provenance records of the north jiangsu basin, east … and to reconstruct the coupled relation...

Journal of Palaeogeography2014, 3(1): 99-114

Palaeogeography

DOI: 10.3724/SP.J.1261.2014.00006

Geochemistry and sedimentary environments

Provenance records of the North Jiangsu Basin, East China: Zircon U-Pb geochronology and geochemistry from the Paleogene Dainan

Formation in the Gaoyou Sag

Chun‑Ming Lin1, *, Xia Zhang1, Ni Zhang1, Shun‑Yong Chen1, Jian Zhou1, Yu‑Rui Liu2

1. State Key Laboratory for Mineral Deposits Research, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093, China

2. Institute of Geological Sciences, Jiangsu Oilfield Branch Company, SINOPEC, Yangzhou 225009, China

Abstract Detailed zircon U-Pb dating and whole‑rock geochemical analyses were car‑ried out on the sedimentary rocks of the Paleogene Dainan Formation from Gaoyou Sag in the North Jiangsu Basin, East China. Whole‑rock rare earth element characteristics suggest that the provenance was mainly from the Late Proterozoic low‑grade metamorphic felsic rocks in the Dabie-Sulu orogenic belt, with the parent rocks probably being the I‑type high‑potas‑sium granite gneiss. Cathodoluminescence images indicate that most of the detrital zircons are originally magmatic. A few zircons show overgrowths, indicating multiple‑episode tectonic events. The U-Pb age distribution patterns of the detrital zircons suggest four main mag‑matic episodes in the provenance: Late Archean-Early Proterozoic (2450-2600 Ma), Early Proterozoic (1700-1900 Ma), Late Proterozoic (700-850 Ma), and Late Paleozoic-Mesozoic (100-300 Ma). These zircon U-Pb age and whole‑rock geochemical results suggest that the sediments of the Dainan Formation were mainly sourced from the recycled orogenic belts within and/or around the North Jiangsu Basin, including the basement of the Yangtze Block, the Neoproterozoic rocks in the Dabie-Sulu orogenic belt, and the Mesozoic igneous rocks in the south part of Zhangbaling Uplift.

Key words zircon U-Pb dating, Paleogene, provenance analysis, Dainan Formation, North Jiangsu Basin, East China

1 Introduction*

The North Jiangsu Basin is one of the richest regions in oil and gas of East China, with widely distributed and thickest Mesozoic-Cenozoic strata. The Paleogene Dain-an Formation is one of the most productive reservoir in-tervals in the Gaoyou Sag, North Jiangsu Basin (Qiu et al., 2006). It shows a well exploration prospect as a struc-

* Corresponding author. E-mail: [email protected]. Received: 2013-07-27 Accepted: 2013-10-25

ture-lithologic reservoir (Zhang et al., 2005). There is a close relationship between the reservoir distribution and sedimentary facies, which in turn is controlled by a combi-nation of the tectonic system and sediment supply. Previ-ous studies on the Dainan Formation were predominantly focused on the paleontology, sequence stratigraphy, reser-voir and sedimentary facies (Zhang et al., 2005; Qiu et al., 2006; Zhou et al., 2010; Gao and Lin, 2012), however, lit-tle attention has been paid to the provenance studies (Shu et al., 2005).

At present, provenance analysis for sedimentary rocks

100 JOURNAL OF PALAEOGEOGRAPHY Jan. 2014

is conducted mainly by traditional methods such as min-eral components, heavy mineral analysis, and sedimentol-ogy. In contrast, there are few studies on the sedimentary basin using zircon U-Pb chronology and whole-rock geochemistry to recover sediment provenance character-istics (e.g., the types of parent rocks, formation stage and the related tectonic events) and to identify the different provenance contribution (Zhou et al., 2011; Zhang et al., 2012a, 2012b). The zircon U-Pb geochronology has its unique advantage in tracing the provenance of various sediments and sedimentary rocks, on which we can recon-struct palaeogeographic patterns, define related tectonic processes, and reveal the early continental evolution, and as a result the utility in provenance analysis has become one of the international research hot spots (Rainbird et al. 1997; Wysoczanski et al., 1997; Sircombe and Freeman, 1999; Cawood and Nemchin, 2000; Wilde et al., 2001; Vermeesch, 2004; Yue et al., 2005; Weislogel et al., 2006; Zheng et al., 2006; Xu et al., 2008; Zhou et al., 2008; Liu et al., 2012). In this paper, the provenance of the Paleo-gene Dainan Formation from Gaoyou Sag in the North Jiangsu Basin was studied in detail, based on the zircon U-Pb dating and whole-rock geochemistry analysis, which will be helpful to study the information of source rocks and to reconstruct the coupled relation between the sedimentary basin and provenance.

2 Geologic setting

The basement of the Yangtze Block experienced a se-ries of tectonic movements since it formed, and it was eventually stablized after the formation of the unified cra-ton by the Jinning Movement. It is characterized by a dual structure including the low-grade metamorphic rock series and plutonic metamorphic rock series, in which the latter is characterized by high seismic velocity, resistivity, mag-netic field strength and density. The plutonic metamor-phic rock series is present as clumps surrounded by the low-grade metamorphic rock series, and the biggest one is located in the east of Jianhu, north of Dafeng, which stitches together with the positive gentle magnetic fields of the central South Yellow Sea to form the “South Yellow Sea continental nucleus” in the Early Archean-Late Prote-rozoic; there are a number of small blocks scattered in the nuclear periphery (Figure 1; Zhang, 1991).

The North Jiangsu Basin is a large Cretaceous-Tertiary fault depressed basin developed on Proterozoic metamor-phic rocks and Early Mesozoic carbonate, turbidite, and clastic rocks basement in the northeast corner of the Yang-

tze Block and southern edge of the Sulu Orogen (Figure 2a; Shu et al., 2005). Geographically, it is located in the north of Jiangsu Province, with a small part lying in the Tianchang area of the East Anhui Province. It is 260 km in length and tapers from the east (220 km) to the west (110 km); it could be divided into three nearly east-west trending first-order tectonic units: the Dongtai Depression, the Jianhu Uplift, and the Yanfu Depression, from south to north; it is bounded by the Binhai Uplift in the north, the Sulu upheavals in the west and the Tongyang Uplift in the south, and it penetrates into the South Yellow Sea in the east, being the onshore part of the North Jiangsu-South Yellow Basin (Figure 2a, 2b; Shu et al., 2005). Before the Cretaceous Taizhou Formation, the North Jiangsu Basin was mainly controlled by the ancient Pacific tectonic re-gime; then it was affected by the combination of the Pa-cific Plate and the India Plate (Shu et al., 2005). The North Jiangsu Basin has experienced large-scale nappes during the Yinzhi-Yanshan period, forming a series of reverse faults with the cross-section west-dipping and the strike in a NE direction. At present, the oil and gas exploration lay-ers in the North Jiangsu Basin include the Late Cretaceous Taizhou Formation (E2t, 65-83.5 Ma), and the Paleogene Funing (E1f, 53-65 Ma), Dainan (E2d, 46-53 Ma), and Sanduo Formations (E2s, 37-46 Ma), which are character-ized by the lacustrine clastic-sedimentary rocks (Qiu et al., 2006; Chen, 2010; Liu, 2010).

The Gaoyou Sag is located in the central part of the Dongtai Depression and it is a dustpan-shaped fault-depression that is faulted in the south and overlapped in the north. It was formed by the differential elevation and subsidence of fault blocks during the Late Cretaceous-Late Paleocene Yizheng and Wubao movements. There are three fault systems (ENE, NE, and NW) formed in the Cenozoic in the study area; from south to north they are Zhen 1, Zhen 2, and Hanliu faults, which present as the boundary of the sag and divide the Gaoyou Sag into three secondary tectonic units (southern step-fault zone, central deep depression zone, and northern slope zone; Figure 2c). Hanliu fault is a south-dipping contemporaneous fault with strong activity in the western depression.

3 Samples and analytical methods

This study collected 60 mudstone samples, from 52 wells of Zhouzhuang, Huazhuang, Fumin, Yong’an, Caozhuang, Zhenwu, Shaobo, Lianmengzhuang, and Majiazui regions, for the rare earth element (REE) analysis in the Gaoyou Sag, North Jiangsu Basin. Four representative sandstone

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Chun-Ming Lin et al.: Provenance records of the North Jiangsu Basin, East China: Zircon U-Pb geochronology and geochemistry from the Paleogene Dainan Formation in the Gaoyou Sag

Figure 1 Distribution of the metamorphic basement in the North Jiangsu Basin and the adjacent regions (modified from Zhang, 1991).


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samples were obtained for detrital zircon U-Pb dating, lo-cated respectively at 2727.26 m in Well Z27 of Zhouzhuang (Zr1), 3165.0 m in Well F83 of South Fumin (Zr2), 3215.5 m in Well Sx14 of Shaobo (Zr3), and 2339.19 m in Well H32 of Huangjue (Figure 2c). Sandstone samples were firstly prepared by crushing, washing and magnetic separa-tion to detach zircons, which were in turn purified by hand-picking under a binocular microscope. These zircon grains were put on a double-sided adhesive and placed into a ring mold mounted by epoxy, and then polished about one-third of an individual grain diameter. Cathodoluminescence (CL) images of the zircon grains were taken at the State Key Laboratory of Continental Dynamics of Northwest Uni-versity, using scanning electron microscopy (Quanta 400 FEG) with Mono CL3+ (Gatan, USA). Zircon U-Pb dat-ing was carried out at the State Key Laboratory for Mineral Deposits Research of Nanjing University using an Agilent 7500a type ICP-MS attached with a New Wave UP213 laser ablation system (wavelength 213 nm; laser beam spot diameter 21-32 μm; frequency 5Hz; energy density 9J/cm2). The standard zircon GEMOC GJ-1 of Australia (207Pb/206Pb age=608.5 1.5 Ma) was used to correct the U-Pb fractionation, and standard zircon Mud Tank (inter-cept age of 732 5 Ma) as an internal standard to control the accuracy of analysis. More detailed analytical methods and procedures are described by Jackson et al. (2004) and Wang et al. (2013a). In addition, a key problem that us-ing detrital zircon U-Pb geochronology method for source tracing is the choice of the statistical-particle number. In this study, the zircon number per sample is 90-110 in con-sistent with the requirements of mathematical statistics (cf., Vermeesch, 2004; Weislogel et al., 2006). REE analysis is obtained using high resolution inductively coupled plasma mass spectrometry (Finnigan Mat Element 2) according to a standard method described by Gao et al. (2003).

4 Results

4.1 Rare earth elements (REE) characteristics

The chondrite-normalized REE patterns for the stud-ied sedimentary rocks are characterized by the significant enrichment of light REE, strong depletion in heavy REE, and obviously negative anomalies of Eu (the average δEu of 0.4). The total REE (∑REE) concentrations fall in the range 50.01-250.70 μg/g (average at 174.00 μg/g), which is higher than that of the North American shale (mean of 163.94 μg/g), but lower than the average post-Archean sedimentary rocks (184.77 μg/g) (Taylor and McLennan,

1985; McLennan, 1989). In addition, the REE parameters are similar to those of active continental margin, indicating that the tectonic background of parent rocks for the studied sedimentary rocks belongs to an active continental margin setting, with the parent rocks from the uplifted basement (Zhang et al., 2012a). However, comparing with the (La/Yb)N and LREE/HREE values (9.1 and 8.5, respectively) of the active continental margin sedimentary rocks (Bha-tia, 1985), the values of (La/Yb)N and LREE/HREE in the study area are relatively high (11.55 and 11.29, respective-ly), illustrating near-source characteristics, and the parent rocks are comparable with the felsic material of the aver-age continental crust (Zhang et al., 2012a).

4.2 Zircon U-Pb ages

4.2.1 Zircon morphology

Zircons from sample Zr1 are mainly misty rose, sec-ondarily deep rose, and the morphology is dominantly sub-rounded granular with a little sub-angular prismatic, irreg-ular shape and equigranular, euhedral columnar, showing the character of detrital zircons. Zircons from this sample are generally 30-70 μm in length. Zircons from sample Zr2 is mainly deep rose to pale pink, and the morphology is mainly sub-angular prismatic to sub-rounded granular. They are generally 50-100 μm in length, with a few of 100-150 μm. Zircons from sample Zr3 is dominantly deep rose, secondarily pale pink, and the morphology is mainly sub-rounded granular, with a little prismatic and irregular equigranular, occasionally angular columnar. The length is generally 50-120 μm. Zircons from sample Zr4 is mainly pale pink, with a bit deep rose and colorless; the morphol-ogy is predominantly sub-rounded granular and elongated oval granular, secondly angular, sub-angular and prismat-ic. They are mainly 50-120 μm in length, with a small part of 120-150 μm (Figure 3).

4.2.2 Zircon U-Pb age

In general, the radiogenic components are less in young zircon (<1000 Ma), and the radiogenic 207Pb abundance is lower than the 206Pb by about an order of magnitude for the differences in half-life and abundance between 235U and 238U, as a result, the higher precision 206Pb/238U age of the young zircon is selected as the crystallization age of the rock, while the 206Pb/207Pb age generally shows more un-certainty for the older zircon (>1000 Ma) (Compston et al., 1992). In addition, the computational-concordant ages of young zircons with discordance (%) more than 20% and of older ones with discordance (%) more than 15% are


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unreliable (Kong et al., 2009). Thus, the test samples of Zr1-Zr4 respectively got 97, 94, 100 and 85 valid data. In 206Pb/238U-207Pb/235U concordia diagram, all measured points are plotted on or near the concordia (Figure 4).

The Th/U ratios for all the spot analyses vary signifi-cantly, from 0.11 to 3.56 (Table 1), consistent with the high Th/U ratio of typical magmatic zircon (Wu and Zheng, 2004). Most zircon grains show oscillatory zoning in CL images (Figure 3), indicating a magmatic origin (cf., Connelly, 2000). A few zircons are composed of a dark core and a bright overgrowth, showing the metamorphic growth (overgrowth) or recrystallization, which indicates the sources of the Dainan Formation sediments have expe-rienced multiple tectonic-thermal events. For this case, we focus on the age of zircon cores. In fact, the analyses with ages >2500 Ma are generally from the zircon cores with higher psephicity (Figure 3), indicating that some of the sediments in the study area came from the Late Archean

provenance through long-distance and/or multiple trans-portations.

1) Sample Zr1: Zircon U-Pb ages of this sample vary significantly from 118±7 Ma to 2710±12 Ma, indicating the multi-sources for the detrital zircons (Figure 4; Table 2). A total of 30 analyses (accounting for 30.9%) are dis-tributed in the Paleoproterozoic (Pt1); There are separately 12 analyses belonging to the Archean (Ar) and Carbonifer-ous (C), accounting for 12.4% of the number of statistics; there are 11 and 10 analyses distributed in the Triassic (T) and Permian (P), accounting for 11.3% and 10.3% of the number of statistics, respectively; the analyses with ages in the Neoproterozoic (Pt3), Jurassic (J) and Cretaceous (K) are 6.2%, 6.2% and 5.2%, respectively, of the number of statistics; the other analyses are less than 5.0% of total zircons.

2) Sample Zr2: Zircon U-Pb ages of this sample range from 108±2 Ma to 3068±11 Ma (Figure 4; Table 2), with

Figure 4 Concordant diagrams of zircon U-Pb ages for clastic rocks from the Dainan Formation in Gaoyou Sag.


the main proportions at Pt1 and Ar, accounting for 22.9% and 19.8% of the number of statistics, respectively. The analyses at P, T and Pt3, occupying 11.5%, 9.4% and 9.4%, respectively; zircons at Mesoproterozoic (Pt2) made up about 8.4% of the number of statistics; C and K zircon grains are generally 5.2% of the number of statistics; Or-dovician (O), Silurian (S) and Devonian (D) zircon grains are less than 5.0% of the number of statistics (Table 2).

3) Sample Zr3: Zircon U-Pb ages of this sample range from 126±7 Ma to 2715±48 Ma (Figure 4; Table 2). They are mainly of Pt1 (39.0%) and Pt3 (26%). The Ar analyses

only occupy 12.0% of statistics; while the Permian (P) and other analyses account for about 6.0% and less than 5.0%, respectively (Table 2).

4) Sample Zr4: The zircon U-Pb ages are between 94±2 Ma and 3656±17 Ma with good coordination (Figure 4; Table 2). They are mainly distributed in the K and Pt3, accounted for 25.9% and 24.7% of statistics, respectively; secondly in the Pt1, about 15.3% of statistics; there are sep-arately 6 zircons from the C and T, about 7.1% of statistics. The zircon of other ages is all less than 5.0%, and the O and D zircons were not observed (Table 2).

Table 1 LA-ICP-MS zircon U-Pb dating results of the Dainan Formation in Gaoyou Sag

Spot Th(ppm)

U(ppm) Th/U 207Pb/206Pb 1σ 207Pb/235U 1σ 206Pb/238U 1σ

207Pb/206Pbage (Ma) 1σ

207Pb/235Uage (Ma) 1σ

206Pb/238Uage (Ma) 1σ %conc

Sample Number: Zr1; Position: Zhouzhuang (Well Zhou 27)

z14 561 1954 0.29 0.12041 0.00157 2.91579 0.04459 0.17568 0.00236 1962 12 1386 12 1043 13 188

z25 1107 799 1.38 0.05719 0.00109 0.53517 0.01060 0.06787 0.00093 499 22 435 7 423 6 103

z31 374 504 0.74 0.05278 0.00138 0.19179 0.00502 0.02635 0.00039 319 33 178 4 168 2 106

z32 81 92 0.88 0.05564 0.00397 0.38633 0.02645 0.05036 0.00129 438 107 332 19 317 8 105

z46 1144 2324 0.49 0.11547 0.00194 5.26227 0.09936 0.33069 0.00479 1887 16 1863 16 1842 23 102

z54 170 115 1.47 0.17021 0.00267 11.2415 0.19113 0.47908 0.00663 2560 13 2543 16 2523 29 101

z55 518 428 1.21 0.06762 0.00124 1.13205 0.02177 0.12143 0.00167 857 19 769 10 739 10 104

z58 285 204 1.40 0.10001 0.00390 0.24891 0.00919 0.01805 0.00035 70 275 115 22 118 7 97

z63 1937 1904 1.02 0.05169 0.00101 0.27988 0.00577 0.03928 0.00056 272 23 251 5 248 3 101

z70 136 849 0.16 0.06635 0.00132 1.18588 0.02463 0.12960 0.00182 817 22 794 11 786 10 101

z75 244 261 0.93 0.16335 0.00255 10.4333 0.18297 0.46337 0.00675 2491 13 2474 16 2454 30 102

z76 124 178 0.70 0.18630 0.00277 13.3371 0.21732 0.51929 0.00705 2710 12 2704 15 2696 30 101

z86 364 426 0.86 0.17517 0.00236 12.1089 0.18793 0.50141 0.00686 2608 12 2613 15 2620 29 100

z88 199 234 0.85 0.11015 0.00182 4.82197 0.08576 0.31759 0.00444 1802 15 1789 15 1778 22 101

z92 336 300 1.12 0.16136 0.00234 9.65682 0.15722 0.43418 0.00597 2470 12 2403 15 2325 27 106

z102 629 831 0.76 0.05092 0.00153 0.29028 0.00874 0.04134 0.00066 237 41 259 7 261 4 99

Sample number: Zr2; Position: Fumin (Well Fu 83)

fu14 1247 563 2.22 0.05540 0.00139 0.40730 0.01051 0.05332 0.00082 428 31 347 8 335 5 104

fu26 274 262 1.04 0.23226 0.00301 19.0164 0.28997 0.59392 0.00817 3068 11 3043 15 3005 33 101

fu38 377 839 0.45 0.11059 0.00180 5.27816 0.09795 0.34619 0.00523 1809 15 1865 16 1916 25 97

fu44 1493 1246 1.20 0.05157 0.00137 0.12781 0.00339 0.01798 0.00026 266 35 122 3 115 2 231

fu46 367 442 0.83 0.10989 0.00185 4.79419 0.08688 0.31643 0.00446 1798 15 1784 15 1772 22 101

fu49 282 1544 0.18 0.15925 0.00246 6.59934 0.11402 0.30060 0.00424 2448 13 2059 15 1694 21 145

fu55 503 505 1.00 0.05121 0.00171 0.34849 0.01157 0.04936 0.00081 250 47 304 9 311 5 80

fu60 635 762 0.83 0.05151 0.00149 0.27305 0.00802 0.03845 0.00060 264 39 245 6 243 4 109

fu70 758 527 1.44 0.05465 0.00156 0.30966 0.00895 0.04110 0.00064 398 38 274 7 260 4 153

fu76 321 295 1.09 0.10806 0.00191 4.66600 0.08874 0.31323 0.00450 1767 16 1761 16 1757 22 101

fu78 830 753 1.10 0.05258 0.00126 0.27430 0.00675 0.03784 0.00056 311 30 246 5 239 3 130

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Spot Th(ppm)

U(ppm) Th/U 207Pb/206Pb 1σ 207Pb/235U 1σ 206Pb/238U 1σ

207Pb/206Pbage (Ma) 1σ

207Pb/235Uage (Ma) 1σ

206Pb/238Uage (Ma) 1σ %conc

fu89 745 1037 0.72 0.06304 0.00194 0.14946 0.00455 0.01720 0.00027 63 193 106 9 108 2 58

fu90 434 411 1.06 0.05348 0.00269 0.15167 0.00744 0.02057 0.00038 349 77 143 7 131 2 266

fu91 419 760 0.55 0.05638 0.00127 0.44222 0.01018 0.05689 0.00081 467 27 372 7 357 5 131

fu94 333 165 2.02 0.16056 0.00294 9.01757 0.17347 0.40735 0.00585 2435 23 2386 24 2333 33 104

Sample: Zr3; Position: Shaobo (Well Shao x 14)

sh04 770 337 2.29 0.07217 0.00135 1.44543 0.02887 0.14534 0.00210 991 20 908 12 875 12 104

sh06 620 321 1.93 0.05118 0.00183 0.29859 0.01067 0.04233 0.00070 249 52 265 8 267 4 99

sh07 307 192 1.60 0.06897 0.00185 1.23840 0.03363 0.13030 0.00207 898 31 818 15 790 12 104

sh10 653 927 0.70 0.05455 0.00170 0.14792 0.00462 0.01968 0.00032 394 41 140 4 126 2 111

sh11 426 300 1.42 0.15382 0.00257 9.48698 0.17475 0.44763 0.00644 2389 14 2386 17 2385 29 100

sh14 1057 466 2.27 0.06591 0.00118 1.11363 0.02131 0.12257 0.00172 804 19 760 10 745 10 102

sh29 692 874 0.79 0.05504 0.00137 0.31101 0.00061 0.04097 0.00790 414 392 275 0.5 259 49 106

sh43 390 256 1.52 0.06634 0.00142 1.09417 0.02400 0.11956 0.00167 817 24 751 12 728 10 103

sh44 496 223 2.22 0.06399 0.00177 1.01939 0.02823 0.11549 0.00173 741 34 714 14 705 10 101

sh45 158 93 1.69 0.06397 0.00245 1.06487 0.04039 0.12067 0.00193 741 53 736 20 734 11 100

sh46 379 222 1.71 0.06474 0.00167 1.05036 0.02720 0.11762 0.00172 766 31 729 13 717 10 102

sh56 87 93 0.94 0.15342 0.00263 9.47946 0.16868 0.44818 0.00644 2384 14 2386 16 2387 29 100

sh57 319 201 1.58 0.04637 0.00366 0.22353 0.01741 0.03496 0.00068 17 134 205 14 222 4 92

sh63 263 229 1.15 0.11192 0.00182 5.06141 0.08773 0.32832 0.00442 1831 15 1830 15 1830 21 100

sh88 0 6 0 0.18689 0.01035 13.4384 0.70825 0.52142 0.01581 2715 48 2711 50 2705 67 100

sh89 521 324 1.60 0.08301 0.00200 1.51272 0.03640 0.13218 0.00192 1269 25 936 15 800 11 117

sh105 450 1977 0.23 0.11061 0.00136 4.39679 0.00371 0.28837 0.06226 1801 14 1711 14 1640 21 110

Sample: Zr4; Position: Huangyu (Well Huang 32)

h02 797 577 1.38 0.06000 0.00187 0.78127 0.02409 0.09446 0.00156 604 39 586 14 582 9 101

h04 2584 882 2.93 0.05390 0.00163 0.12292 0.00371 0.01654 0.00027 367 39 118 3 106 2 111

h17 432 388 1.11 0.33853 0.00738 35.1293 0.78445 0.75306 0.01120 3656 17 3642 22 3619 41 101

h21 457 223 2.04 0.07771 0.00176 1.63339 0.03760 0.15249 0.00228 1139 24 983 14 915 13 107

h32 188 101 1.85 0.10444 0.00220 4.18884 0.09135 0.29091 0.00443 1704 20 1672 18 1646 22 104

h33 268 365 0.73 0.05508 0.00194 0.41197 0.01427 0.05425 0.00092 415 47 350 10 341 6 103

h35 1495 742 2.02 0.05209 0.00132 0.31434 0.00805 0.04378 0.00065 289 32 278 6 276 4 101

h37 537 235 2.29 0.07171 0.00145 1.21195 0.02541 0.12260 0.00175 978 21 806 12 746 10 108

h40 140 1822 0.08 0.11260 0.00305 4.68453 0.13002 0.30181 0.00510 1842 27 1764 23 1700 25 108

h47 409 247 1.65 0.04904 0.00412 0.09924 0.00807 0.01468 0.00038 150 134 96 7 94 2 102

h49 81 69 1.17 0.05084 0.00440 0.26476 0.02229 0.03777 0.00098 234 143 238 18 239 6 100

h50 202 152 1.33 0.05719 0.00198 0.44664 0.01521 0.05665 0.00092 499 47 375 11 355 6 106

h67 422 188 2.25 0.07102 0.00164 1.18904 0.02799 0.12147 0.00181 958 25 796 13 739 10 108

h69 248 519 0.48 0.16117 0.00250 7.48833 0.12741 0.33713 0.00457 2310 79 2235 38 2153 28 107

h79 2833 624 4.54 0.06696 0.00162 1.21789 0.03018 0.13192 0.00202 837 27 809 14 799 12 101

h80 853 787 1.08 0.05701 0.00140 0.54283 0.01357 0.06907 0.00103 492 30 440 9 431 6 102

Table 1 (continued)


Table 2 Frequency data of zircon U-Pb ages for clastic rocks from the Dainan Formation in Gaoyou Sag

Sample CzMz Pz Pt3 Pt2 Pt1 Ar

K J T P C D S O ∈ Z Nh Qb Jx Ch

Zr1 0.0 5.2 6.2 11.3 10.3 12.4 1.0 2.1 1.0 0.0 0.0 5.2 1.0 0.0 1.0 30.9 12.4

Zr2 0.0 5.2 4.1 9.4 11.5 5.2 2.1 1.0 1.0 0.0 2.1 4.2 3.1 4.2 4.2 22.9 19.8

Zr3 0.0 1.0 3.0 3.0 6.0 2.0 0.0 1.0 2.0 0.0 1.0 19.0 6.0 2.0 3.0 39.0 12.0

Zr4 0.0 25.9 3.5 7.1 3.5 7.1 0.0 2.4 0.0 1.2 4.7 16.5 3.5 2.4 2.4 15.3 4.7

Note: The values in the table are zircon U-Pb measuring points percentage (%).

Cenozoic (Cz) zircons are absent in the study area (Ta-ble 2).

5 Discussion

5.1 Provenance comparison

A variety of rocks of the Early Mesozoic, Paleozoic and Neoproterozoic are exposed around the North Jiangsu Basin. Previous studies suggested that the sediments of the North Jiangsu Basin are mainly derived from five prov-enance regions since the Cretaceous: (1) the western Da-bie orogen and the east section of the Tan-Lu fault zone characterized by Proterozoic metamorphic and volcanic rocks; (2) the northeastern Binhai Uplift; (3) the north-western Sulu orogenic belt composed mainly of metamor-phic and igneous rocks; (4) the southwestern Zhangbaling Uplift with Neoproterozoic metamorphic rocks and Meso-zoic igneous rocks; (5) the southern Jiangdu and Ningzhen mountains characterized by Paleozoic-Early Mesozoic clastic and carbonate rocks (Shu et al., 2005). This paper will discuss how the bed rocks or intrusive rocks from the above peripheral large provenances affect the weathering deposits in the study area by the comparison of the REE pattern (Figure 5).

The Neoproterozoic high-potassium I-type granitic gneiss of the Jiaodong Section in the Sulu orogenic belt is characterized by the strong REE fractionation ((La/Yb)N=7.4-13.9) and the obviously negative Eu anomaly (δEu=0.47-0.61), similar to the granites in active conti-nental margins and clastic rocks of the Dainan Formation in the Gaoyou Sag (Xue et al., 2006; Figure 5a). Figure 5b shows that the REE distribution patterns of the mudstones from the Dainan Formation in the study area is very simi-lar to the granitic gneiss of Dabie Group in Dabie Orogen, which is characterized by a significant deficit of Eu with the ΣREE of 126-311 μg/g and LREE/HREE of 10.5 (Wu et al., 1998). In addition, the REE distribution patterns for

the Mesozoic-Cenozoic sandstones in the southeastern Dabie Orogen are coincident with the Proterozoic blues-chist belt of the Susong and Dabie groups in the southern Dabie Orogen, indicating the feasibility that the blueschist belt of the Susong Group and part of the Dabie Group had been denuded as a source in the Middle-Late Triassic (Li et al., 2005). Therefore, the provenance of the Dainan For-mation has genetic relationship with the Proterozoic low-grade metamorphic felsic igneous rocks in the Dabie-Sulu orogenic belt, with the parent rocks as the high-potassium I-type granitic gneiss.

The Zhangbaling Uplift is characterized by the Prote-rozoic epimetamorphic rocks with some Mesozoic igneous rocks, lying between the Dabie and Sulu orogens extend-ing along the Tan-Lu fault zone in a NNE direction (Fig-ure 2b). The Proterozoic Zhangbaling Group is exposed at the north section of the uplift, and the exposed south section of the uplift consists dominantly of the Archean-

Paleoproterozoic Feidong Group and the Neoproterozoic Zhangbaling Group. Feidong metamorphic complex be-longs to part of the Dabie-Jiaonan orogenic belt which is characterized by the occurrence of high-potassium calc-alkali granites. The REE distribution pattern (ΣREE 32.7-

161 μg/g, LREE/HREE 3.87-7.94, (La/Yb)N 2.45-6.38, δEu 0.62-0.97) of the upper part of the Zhangbaling Group composed mainly of spilite-quartz keratophyre series (also known as the blueschist), is obviously different from that in the study area (Guo and Wang, 1995; Figure 5c), which shows that the Neoproterozoic spilite-quartz keratophyre series in the Zhangbaling Uplift has had little impact on the study area. The lower part of the Zhangbaling Group is distinguished by greenschist-series metamorphic rocks with a small amount of blueschist. Given that the green-schist were primarily formed by blueschist through the ductile deformation and metamorphism in a high pres-sure, and relatively low oxygen fugacity environment, the greenschists widespread in the Zhangbaling region may be unlikely the provenance of the study area. Although there

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are a small amount of Mesozoic igneous rocks exposed in the Zhangbaling Uplift, previous studies on the Mesozoic igneous rocks in the northern Zhangbaling Uplift showed that, the REE distributions own similar ΣREE (112-126 μg/g) and LREE /HREE values (14-18) to those in the Gaoyou Sag, but present positive Eu anomalies; REE pat-terns of the igneous rocks in the southern section are simi-lar to those of the studied area with close δEu (0.53-0.74), whereas higher ΣREE (215-323 μg/g) and LREE/ HREE ratios (19-22) (Niu, 2006; Cao et al., 2010; Figure 5d). Therefore, the influence of the igneous rocks in the Zhang-baling Uplift on the deposits of the Dainan Formation in the Gaoyou Sag needs further detailed study, which will be discussed later.

Most exposed-rock masses in the middle Ningzhen Mountains are I-type intermediate-acidic granite, with the enrichment of LREE, the absence of Eu negative anoma-

ly, and occasionally a Ce negative anomaly in some rock masses (Zhang et al., 2012a). Therefore, the intrusive rocks in the Ningzhen Mountains have little influence on the source of sedimentary rocks of the Gaoyou Sag.

In summary, the sedimentary rocks of the studied Dain-an Formation were predominantly derived from the Pro-terozoic low-grade metamorphic rocks in the Dabie-Sulu orogenic belt, with the parent rocks as I-type high-potas-sium granitic gneiss. However, the Proterozoic blueschist belt in the Zhangbaling Uplift, the large-scale eclogite dis-tributed in the southern Dabie Orogen, and the Mesozoic intermediate-acid intrusive rocks widely distributed in the Ningzhen Mountains have negligible effect on the sedi-mentary rocks of the Gaoyou Sag.

5.2 Geochronology

It is noteworthy that this study simultaneously captured

Figure 5 Chondrite-normalised REE distribution patterns of studied rocks and the possible provenances surrounding the North Jiangsu Basin (Chondrite-normalised data from Taylor and McLennan, 1985). The shadow zones represent the REE distribution patterns of the Dainan Formation in the study area. a-High-potassium I-type granitic gneiss of the Sulu Orogen, with data from Xue et al., 2006; b-

Proterozoic granite gneiss in eastern Dabie Mountains with data from Wu et al., 1998; c-Neoproterozoic spilite-quartz keratophyre of Zhangbaling Uplift with data from Guo and Wang, 1995; d-Mesozoic intrusive rocks of Zhangbaling Uplift with data from Niu, 2006 and Cao et al., 2010.


the latest and oldest zircon grains in the Huangjue area. The zircon grain with the youngest age is subhedral and homogeneous with clear rhythm zonation, indicating a magmatic origin. Its age (94±2 Ma) suggests that the Late Cretaceous igneous rocks may have partly presented as a provenance in the study area. In addition, it also shows that the tectonic movements after the Late Cretaceous in the North Jiangsu Basin have not been significantly recorded in zircons, but are just characterized by the basin filling and sediment redistribution. The oldest zircon of this study belongs to metamorphic type with core-rim structure. The magmatic core gave an age of 3656±17 Ma, which cor-responds to the ancient detrital zircons (>3500 Ma, up to 3900 Ma) found in the sedimentary rocks in the Yangtze Craton, further confirming the existence of very old Early-Archean crust material in Yangtze Craton (cf., Jiao et al., 2009; Wang et al., 2013b). At the same time, a zircon with the age of 546±8 Ma is found in the Fumin region, corre-sponding to the global Pan-African orogenic event refer-ring to the close of the Mozambique Ocean, progressive polymerization of east and west Gondwana, and the even-tual formation of Gondwanaland (550-600 Ma; Lu et al., 2004). As a whole, zircons from the studied samples can be divided into four episodes based on their U-Pb ages, which reflect the multiple sources of the sedimentary rocks (Figure 6; Table 1).

1) 2450-2600 Ma (Paleoproterozoic-Neoarchaean): This period yields a weighted average age of 2516 Ma (N=49, MSWD=0.34), consistent with one of the main age peaks for the Yangtze Block basement (2500 Ma; She, 2007), which reveals the recycling of the Neoarchaean crystalline basement of the Yangtze Block in the prove-nance in the study area.

2) 1700-1900 Ma (Paleoproterozoic): The weighted average age for this period is 1855 Ma (N=74, MSWD=5.6). Since the Yangtze Block is characterized by the age peaks at 2500 Ma, 2000 Ma and 800 Ma and the absence of 1800-1900 Ma age peak, the zircons of this group are un-likely to be derived from the crystalline basement of the Yangtze Block (She, 2007). Although the Archean base-ment of the Yangtze Block is occasionally exposed (such as the Kongling complex), recent studies have showed that the Yangtze Block has the records of a 1800-2100 Ma tectonothermal event. This age group (1700-1900 Ma) is after the polymerization between the Yangtze Block and the Columbia Supercontinent that happened in 1900-2000 Ma (Peng et al., 2009), more close to the formation age of the mafic dikes (1850 Ma) in response to the regional extension found in the Kongling high-grade metamor-

phic body. This indicates the magmatism in the Yangtze Block may have occurred in relation with the breakup of the Columbia Supercontinent during the conversion period (about 1850 Ma) from the collision compression to exten-sion (Zhang et al., 2011).

3) 700-850 Ma (Neoproterozoic): The weighted aver-age age for this period is 789 Ma (N=33, MSWD=4.9). This age group corresponds to the dating results of the Ne-oproterozoic granitic gneiss in the Dabie-Sulu orogenic belt, which are mainly concentrated in the 700-800 Ma with a peak age of 750 Ma (cf., Zheng et al., 2006; Hu et al., 2010; Liu et al., 2012). Available studies suggested that the Neoproterozoic granitic magma event and associ-ated mafic magmatic events lasted from 780 Ma to 680 Ma in the south Dabie-Sulu ultrahigh pressure metamorphic belt, corresponding to the breakup of the Rodinia Super-continent and the 800-850 Ma orogenic event before the breakup (Xu et al., 2006; Hu et al., 2007).

4) 100-300 Ma (Mesozoic-Late Paleozoic): This group occupies the largest proportion of the zircons in the Gaoyou Sag. It can be further subdivided into three sub-groups. Firstly, the 100-200 Ma subgroup corresponds to the Jurassic-Cretaceous (Yanshanian period), with a weighted average age of 108.3 Ma (N=21, MSWD=3.0), consistent with the multi-period magmatic activity in the south section of the Zhangbaling Uplift (Niu et al., 2008). Secondly, the 200-250 Ma subgroup refers to the Late Permian-Triassic (Indosinian period), with a weighted av-erage age of 228 Ma (N=28, MSWD=3.4), in accordance with the formation age for the ultrahigh pressure metamor-phic rocks (225-240 Ma) in the Dabie-Sulu orogenic belt (Zheng, 2008), reflecting the Triassic collisional event be-tween South China and North China recorded in the study area (Liu et al., 2012). Thirdly, the 250-300 Ma subgroup corresponds to the Permian (late Hercynian period), with a weighted average age of 267 Ma (N=37, MSWD=1.6), corresponding to the first phase of the felsic magmatic activity (the end time of which is about 260 Ma) of the Emeishan large igneous province in the western margin of the Yangtze Block (Tao et al., 2008; Xu et al., 2008).

Combined with the regional tectonic evolution and sed-imentary history, the sediments of the Dainan Formation in the study area are mainly derived from the internal part of sedimentary basin (crystalline basement) and the recycled orogenic belts around the basin. That is to say, the sedi-ments are predominantly from the Neoarchaean-Paleo-proterozoic crystalline basement of the Yangtze Block and Neoproterozoic low-grade metamorphic basement of the Dabie-Sulu orogenic belt, with the parent rock as the

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high-potassium I-type granitic gneiss. The Mesozoic intru-sive rocks of the south Zhangbaling Uplift may have also provided a part of the sediments for the Dainan Formation.

6 Conclusions

Provenance comparative analysis of the REE shows that the provenance of the study area is mainly low-grade

metamorphic acidic igneous rocks of the Neoproterozoic basement in the Dabie-Sulu orogenic belt, and the specific parent rock type may be the high-potassium I-type granitic gneiss. Zircon U-Pb dating results show that the detrital zircons of the Dainan Formation in the North Jiangsu Ba-sin are dominated by magmatic zircons, and the ages could represent the crystallization age of their parent rocks. A small proportion of zircon grains belong to the hyperpla-

Figure 6 Frequency spectrum diagram of zircon U-Pb ages for clastic rocks from the Dainan Formation in Gaoyou Sag.


sia-mixed zircon, which indicates the provenance area had experienced multi-phase tectonic-thermal events. Zircons from the studied samples can be divided into four groups: (1) Neoarchaean-Paleoproterozoic (2450-2600 Ma), in-dicating the Yangtze Block crystalline basement existed in the study area; (2) Paleoproterozoic (1700-1900 Ma), in response to the breakup of the Columbia Superconti-nent, indicating the conversion process from the collision compression to extension of the Columbia Supercontinent may have occurred in the Yangtze Block in about 1850 Ma; (3) Neoproterozoic (700-850 Ma), in relation with the Neoproterozoic granitic gneiss in the Dabie-Sulu oro-genic belt and responding to the assembly and breakup of the Rodinia Supercontinent; (4) Late Paleozoic-Mesozoic (100-300 Ma), indicating that the provenances are igne-ous rocks formed by multi-stage magmatic activities in the south section of the Zhangbaling Uplift (100-200 Ma), the ultrahigh-pressure metamorphic rocks of the Dabie-

Sulu orogenic belt (200-250 Ma), and a few from the first phase of felsic magmatic activity of the Emeishan large ig-neous province in the western margin of the Yangtze Block (250-300 Ma).

Acknowledgements

Thanks are extended to Jian-Sheng Qiu, Xiao-Lei Wang, and Bing Wu of Nanjing University for their help in sample analysis and useful suggestions. Thanks are also given to the relevant staff of the Jiangsu Oilfield for pro-viding the borehole data.

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The development of Journal of Palaeogeography depends on support from scholars and specialists. Names of scholars and specialists as reviewers for Journal of Palaeogeography in year 2012-2013 are listed below (numbers in the brackets are reviewing times). Great gratitude is extended to them!

Specialists of non-Editorial-Committee-Members of Journal of Palaeogeography are presented 4 issues of year 2014 of the journal.

Wish all specialists and scholars happy new year and be healthy each day!Ekdale A. A. (1) Allen W. Archer (10) Markus Aretz (2) Gypsum Association (1)Gerhard H. Bachmann (4) Santanu Banerjee (6) Christian G. Betzler (9) Carsten Brauckmann (4)O. Catuneanu (1) Zhong-Qiang Chen (7) Mark Cloos (1) David (1)Hong-Wen Deng (1) Peter Druschke (6) Yuan-Sheng Du (1) Dai-Du Fan (6)Jia-Song Fan (2) Nian-Qiao Fang (1) Zeng-Zhao Feng (7) Margaret Lee Fraiser (4)Franz Theodor Fürsich (6) Lin-Zhi Gao (2) Elizabeth Gierlowski-Kordesch (1)Wei-Gang Kong (1) Yi-Ming Gong (2) Ying-Hai Guo (1) Guo-Qi He (1)Qi-Xiang He (2) You-Bin He (1) Jason Hilton (5) Mikael Hook (1)Bin Hu (1) Xiu-Mian Hu (2) Bao-Qi Huang (1) Si-Jing Huang (2)Gan-Qing Jiang (3) Zai-Xing Jiang (2) Zhen-Kui Jin (1) Nemeth Karoly (1)Steve Kershaw (4) Wei-Gang Kong (1) Cheng-Sen Li (1) Cong-Xian Li (1)Hai-Bing Li (1) Jing-Yi Li (1) Ben-Pei Liu (3) Chi-Yang Liu (1)Chun-Lian Liu (1) Hao Liu (2) Jian-Bo Liu (6) Yong-Qing Liu (2)Spencer G. Lucas (5) Vinicio Manzi (1) Moretti Massimo (1) Ming-Xiang Mei (3)Tadeusz Peryt (6) Fotini A. Pomoni (1) Paul Robinson (1) Subir Sarkar (2)Patrick M. Shannon (1) Long-Yi Shao (3) Graham Shields-Zhou (4) Ian D. Somerville (4)Christopher J. Stevenson (1) Carl W. Stock (1) De-Chen Su (3) Xiao-Meng Sun (1)Zuo-Yu Sun (1) Hao-Wen Tong (2) A. J. (Tom) van Loon (8) John J. Walsh (1)Xiao-Qiao Wan (1) Jian Wang (1) Ping Wang (4) Ya-Ping Wang (1)Yong-Biao Wang (2) Adam D. Woods (6) Gen-Yao Wu (1) Ya-Sheng Wu (1)Yin-Ye Wu (1) Qing-Hai Xu (1) Xiao-Song Xu (2) Jin-Zhuang Xue (2)Shou-Ren Yang (6) Wan Yang (7) Ezaki Yoichi (5) Chuan-Heng Zhang (1)Jin-Chuan Zhang (1) Mi-Man Zhang (1) Jing-Quan Zhu (1) Mao-Yan Zhu (1)

provenance records of the north jiangsu basin, east … and to reconstruct the coupled relation...

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