which consists mainly of gray, gray-green sandstone and gray viously was thought to have begun with deposition of the Sifangtai green, reddish brown, and purplish red mudstone. Formation (~73 Ma) (Zhai et al, 1993; Zhang et al, 1996; Chi et al, Zircons were separated using heavy liquids and a Frantz magnetic 2002). This phase was a response to the interaction between the Pacific separator at the Langfang Regional Geological Survey, Hebei Province, plate and the Eurasian plate in Late Cretaceous (Maruyama et al., 1997; China. Approximately 400 zircons were handpicked from each sam- Ren et al., 2002; Ren, 2004; Stepashko, 2006; Muller and Maria, 2008; ple under a binocular microscope, and mounted in epoxy resin. The Stuart and Muller, 2008). Stratigraphic units deposited in the Songliao resin discs were then polished until most of the zircon grains were Basin during the Late Cretaceous (Fig. 3) consist of the Quantou Forma- exposed at the grain centre in preparation for analysis by laser tion (K1q), the Qingshankou Formation (K2qn) (divided into three ablation-inductively coupled plasma-mass spectrometer (LA-ICP- members), the Yaojia Formation (K2y) (divided into three members), MS). The standards were mounted in a separated epoxy resin. Images the Nenjiang Formation (K2n) (divided into five members), the Sifangtai of the zircons were taken using an optical microscope in transmitted Formation (K2s), and the Mingshui Formation (K2m) (divided into two and reflected light, and the surfaces of the zircon grains were washed members) (Huang et al., 1999; Wang et al., 2009). in dilute HNO3 and pure alcohol to remove any lead contamination, and then gold was coated on the mounts (Meng et al., 2010). Catho- 3. Materials and analytical methods doluminescence (CL) images were obtained using a JEOL scanning electron microscope housed at the Chinese Academy of Geological Samples in this study were collected from the core library of Sciences, to identify internal structures and select target sites for U–Pb Daqing Petroleum Exploration and Development Institute, in Daqing, analyses. Zircons were dated using a 193 nm Elan 6100 DRC ICPMS China. We selected two samples: a-1 and z-1. Sample a-1 was housed at the State Key Laboratory of Continental Dynamics, Northwest B. Zhao et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 385 (2013) 83–94 89

Fig. 6. Age histograms of zircon U–Pb from the sample a-1 and sample z-1 (b600 Ma).

University in Xi'an, following the standard operating techniques described by Yuan et al. (2004). 207Pb/206Pb and 206Pb/238Uvalueswere calculated using the ICPMSDataCal program (Liu et al., 2009a,b), with Zircon 91500 used as an external standard (206Pb/238U age: 1065.4± 0.6 Ma; Wiedenbeck et al., 1995), and the standard silicate glass GSE- 1G used to optimize the ICPMS. The spot diameter was 35 μm, and ages were calculated using ISOPLOT 3 (Ludwig, 2003). The measurements of standard sample GJ-1 yielded a weighted mean 206Pb/238Uageof 602.2±2.4 Ma (2σ, MSWD=1.15, n=19; MSWD = mean square of – weighted deviates; Yuan et al., 2004), in good agreement with the Fig. 7. Probability plot of the U Pb ages. A1, the northern Great Xing'an Range (Wu et 206 238 – al., 2002; Miao, 2003; Miao et al., 2004; Ge et al., 2007; Sui et al., 2007, 2009; Wu et al., recommended ID-TIMS Pb/ U age of 598.5 602.7 Ma Jackson et 2011). A2, the central Great Xing'an Range (Ge et al., 2005, 2007; Wu et al., 2011). A3, al., 2004). The common-Pb correction followed the method described the southern Great Xing'an Range (Liu et al., 2005; Bao et al., 2007; Liu et al., 2009a,b; by Anderson (2002).The206Pb/238U ages are used for the grains with Wu et al., 2011). ages younger than 1000 Ma, while the 206Pb/207Pb ages are used for the grains with ages older than 1000 Ma. For statistical purposes, zircons >1000 Ma with discordance b10% and b1000 Ma with discordance b20% were considered as usable. because of their discordant ages. The remaining 68 grains gave concordant ages at the 90% conﬁdence level. The 68 ages mainly fall 4. Analytical results into three groups: 80–146 Ma (17 grains), 172–310 Ma (35 grains), and 1813–2139 Ma (10 grains). The oldest zircon age is 2569± 4.1. Sample a-1 from Nenjiang Formation (Campanian) 16 Ma and the youngest zircon grain is 80±1 Ma (Table 1 and Fig. 5).

Most grains show oscillatory growth zoning in CL images (Fig. 4); some grains are incomplete and they may have been damaged during 4.2. Sample z-1 from Yaojia Formation (Coniacian–Santonian) transport. Eighty randomly selected zircons grains were analyzed for U–Pb ages using LA-ICP-MS. Some grains are opaque because their Th Most grains show oscillatory growth zoning in CL images; some and U content are too high. Th/U values range from 0.14 to 1.71 grains are incomplete because of post-destruction (Fig. 4). Eighty ran- (Table 1), suggesting a magmatic origin (Wu et al., 2004). After domly selected zircon grains from sample z-1 were analyzed for U–Pb common-Pb corrections were made, twelve analyses were discarded ages. Some grains are opaque because of their high Th and U content. 90 B. Zhao et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 385 (2013) 83–94

5. Interpretation and discussion

5.1. Source characteristics of different tectonic units

The Great Xing'an Range, the Lesser Xing'an Range, the Jiamusi Massif, the Zhangguangcai Range, and the North China Craton all constitute potential sedimentary sources for the Songliao Basin during the Late Cre- taceous. Determining the provenance from these tectonic units is the im- petus for this study. The North China Craton (NCC) is characterized by Neoarchean and Paleoproterozoic basement (Darbya and Gehrelsb, 2006), which will not be discussed here. In this paper, comprehensive zircon U–Pb age data around the Songliao Basin were collected for provenance analysis. In order to facilitate comparison and recognizing that few grain are as old as ~1800 Ma, ~2200 Ma and ~2500 Ma, which ages are widely distributed in northeast China, the histogram of zircon U–Pb ages ranges is limited to ages b1000 Ma.

5.1.1. The Great Xing'an Range Most granitoids in the northern Great Xing'an Range (in the Xing'an Massif, Fig. 1, area A1) were traditionally considered as Late Paleozoic, and four stages of granitic magmatism can be identified (IMBGMR, 1991; HBGMR, 1993; Miao et al., 2004; Wu et al., 2011). Carboniferous I-type granitoids are rarely developed in the massif, with isotopic ages of 340–300 Ma. Permian A-type granitoids occur as part of a huge Late Paleozoic A-type granitic in northern Great Xing'an Range; they were emplaced between 290 and 260 Ma (Hong et al., 1995,Rb–Sr isochron ages; Han et al., 1997; Wu et al., 2002, 2011). Another important stage of granitic magmatism took place in the north of the area in the Middle Jurassic, which ages range from 187 Ma to 157 Ma (Wu et al., 2011). The most important stage of granitic magmatism in this massif is the Early Cretaceous, in a belt extending in a NNE direction and crossing the mas- – Fig. 8. Probability plot of the U Pb ages. Area B, the Lesser Xing'an Range (Sun et al., sif boundaries. The age spectrum of this magmatic stage is 145–106 Ma 2000, 2004a; Miao et al., 2003). Area C, the Jiamusi Massif (Wilde et al., 2000, 2001, 2003; Wu et al., 2001; Huang et al., 2008; Meng et al., 2008, 2010; Xie et al., 2008). (Wu et al., 2011). Three stages of granitic magmatism are developed in the central Great Xing'an Range, which crosses the boundary between the Xing'an Th/U values range from 0.61 to 4.75 (Table 1), suggesting a magmatic and Songnen Massifs (Fig. 1,areaA2).Thefirst stage is represented by origin. One analysis was discarded because of low data acquisition. an intensively deformed granitic gneiss and associated quartz diorite After common-Pb corrections were made, eight analyses were dis- from Zhalantun with zircon U–Pb ages of 466–446 Ma, indicating that carded because of their discordant ages. The remaining 72 grains gave minor Early Paleozoic granitoids were developed in this terrane. Car- concordant ages at the 90% confidence level. The 72 ages mainly fall boniferous–Permian granitoids (359–249 Ma) are mainly distributed into three groups: 117–169 Ma (48 grains), 179–238 Ma (12 grains) in the north of the area. The main stage of granitic magmatism was dur- and 305–381 Ma (9 grains). The oldest zircon grain is 1825±10 Ma, ing the Early Cretaceous (145–120 Ma) in both the Xing'an and Songliao and the youngest zircon grain is 89.6±0.8 Ma. Analytical results are Massifs (Ge et al., 2005, 2007; Wu et al., 2011). presented in Table 1 and Fig. 5. The southern Great Xing'an Range (Fig. 1, area A3), which extends into the western part of the Songliao Massif, developed two separate stages of granitic magmatism. Paleozoic granitoids are mostly located in the western part and the zircon U–Pb ages range from 321 to 237 Ma. Mesozoic granitoids include granodiorite, monzogranite and syenogranite, with ages in the range of 150–131 Ma (Ge et al., 2005, 2007; Wu et al., 2011). The volcanic rocks in the Great Xing'an Range were considered to be Late Jurassic to Early Cretaceous. The majority of the dated volcanic rocks in the northern segment erupted in the Early Cretaceous, with a minority erupted in the Late Jurassic and mostly in the west of the northern Great Xing'an Range (Ge et al., 2001; Wang et al., 2006; Zhang et al., 2008). Volcanic rocks in the entire southern Great Xing'an Range erupted in both the Late Jurassic and Early Cretaceous (Zhang et al., 2010). Two stages of volcanism in the southern Great Xing'an Range are dated in the Late Jurassic at 160–150 Ma and in the Early Cretaceous at 141–122 Ma (Guo et al., 2008).

5.1.2. The Lesser Xing'an Range The granitoids in northwestern Lesser Xing'an Range (Fig. 1,areaB) are mainly two stages, the older one is characterized by the peralkaline Fig. 9. Probability plot of the U–Pb ages of the Zhangguangcai Range (Wu et al., 2000a, – 2002, 2004; Sun et al., 2004a, 2005; Liu et al., 2008; Chen et al., 2009a,b; Wu et al., pluton (A-type granite), which has an age spectrum of 290 260 Ma, 2011). and younger granitic magmatism took place in the Middle Jurassic B. Zhao et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 385 (2013) 83–94 91

Fig. 10. Maps of Late Cretaceous depositional environments in the Songliao Basin and the provenance directions. A. K2y1 is the first member of the Yaojia Formation. B. K2n4 is the fourth member of the Nenjiang Formation. Sample z-1 is from the older K2y1 unit and sample a-1 is from the younger K2n4 unit. . The K2y1 depositional facies map modified after Feng et al. (2010). from 160 Ma to 171 Ma (Sun et al., 2000; Miao et al., 2003). In the east- granitic magmatism in the area. The first, characterized by deforma- ern Lesser Xing'an Range, peralkaline pluton (A-type granite) intrusion tion structures with limited exposure, is Early Paleozoic with ages took place in 222±5 Ma, which was much later than the northwestern ranging from 447 to 508 Ma. The second has zircon U–Pb age of event (Sun et al., 2004a). In addition, Early Paleozoic granites (ages from 175–222 Ma, with the A-type Qingshui, Chaoxiantun, Milin and 508 Ma to 471 Ma) are found in the east of the Lesser Xing'an Range Maojiatun plutons recording ages of 222 ± 5 Ma, 176 ± 2 Ma, 197 ± (Liu et al., 2008). 2 Ma and 212 ±2 Ma, respectively (Wu et al., 2002; Sun et al., 2004a; Liu et al., 2008). 5.1.3. The Jiamusi Massif The Jiamusi Massif (Fig. 1, area C) is dominated by the granulite- 5.2. Detrital zircon provenance analysis facies Mashan complex, the Heilongjiang complex, Paleozoic granitoids, and volcanic rocks. Moreover, the Mesozoic–Cenozoic volcanic- First and the most important, zircons from the fourth member of sedimentary assemblages also widely occur in the region (Meng et Nenjiang Formation (sample a-1) are quite different from grains al., 2010). The granitoids in the area can be divided into deformed from the first member of the Yaojia Formation (sample z-1, Fig. 6). and undeformed types. The recorded granitic magmatism in the Detrital zircon ages of sample a-1 mainly fall into three groups: area was between 530 and 515 Ma, followed by granulite/amphiolite 90–110 Ma (10 grains), 190–220 Ma (14 grains) and ~1800 Ma (10 facies metamorphism at about 500 Ma. Another stage of granitic mag- grains, Figs. 5 and 6). Generally, ages of the zircons from the Nenjiang matism took place in the Permian at 270–254 Ma (Wilde et al., 1997; Formation are scattered. On the contrary, detrital zircons from the Wu et al., 2000a, 2001, 2011). first member of the Yaojia Formation are distributed in a more con- centrated range. The ages of about half of the zircons (39 grains) 5.1.4. The Zhangguangcai Range range from 130 Ma to 160 Ma, with a peak at ~144 Ma, and the re- The Zhangguangcai Range (Fig. 1, area D) is characterized by mainder are b200 Ma. In addition, a small peak is around 350 Ma voluminous Phanerozoic granitoids, with rare Proterozoic metamor- (Fig. 6). This clearly shows that source areas of the fourth member phic rocks, Paleozoic strata and Late Mesozoic-Cenozoic volcanic- of the Nenjiang Formation are quite different from the source of the sedimentary assemblages (Wu et al., 2000b, 2002). Most of the gran- first member of the Yaojia Formation. itoids in the Zhangguangcai Range were emplaced during the Late Detrital zircons with the age of 98–109 Ma (five grains) from sam- Triassic–Middle Jurassic, with a limited number emplaced during ple a-1 may have come from the Liaoyuan Terrane, southeast of the the Early Paleozoic (Wu et al., 2011). There are two main phases of Songliao Basin, the only site where granite of this age range is found 92 B. Zhao et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 385 (2013) 83–94

((Sun et al., 2008; Wu et al., 2011). Grains of ages from 190 to 220 Ma the Okhotsk Sea to the north and Pacific Plate subduction beneath in sample a-1 are very important for the judgment of the source areas, the Asian continent to the east were the major tectonic events affect- because this age range is not present in either the Great Xing'an ing the formation and evolution of the Songliao Basin (Maruyama and Range or the Jiamusi Massif (Figs. 7 and 8). However, these phases Seno, 1986; Watson et al., 1987; Li, 1996; Davis et al., 1998; Zheng et of granitoids are widely distributed in the eastern Lesser Xiang'an al., 1998; Yang et al., 2003). Compression from the Okhotsk Sea dom- Range and the Zhangguangcai Range (Wu et al., 2002, 2011; Sun et inated in early basin history (Davis et al., 1998; Zheng et al., 1998; Shan al., 2004a, 2005; Figs. 8 and 9). In addition, this sample contains et al., 2009), but then weakened. In contrast, compression from the Pa- minor zircons dated from 250 to 290 Ma, which possibly came from cific Plate was modest early in basin history, but became dominant by the Great Xing'an Range (Wu et al., 2002; Fig. 7), which suggests the end; the turning point occurred in the early Late Cretaceous, which that the Great Xing'an Range was still a minor source area of the resulted in a tectonic inversion of the eastern Songliao Basin (Feng et Songliao Basin in this period. It can be concluded from the above anal- al., 2010). This paper demonstrates clearly that the provenance of the ysis that the main source areas of the fourth member of the Nenjiang fourth member of the Campanian Nenjiang Formation was different Formation were mainly the Zhangguangcai Range, the eastern Lesser from the first member of the Coniacian–Santonian Yaojia Formation, Xiang'an Range and areas southeast of Songliao Basin. The sedimento- and the provenance above the nonconformity became much more com- logic evidence also support this view; studies show that numerous plex and the eastern source increased significantly, while the western deltas along the eastern margin of the Songliao Basin deposited sedi- source sharply declined. This means that the tectonic inversion began ments of the third and fourth members of the Nenjiang Formation much earlier than 73 Ma as previously thought. According to the depo- (Feng et al., 2010, 2012). sitional age of the first member of the Yaojia Formation, inversion was Sample z-1 from the first member of the Yaojia Formation, which younger than about 87 Ma and older than about 73 Ma. is below the nonconformity, shows completely different source areas. Detrital zircons in this sample are dated between 130 Ma and 150 Ma 6. Conclusions (24 grains) and are most show elevated Th/U ratios, indicating a magmatic origin. The zircon source histograms clearly show that the Great The following conclusions are based on analyses of the detrital zir- Xing'an Range could be the source terrrane, including the northern, con U–Pb geochronology of selected sandstones from Upper Cretaceous the central and the southern areas (Fig. 7, A1, A2 and A3). In addition, strata in the Songliao Basin. The main source areas of the fourth mem- zircons with age around 350 Ma (eight grains) could be from the cen- ber of the Nenjiang Formation were mainly the Zhangguangcai Range, tral Great Xing'an Range or the northeastern part of the Lesser the eastern Lesser Xiang'an Range and the southeastern margin of the Xing'an Range (Miao et al., 2004; Wu et al., 2011; Figs. 7-A2, 8). Songliao Basin. The dominant provenance during deposition of the Therefore, the main provenance of the first member of the Yaojia For- first member of the Yaojia Formation was the northern, the central mation was the northern, the central and the southern Great Xing'an and the southern Great Xing'an Range. This change could have hap- Range. pened any time before deposition of the third member of the Nenjiang In summary, the source areas above and below the nonconformity Formation and after the first member of the Yaojia Formation. It may are of significant difference. The dominant provenance below the non- have been associated with increased westward subduction of the Pacific conformity is from the northern, western and southwestern margins plate. The tectonic inversion of the eastern Songliao Basin began be- of the Songliao Basin (Fig. 10,Ky ). But sediments above were from 2 1 tween 87 Ma and 73 Ma, much earlier than previously thought at the northeastern, eastern and southeastern margins of the Songliao 73 Ma. Basin (Fig. 10,K2n4). However, the specifictimeofthischangecannot be defined more accurately; it could have happened before the third member of the Nenjiang Formation and after the first member of the Acknowledgements Yaojia Formation. We thank the staff of the State Key Laboratory of Continental 5.3. Summary and further discussion Dynamics, Northwest University, Xi'an, China, for their advice and assistance during U–Pb zircon dating using LA-ICP-MS. Thanks to Detrital zircon U–Pb geochronology was used to explore three the Daqing Petroleum Exploration and Development Institute for major geological problems: the maximum depositional age of select- supplying the drilling core samples. The authors are grateful to Prof. ed Upper Cretaceous strata, the provenance of the sediment and the C.S. Wang for his constructive comments which greatly improved tectonic setting of the geological unit(Cawood and Nemchin, 2000; the quality of the manuscript. We also thank Prof. Robert W. Scott Andrew et al., 2008; William and George, 2009; Bethunea et al., and Prof. Luba Jansa for their help to improve the manuscript. This 2010; Long et al., 2010; Adams et al., 2011). Among these, the second study was financed by the National Basic Research Program of China has the widest and the most direct application to the geology of the (973 Program) 2012CB822000 (to CW). Songliao Basin. Feng et al. (2010) identified the nonconformity interface in the Upper Cretaceous Nenjiang Formation (Campanian) in the References north-central Songliao Basin through the seismic method, but the structural mechanism of the nonconformity is still unknown. Our hy- Adams, C.J., Miller, H., Aceñolaza, F.G., 2011. The Pacific Gondwana margin in the late Neoproterozoic–early Paleozoic: detrital zircon U–Pb ages from metasediments pothesis is that the provenance below and above the nonconformity in northwest Argentina reveal their maximum age, provenance and tectonic set- interface changed. Provenance analysis was used to solve the prob- ting. Gondwana Research 17 (1), 71–83. lem. Highly accurate sampling of cores from members was carried Anderson, T., 2002. Correction of common lead in U–Pb analyses that do not report 204 – out to avoid contamination and to improve the credibility of the anal- Pb. Chemical Geology 192, 59 79. Andrew, M., Mark, F., Paul, M., 2008. Provenance characteristics of Scandinavian base- ysis. In ensuring the accuracy of the sampling condition, Laser abla- ment terrains: constraints from detrital zircon ages in modern river sediments. tion ICP-MS which represents a highly suitable method for sediment Sedimentary Geology 210, 61–85. provenance studies where large numbers of analyses are often re- Bao, Q.Z., Zhang, C.J., Wu, Z.L., Wang, H., Li, W., Sang, J.H., Liu, Y.S., 2007. SHRIMP zircon U–Pb geochronology of a Carboniferous quartz diorite in Baiyingaole area, Inner quired to identify the major sources of sediments (Kosler et al., Mongolia and its implications (in Chinese with English abstract). Journal of Jilin 2002; Dhuimea et al., 2007) was used for U–Pb dating in this study. University (Earth Sciences) 37, 15–23. The results fit the hypothesis very well. Bethunea, K.M., Hunterb, R.C., Ashtonc, K.E., 2010. Age and provenance of the Paleo- proterozoic Thluicho Lake Group based on, detrital zircon U–Pb SHRIMP geo- The Songliao Basin formed and evolved during the Middle Jurassic chronology: new insights into the protracted tectonic evolution of the to Late Cretaceous (Gao and Cai, 1997). The closure and collision of southwestern Rae Province, Canadian Shield. Precambrian Research 182, 83–100. B. Zhao et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 385 (2013) 83–94 93

Bruguier, O., Lancelet, J.R., 1997. U–Pb dating on single detrital zircon grains from the Kosler, J., Fonneland, H., Sylvester, P., Tubrett, M., Pedersen, R.B., 2002. U–Pb dating of Triassic Songpan–Ganze flysch (central China): provenance and tectonic correla- detrital zircons for sediment provenance studies-a comparison of laser ablation tions. Earth and Planetary Science Letters 152, 217–231. ICPMS and SIMS techniques. Chemical Geology 182, 605–618. Carter, A., Steve, J.M., 1999. Combined detrital-zircon fission-track and U–Pb dating: a Lee, J., Williams, I., Ellis, D., 1997. Pb, U and Th diffusion in nature Zircon. Nature 390, new approach to understanding hinterland evolution. Geology 27 (3), 235–238. 159–162. Cawood, P.A., Nemchin, A.A., 2000. Provenance record of a rift basin: U/Pb ages of de- Li, D.S., 1996. Basic characteristics of oil and gas basins in China. Southeast Asian Earth trital zircons from the Perth Basin, Western Australia. Sedimentary Geology 134, Science 13, 299–304 (in Chinese). 209–234. Li, S.L., Ouyang, Z.Y., 1998. Tectonic framework and evolution of Xing'anling Mongolian Chen, L., Sun, J.G., Chen, X.S., 2009a. Zircon LA-ICP MS U–Pb dating of granite from the Orogenic Belt (XMOB) and its adjacent region (in Chinese with English abstracts). Yingchengzi gold deposit area in the Eastern Zhangguangcailing area and its geo- Marine Geology & Quaternary Geology 18, 45–54. logical significance. Acta Geologica Sinica 83 (9), 1327–1334. Li, J.Y., Niu, B.G., Song, B., 1999. Crustal formation and evolution of Northern Changbai Chen, Z.P., Zhong, J.H., Yang, Y.F., 2009b. Heavy mineral features and source of sedi- Mountains, Northeast China (in Chinese with English abstract). Geological Publish- ments of Fuyu oil bed in the western area of Daqing Placanticline. Inner Mongolia ing House, Beijing. 1–137 pp. Petrochemical Industry 15, 119–125 (in Chinese with English abstract). Li, J.Y., Wang, K.Z., Sun, G.H., 2006. Paleozoic active margin slices in the southern Cherniak, D.J., Watson, E.B., 2000. Pb diffusion in zircon. Chemical Geology 172, 5–24. Turfan–Hami basin: geological records of subduction of the Paleo-Asian Ocean Chi, Y.L., Yun, J.B., Meng, Q.A., 2002. Deep Structure and Dynamics of Songliao Basin and plate in central Asian regions (in Chinese with English abstracts). Acta Petrologica Hydrocarbon Accumulation. Petroleum Industry Press, Beijing, pp. 1–112. Sinica 22, 1087–1102. Darbya, B.J., Gehrelsb, G., 2006. Detrital zircon reference for the North China block. Liu, W., Siebel, W., Li, X.J., Pan, X.F., 2005. Petrogenesis of the Linxi granitoids, northern Journal of Asian Earth Sciences 26, 637–648. Inner Mongolia of China: constraints on basaltic underplating. Chemical Geology Davis, G.A., Zheng, Y., Zhang, J., 1998. The enigmatic Yinshan fold-and-thrust belt of 219, 5–35. northern China: new views on its intraplate contractional styles. Geology 26, 43–46. Liu, J.F., Chi, X.G., Dong, C.Y., 2008. Discovery of Early Paleozoic granites in the eastern Dhuimea, B., Bosch, D., Bruguier, O., 2007. Age, provenance and post-deposition metamor- Xiao Hinggan Mountains, northeastern China and their tectonic significance. Geo- phic overprint of detrital zircons from the Nathorst Land group (NE Greenland) — a logical Bulletin of China 27 (4), 535–544. LA-ICP-MS and SIMS study. Precambrian Research 155, 24–46. Liu, J.F., Chi, X.G., Zhang, X.Z., Ma, Z.H., Zhao, Z., Wang, T.F., Hu, Z.C., Zhao, X.Y., 2009a. Fedo, C.M., Sircombe, K.N., Rainbird, R.H., 2003. Detrtial zircon analysis of the sedimen- Geochemical characteristics of Carboniferous quartz diorite in the southern Xiwuqi tary record. Reviews in Mineralogy and Geochemistry 53, 277–303. area, Inner Mongolia and its tectonic significance (in Chinese with English ab- Feng, Z.Q., Jia, C.Z., Xie, X.N., 2010. Tectonostratigraphic units and stratigraphic se- stract). Acta Geologica Sinica 83, 365–376. quences of the nonmarine Songliao Basin, northeast China. Basin Research 22, Liu, Y.S., Hu, Z.C., Gao, S., 2009b. In situ analysis of major and trace elements of anhy- 79–95. drous minerals by LA-ICP-MS without applying an internal standard. Chemical Ge- Feng, Z.Q., Zhang, S., Fu, X.L., 2012. Depositional evolution and accumulation response ology 257 (1–2), 34–43. of Yaojia–Nenjiang Formation in Songliao Basin. Earth Science Frontiers 19 (1), Long, X.P., Yuan, C., Sun, M., 2010. Detrital zircon ages and Hf isotopes of the early 078–088. Paleozoic flysch sequence in the Chinese Altai, NW China: new constrains on Gao, R., Cai, X., 1997. Hydrocarbon Formation Conditions and Distribution Rules in the depositional age, provenance and tectonic evolution. Tectonophysics 480, Songliao Basin. Petroleum Industry Press, Beijing. (in Chinese). 213–231. Ge,W.C.,Li,X.H.,Lin,Q.,Sun,D.Y.,Wu,F.Y.,Yun,S.H.,2001.Geochemistryofearly Ludwig, K.R., 2003. ISOPLOT 3: a geochronological toolkit for Microsoft Excel. Berkeley Cretaceous alkaline rhyolites from Hulun Lake, Da Xing'an Ling and its tectonic Geochronology Centre Special Publication, 4, p. 74. implication. Chinese Journal of Geology 36, 17–183 (in Chinese with Maruyama, S., Seno, T., 1986. Orogeny and relative plate motions: example of the Englishabstract). Japanese Islands. Tectonophysics 127 (3–4), 305–329. Ge, W.C., Wu, F.Y., Zhou, C.Y., 2005. Zircon U–Pb ages and its significance of the Maruyama, S., Isozaki, Y., Kimura, G., 1997. Paleogeographic maps of the Japanese Mesozoic granites in the Wulanhaote region, central Da Hinggan Mountain. Acta Islands: plate tectonic synthesis from 750 Ma to the present. The Island Arc 6, Petrologica Sinica 21 (3), 749–760. 121–142. Ge, W.C., Wu, F.Y., Zhou, C.Y., Zhang, J.H., 2007. Porphyry Cu–Mo deposits in the eastern Meng, E., Xu, W.L., Pei, F.P., 2008. Chronology of Late Paleozoic volcanism in eastern Xing'an–Mongolian Orogenic Belt: mineralization ages and their geodynamic im- and southeastern margin of Jiamusi Massif and its tectonic implications. Chinese plications. Chinese Science Bulletin 52, 3416–3427. Science Bulletin 53, 1231–1245. Gradstein, F.M., Ogg, J.G., Smith, A.G., Bleeker, W., Lourens, L.J., 2004. A new Geologic Meng, E., Xu, W.L., Pei, F.P., 2010. Detrital-zircon geochronology of Late Paleozoic sed- Time Scale, with special reference to Precambrian and Neogene. Episodes 27 (2), imentary rocks in eastern Heilongjiang Province, NE China: implications for the 83–100. tectonic evolution of the eastern segment of the Central Asian Orogenic Belt. Tec- Griffin, W.L., Belousova, E.A., Shee, S.R., Pearson, N.J., O'Reilly, S.Y., 2004. Archean crust- tonophysics 485, 42–51. al evolution in the northern Yilgarn craton: U–Pb and Hf-isotope evidence from de- Miao, L.C., 2003. SHRIMP Zircon geochronological studies of the Da Hinggan Mountains. trital zircons. Precambrian Research 131, 231–282. Report of the Postdoctoral Research, Institute of Geology and Geophysics, Chinese Guo, F., Fan, W.M., Li, C.W., Gao, X.F., Miao, L.C., 2008. Early Cretaceous highly positive Academy of Sciences.

εNd felsic volcanicrocks from the Hinggan Mountains, NE China: origin and impli- Miao, L.C., Fan, W.M., Zhang, F.Q., 2003. Zircon SHRIMP geochronology study and its cations for Phanerozoic crustal growth. International Journal of Earth Sciences 98 significance of the Xinkailing–Kolo complex in Northwest of Xiaoxing'an. Chinese (6), 1395–1411. Science Bulletin 48 (22), 2315–2323. Han, B.F., Wang, S.G., Jahn, B.M., Hong, D.W., Kagami, H., Sun, Y.L., 1997. Depletedman- Miao, L.C., Fan, W.M., Zhang, F.Q., Liu, D.Y., Jian, P., Shi, G.H., Tao, H., Shi, Y.R., 2004. tle magma source for the Ulungur River A-type granites from north Xinjiang, Zircon SHRIMP geochronology of the Xinkailing–Kele complex in the northwestern China: geochemistry and Nd–Sr isotopic evidence, and implication for Phanerozoic Lesser Xing'an Range, and its geological implications. Chinese Science Bulletin 49, crustal growth. Chemical Geology 138, 135–159. 2201–2209. HBGMR (Heilongjiang Bureau of Geology and Mineral Resources), 1993. Regional Moecher, D.P., Samson, S.D., 2006. Differential zircon fertility of source terranes and Geology of Heilongjiang Province (in Chinese with English abstract). Geological natural bias in the detrital zircon record: implications for sedimentary provenance Publishing House, Beijing. pp. 347–418. analysis. Earth and Planetary Science Letters 247, 252–266. Himeno, O., Ohira, H., Liu, Z.J., Jin, X., Watanabe, K., 2001. Provenance ages of Creta- Muller, R.D., Maria, S., 2008. Age, spreading rates, and spreading symmetry of the ceous strata in the Songliao Basin, northeast China inferred from fission track world's ocean crust. Geochemistry, Geophysics, Geosystems 9 (4), 1–19. data. International Geology Review 43 (10), 945–952. Peng, G.L., Wu, C.D., Zhang, S., 2010. Provenance Analysis of the Member 2 and 3 of the Hong, D.W., Huang, H.Z., Xiao, Y.J., Xu, H.M., Jin, M.Y., 1995. Permian alkaline granites in Upper Cretaceous Nenjiang Formation in Northern Songliao Basin. Acta Scien- central Inner Mongolia and their geodynamic significance. Acta Geologica Sinica 8, tiarum Naturalium Universitatis Pekinensis 46 (4), 555–562. 27–39. Ren, J.Y., 2004. Tectonic significance of S6 boundary in Dongying Depression, Bohai Huang, Q.H., Tan, W., Yang, H.C., 1999. Stratigraphic succession and chronosrata of Cre- Gulf Basin. Earth Science-Journal of China University of Geosciences 29 (1), taceous in Songliao Basin. Petroleum Geology & Oilfield Development in Daqing 18 69–76. (6), 18–28. Ren, J.Y., Tamaki, K., Li, S.T., 2002. Late Mesozoic and Cenozoic rifting and its dynamic Huang, Y.C., Ren, D.H., Zhang, X.Z., 2008. Zircon U–Pb dating of the Meizuo Granite and setting in Eastern China and adjacent areas. Tectonophysics 344, 175–205. geological significance in the Huanan Uplift, East Heilongjiang Province. Journal of Shan, X.L., Qin, S.H., Zhang, Y., 2009. Seismic evidence and geological significance of Jilin University (Earth Science Edition) 38 (4), 631–638. thrust-extension structure in upper basement of north Songliao Basin. Chinese IMBGMR (Inner Mongolian Bureau of Geology and Mineral Resources), 1991. Regional Journal of Geophysics 52 (8), 2044–2049 (in Chinese with English abstract). Geology of Inner Mongolian Automo (in Chinese with English summary). Geolog- Stepashko, A.A., 2006. The Cretaceous dynamics of the Pacific plate and stages of mag- ical Publishing House, Beijing. 725 pp. matic activity in Northeastern Asia. Geotectonics 40 (3), 225–235. Jackson, S.E., Pearson, N.J., Griffin, W.L., Belousova, E.A., 2004. The application of laser Stuart, R.C., Muller, R.D., 2008. Convection models in the Kamchatka region using im- ablation-inductively coupled plasma-mass spectrometry to in situ U–Pb zircon posed plate motion and thermal histories. Journal of Geodynamics 46, 1–9. gochronology. Chemical Geology 211, 47–69. Sui, Z.M., Ge, W.C., Wu, F.Y., Zhang, J.H., Xu, X.C., Cheng, R.Y., 2007. Zircon U–Pb ages, Kelty, T.K., Yin, A., Dash, B., Gehrels, G.E., Ribeiro, A.E., 2008. Detrital-zircon geochronol- geochemistry and its petrogenesis of Jurassic granites in northwestern part of ogy of Paleozoic sedimentary rocks in the Hangay–Hentey basin, north-central the Da Hinggan Mts (in Chinese with English abstract). Acta Petrologica Sinica Mongolia: implications for the tectonic evolution of the Mongol–Okhotsk Ocean 23, 461–480. in central Asia. Tectonophysics 451, 97–122. Sui, Z.M., Ge, W.C., Xu, X.C., Zhang, J.H., 2009. Characteristics and geological Kosler, J., Sylvester, P., 2003. Present trends and the future of zircon in geochronology: implications of the Late Paleozoic post-orogenic Shierzhan granite in the Great laser ablation ICPMS. In: Hanchar, J.M., Hoskin, P.M.O. (Eds.), zircon: Review of Xing'an Range (in Chinese with English abstract). Acta Petrologica Sinica 25, Mineral Geochemistry, 53, pp. 243–275. 2679–2686. 94 B. Zhao et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 385 (2013) 83–94

Sun, D.Y., Wu, F.Y., Li, H.M., 2000. The relationship between the times of the orogenic Wu, F.Y., Wilde, S.A., Sun, D.Y., 2001. Zircon SHRIMP U–Pb ages of gneissic granites in late A-type granites in Northwest Xiaoxing'an and with eastern of Sauron Hill– Jiamusi Massif, northeastern China (in Chinese with English abstracts). Acta Petro- Hegen Hill–Zhalaite collided extension. Chinese Science Bulletin 45 (20), logica Sinica 17, 443–452. 2217–2222. Wu, F.Y., Sun, D.Y., Li, H.M., 2002. A-type granites in northeastern China: age and Sun, D.Y., Wu, F.Y., Gao, S., 2004a. LA-ICPMS zircon U–Pb age of the Qingshui pluton in geochemical constraints on their petrogenesis. Chemical Geology 187, 143–173. the east Xiao Hinggan Mountains (in Chinese with English abstract). Acta Geos- Wu, F.Y., Wilde, S.A., Sun, D.Y., Zhang, G.L., 2004. Geochronology and petrogenesis of cientica Sinica 25, 213–218. post-orogenic Cu, Ni-bearing mafic–ultramafic intrusions in Jilin, NE China. Journal Sun, D.Y., Wu, F.Y., Zhang, Y.B., 2004b. The final closing time of the west Lamulun of Asian Earth Sciences 23, 781–797. River–Changchun–Yanji plate suture zone Evidence from the Dayushan granitic Wu, F.Y., Zhao, G.C., Sun, D.Y., 2007a. The Hulan Group: its role in the evolution of the pluton, Jilin Province. Journal of Jiling University (Earth Science Edition) 34 (2), Central Asian Orogenic Belt of NE China. Journal of Asian Earth Sciences 30, 174–181. 542–556. Sun,D.Y.,Wu,F.Y.,Gao,S.,Lu,X.P.,2005.Confirmation of two episodes of A-type Wu, F.Y., Yang, J.H., Lo, C.H., 2007b. The Heilongjiang Group: a Jurassic accretionary granite emplacement during Late Triassic and Early Jurassic in the central Jilin complex in the Jiamusi Massif at the western Pacific margin of northeastern Province, and their constraints on the structural pattern of the east Jilin– China. Journal of Asian Earth Sciences 30, 542–556. Heilongjiang area, China (in Chinese with English abstract). Earth Science Frontiers Wu, F.Y., Sun, D.Y., Ge, W.C., Zhang, Y.B., Grant, M.L., Wilde, S.A., Jahn, B.M., 2011. 12 (2), 263–275. Geochronology of the Phanerozoic granitoids in northeastern China. Journal of Sun, J.G., Chen, L., Zhao, J.K., Men, L.J., Pang, W., Chen, D., Liang, S.N., 2008. SHRIMP U– Asian Earth Sciences 41, 1–30. Pb dating of zircon from Late Yanshanian granitic complex in Xiaoxinancha gold- Xie, M.Q., 2000. Amalgamating plate tectonic and its droved mechanism tectonic evo- rich copper orefield of Yanbian and its geological implications (in Chinese with lution of northeast China and adjacent area (in Chinese). Science Press, Beijing, pp. English abstract). Mineral Deposits 27, 319–328. 21–45. Wang, F., Zhou, X.H., Zhang, L.C., Ying, J.F., Zhang, Y.T., Wu, F.Y., Zhu, R.X., 2006. Late Xie, H.Q., Miao, L.C., Chen, F.K., 2008. Characteristics of the “Mashan Group” and zircon Mesozoic volcanism in the Great Xing'an Range (NE China): timing and implica- SHRIMP U–Pb dating of granite in Muling area, southeastern Heilongjiang Prov- tions for the dynamic setting of NE Asia. Earth and Planetary Science Letters 251, ince, China: constraint on crustal evolution of the southernmost of Jiamusi Massif. 179–198. Geological Bulletin of China 27 (12), 2127–2137. Wang, L.W., Wang, Y., Yang, J., 2007. Pre-Mesozoic basement provenance tracing of the Yang, B.J., Zhang, M.S., Wang, P.J., 2003. Geological–geophysical analytic interpretation Songliao Basin by means of detrital zircon SHRIMP chronology. Earth Science Fron- on oil and gas potential region of China, vol. 1. Science Press, Beijing (in Chinese tiers 14 (4), 152–158. with English abstract). Wang, P.J., Gao, Y.F., Ren, Y.G., 2009. 40Ar/39Ar age and geochemical features of mugear- Ye, H.W., Zhang, X., 1994. The 40Ar–39Ar age of the vein crossite in blueschist in ite from the Qingshankou Formation: significances for basin formation, hydrocar- Mudanjiang area, NE China and its geological implication (in Chinese with English bon generation and petroleum accumulation of the Songliao Basin in Cretaceous. abstract). Journal of Changchun University of Earth Sciences 24, 369–372. Acta Petrologica Sinica 25 (5), 1178–1190. Ye, M., Zhang, S.H., Wu, F.Y., 1994. Tectonic units and evolution along the Manzhouli– Watson, M.P., Hayward, A.B., Parkinson, D.N., 1987. Plate tectonic history, basin devel- Suifenhe Geo-profile (in Chinese with English abstract). Journal of Changchun Uni- opment and petroleum source rock deposition onshore China. Marine and Petro- versity of Science and Technology 24, 241–245. leum Geology 4, 205–225. Yuan, H.L., Gao, S., Liu, X.M., 2004. Accurate U–Pb age and trace element determina- Wiedenbeck, M., Alle, P., Corfu, F., 1995. Three natural zircon standards for U–Th–Pb, tions of zircon by laser ablation inductively coupled plasma mass spectrometry. Lu–Hf, trace element and REE analyses. Geostandard Newsletter 19, 1–23. Geostandard Newsletter 28, 353–370. Wilde, S.A., Dorsett-Bain, H.L., Liu, J.L., 1997. The identification of a Late Pan-African Zhai, G.M., Wang, Z.W., Gao, R.Q., 1993. Petroleum Geology of China, vol.2. Petroleum granulite facies event in northeastern China: SHRIMP U–Pb zircon dating of the Industry Press, Beijing, pp. 55–305. Mashan Group at Liu Mao, Heilongjiang Province, China. Proceedings of the 30th Zhang, G.C., Xu, H., Liu, H.F., 1996. Inversion structures in relation to oil and gas field IGC: Precambrian Geology and Metamorphic Petrology, vol. 17. VSP International distribution in Songliao Basin. Acta Petrolei Sinica 17 (2), 9–14. Science Publishers, Amsterdam, pp. 59–74. Zhang, Y.X., Sun, Y.S., Zhang, X.Z., Yang, B.J., 1998. Manual on the geoscience transect Wilde, S.A., Zhang, X.Z., Wu, F.Y., 2000. Extension of a newly-identified 500 Ma meta- from Manzhouli to Suifenhe, China (1:1000000) (in Chinese). Geological Publish- morphic terrain in Northeast China: further U–Pb SHRIMP dating of the Mashan ing House, Beijing. 6~19. Complex, Heilongjiang Province, China. Tectonophysics 328, 115–130. Zhang, J.H., Ge, W.C., Wu, F.Y., Wilde, S.A., Yang, J.H., Liu, X.M., 2008. Large-scale Early Wilde, S.A., Wu, F.Y., Zhang, X.Z., 2001. The Mashan Complex: SHRIMP U–Pb zircon ev- Cretaceous volcanic events in the northern Great Xing'an Range, Northeastern idence for a Late Pan-African metamorphic event in NE China and its implication China. Lithos 102, 138–157. for global continental reconstructions. Geochimica 30 (1), 35–50. Zhang, F.Q., Cheng, X.G., Chen, H.L., 2009. Zircon chronological and geochemical con- Wilde, S.A., Wu, F.Y., Zhang, X.Z., 2003. Late Pan-African magmatism in Northeastern straints on the Late Mesozoic volcanic events in the southeastern margin of the China: SHRIMP U–Pb zircon evidence for igneous ages from the Mashan Complex. Songliao Basin, NE China. Acta Petrologica Sinica 25 (1), 40–54. Precambrian Research 122, 311–327. Zhang, J.H., Gao, S., Ge, W.C., Wu, F.Y., Yang, J.H., Wilde, S.A., Li, M., 2010. Geochronology William, R.D., George, E.G., 2009. Insights into North American Paleogeography and of the Mesozoic volcanic rocks in the Great Xing'an Range, northeastern China: Impli- Paleotectonics from U–Pb ages of detrital zircons in Mesozoic strata of the Colora- cations for subduction-induced delamination. Chemical Geology 276, 144–165. do Plateau, USA. International Journal of Earth Sciences (Geologische Rundschau) Zheng, Y.D., Davis, G.A., Wang, Z., 1998. Study on Daqingshan mega thrusting tectonics 99, 1247–1265. in Inner Mongolia. Science in China Series D 28 (4), 289–295. Wu, F.Y., Jahn, B.M., Wilde, S.A., 2000a. Phanerozoic crustal growth: U–Pb and Sr–Nd Zhou, J.B., Zhang, X.Z., Ma, Z.H., 2009a. Tectonic framework and basin evolution in isotopic evidence from the granites in northeastern China. Tectonophysics 328, Northeast China. Oil & Gas Geology 30 (5), 530–538. 89–113. Zhou, J.B., Wilde, S.A., Zhang, X.Z., 2009b. The onset of Pacific margin accretion in NE Wu, F.Y., Sun, D.Y., Li, H.M., 2000b. Zircon U–Pb ages of the basement rocks beneath the China: evidence from the Heilongjiang high-pressure metamorphic belt. Tectono- Songliao Basin, NE China. Chinese Science Bulletin 45, 1514–1518. physics 478 (3–4), 230–246.