Provenance analysis of the late Mesoproterozoic to Neoproterozoic Xuhuai Basin in the southeast North China Craton: Implications for paleogeographic reconstruction

Journal Pre-proofs Provenance analysis of the late Mesoproterozoic to early Neoproterozoic Xuhuai Basin in the southeast North China Craton: Implications for paleogeographic reconstruction Fengbo Sun, Peng Peng, Xiqiang Zhou, A. J. C. Magalhaes, F. Guadagnin, Xiaotong Zhou, Zhiyue Zhang, Xiangdong Su PII: DOI: Reference:

S0301-9268(19)30013-0 https://doi.org/10.1016/j.precamres.2019.105554 PRECAM 105554

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Precambrian Research

Received Date: Revised Date: Accepted Date:

12 January 2019 8 November 2019 2 December 2019

Please cite this article as: F. Sun, P. Peng, X. Zhou, A. J. C. Magalhaes, F. Guadagnin, X. Zhou, Z. Zhang, X. Su, Provenance analysis of the late Mesoproterozoic to early Neoproterozoic Xuhuai Basin in the southeast North China Craton: Implications for paleogeographic reconstruction, Precambrian Research (2019), doi: https://doi.org/ 10.1016/j.precamres.2019.105554

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1

Provenance analysis of the late Mesoproterozoic to early

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Neoproterozoic Xuhuai Basin in the southeast North China

3

Craton: Implications for paleogeographic reconstruction

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Fengbo Suna,b, Peng Penga,b,*, Xiqiang Zhouc, A. J. C. Magalhaesd,e, F. Guadagninf,

5

Xiaotong Zhoua,b, Zhiyue Zhanga,b, Xiangdong Sua,b

6

a

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Chinese Academy of Sciences, Beijing 100029, China

8

b

9

Sciences, Beijing 100049, China

State Key Laboratory of Lithospheric Evolution, Institute of Geology and Geophysics,

College of Earth and Planetary Sciences, The University of Chinese Academy of

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c

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Geophysics, Chinese Academy of Sciences, Beijing 100029, China

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dInstituto

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Grande, 1749-016 Lisboa, Portugal

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e

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f Universidade

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* Corresponding author

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Corresponding e-mail address: [email protected]

Key Laboratory of Petroleum Resource Research, Institute of Geology and

Dom Luiz (IDL), Faculdade de Ciências, Universidade de Lisboa, Campo

Universidade Federal do Rio Grande do Norte, Natal, Brazil Federal do Pampa Campus, Pedro Anunciação 111, 96570-000, Brazil

18 19 20 21 22 23 24 25 26 27 28 29 1

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Abstract:

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The late Mesoproterozoic to early Neoproterozoic sedimentary rocks in the southeast

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North China Craton (NCC) are significant in paleogeographic reconstruction. An

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integrated approach of field investigation, detrital zircon U-Pb dating, and Lu-Hf

34

isotope analysis reveals essential information on the tectonic-sedimentary evolution of

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the Xuhuai Basin. New age constraints show that the Xuhuai Basin comprises a lower

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(Huaihe Group, 1.1-0.9 Ga) and an upper (Langan Group, <0.82 Ga) successions,

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with an unconformity between them. The depositional age of the middle to upper part

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of the Huaihe Group (the Niyuan-Wangshan Formations) is limited to 0.97-0.89 Ga.

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A comparison of regional basin formations suggests that the Xuhuai, Jiaolai, Dalian,

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and Pyongnam basins belong to the same rift system (the Xuhuai rift system). There

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was a distinct provenance change from ~2.7-2.5 Ga, ~2.1 Ga and ~1.9 Ga rocks

42

(zircon ages) in the lower part, to 1.8-1.0 Ga in the middle-upper part of the Huaihe

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Group, and back to ~2.7-2.5 Ga, ~2.1 Ga and ~1.9 Ga rocks in the Langan Group. The

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~2.7-2.5 Ga, ~2.1 Ga, ~1.9 Ga, and ~1.8-1.4 Ga provenances could be from the NCC,

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while the 1.2-1.0 Ga provenances were possibly from the Baltica which could be far

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or closely neighbored the NCC in the north before 0.9 Ga. While the 1.4-1.3 Ga

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provenance possibly supports a North China-São Francisco-Congo connection

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hypothesis, in which the Early Neoproterozoic basins such as the Xuhuai rift basins

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along the southeastern margin of the NCC, the coeval basins along the eastern and

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western margins of the São Francisco Craton and the west Congo Craton comprise a

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correlated rift system during 1.1-0.9 Ga.

52 53

Keywords: Late Mesoproterozoic-Neoproterozoic; North China Craton; São

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Francisco–Congo Craton; Xuhuai Basin; Provenance; Paleogeography

55 56 57

2

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1 Introduction

59

Supercontinent cycles and their responses in old cratons are important research

60

topics in Precambrian geology. Recently, there has been a concerted effort to unravel

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the structure and paleogeographic evolution of Proterozoic supercontinents. From ca.

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1.9 to 0.9 Ga, two supercontinents occurred in Earth’s history, the Columbia and

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Rodinia supercontinents (Zhao et al., 2003; Li et al., 2008). Most cratons have

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participated in the Rodinia supercontinent (Li et al., 2008; Cawood et al., 2016;

65

Merdith et al., 2017, and references therein). However, the North China Craton (NCC)

66

has few igneous or orogenic events which are typically related to the evolution of the

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Rodinia supercontinent (Li et al., 2013, and references therein), limiting the

68

understanding of the NCC position within Rodinia. The contrary occurs in respect to

69

the NCC participation in the Columbia supercontinent, which is well-reported (Zhao

70

et al., 2002; Zhao et al., 2003, 2009; Zhang et al., 2009, 2012, 2017; He et al., 2009;

71

Meng et al., 2011; Wang et al., 2014).

72

During the late Mesoproterozoic to early Neoproterozoic eras, a series of

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sedimentary basins developed along the southeast margin of the NCC, which includes

74

the Pyongnam Basin in the Korean peninsula, the Jiaolai Basin in the Shandong

75

peninsula, the Dalian Basin in the Liaoning peninsula, and the Xuhuai Basin at the

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conjunction of the Jiangsu and Anhui provinces (Fig. 1a). These basins record the

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source area denudation and the evolution of the sedimentary environments, thus are

78

essential to unravel the paleography in the time interval of the deposition. Sills

79

intruding those basins as well as coeval mafic dikes in the inland of the craton have

80

been proposed to form a large igneous province at ca. 0.9 Ga (Peng et al., 2011a,

81

2011b; Wang et al., 2012; Zhang et al., 2016; Su et al., 2018; Zhu et al., 2019).

82

The dating of the deposition in such a setting is hampered by the absence of

83

fossil assemblages and volcanic beds. The dating of detrital zircons can help to

84

determine the maximum depositional ages, which can be coupled to the minimum

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depositional ages to define a depositional age interval (e.g. Gehrels, 2014). The U-Pb

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ages of the detrital zircons also provide information on the age of the source rocks (e.g. 3

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Griffin et al., 2004; Luo et al., 2006; Yang et al., 2012; Hu et al., 2012; Itano et al.,

88

2016); while Hf isotopes indicate the mantle or crustal origin of the source rocks (e.g.

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Wu et al., 2006; Yang et al., 2012; Hu et al., 2012; Liu et al., 2017). In this work, we

90

use the stratigraphic record and U-Pb and Hf isotopes of zircon grains in the Xuhuai

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Basin in the southeast margin of the NCC to decipher the early Neoproterozoic

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paleogeographic configuration of the craton and discuss its implications for the Rodinia

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supercontinent.

94 95

2 Geological setting

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The basements of the NCC were consolidated after two major tectonic events at

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~2.5 Ga and ~1.9 Ga (Zhai and Bian et al., 2000; Zhao et al., 2001, 2003, 2008; Kusky

98

et al., 2003; Yang et al., 2003; Wilde et al., 2005; Guo et al., 2005; Santosh, 2010; Wan

99

et al., 2011; Liu et al., 2015; Liu et al., 2018). In the southeast NCC, basement

100

associations include a 2.7-2.5 Ga metamorphic supracrustal rocks and granites and the

101

late Paleoproterozoic Jiao-Liao-Ji belt, which mainly contain 2.3-2.1 Ga

102

volcano-sedimentary sequences which were subjected to high-pressure metamorphism

103

and granitic intrusions at ~1.9 Ga (Meng et al., 2013; Xie et al., 2014; Liu et al., 2015;

104

Liu et al., 2018).

105

From ca. 1.9 to 0.9 Ga, the NCC evolved into a stable continental crust with

106

periodical basin formations (Zhai et al., 2015). Thick late Mesoproterozoic to early

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Neoproterozoic sedimentary record is preserved in the Pyongnam, Jiaolai, Dalian, and

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Xuhuai basins in the southeast NCC. These late Mesoproterozoic to Neoproterozoic

109

basins have a distinct SW-NE trend and comprise the Sangwon system in the

110

Pyongnam Basin, Yongning -Wuxingshan-Jinxian Groups in the Dalian Basin, Penglai

111

and Tumen Groups in the Jiaolai Basin, and Huaihe-Langan/Huainan-Feishui Groups

112

in the Xuhuai Basin (Fig. 2). These basins are separated from each other by the

113

Phanerozoic Tan-Lu fault and some geographic features such as the Bohai Bay (Fig.

114

1a). This study is focused in the Xuhuai Basin which is located on the west flank of the

115

Tan-Lu fault (Fig. 1a), and possibly extends into western Shandong province (BGMRJ, 4

116

1984; BGMRA, 1985, 1987; BGMRS, 1991; Fig. 1b).

117 118

3 Stratigraphic record of the Xuhuai Basin

119

The fill of the Xuhuai Basin, namely the Xuhuai sequence, is exposed in the

120

Huaibei and Huainan regions, separated by the E-W elongated Bengbu basement high

121

(Fig. 1b). The composed stratigraphic columns of the Xuhuai sequence in the two

122

regions are summarized in Fig. 2, based on published and field derived information.

123 124

3.1 The Huaibei region

125

The Xuhuai sequence in the Huaibei area comprises the Huaihe and Langan

126

Groups. The Huaihe Group is composed of the Lanling, Xinxing, Chengshan, Jiayuan,

127

Zhaowei, Niyuan, Jiudingshan, Zhangqu, Weiji，Shijia, and Wangshan Formations,

128

and the Langan Group consists of the Jinshanzhai and Gouhou Formations (Fig. 2).

129

The Huaihe Group is divided into three siliciclastic–carbonate successions, the

130

Lower, Middle, and Upper Huaihe Group. The Lower Huaihe Group is comprised of

131

the Lanling and Xinxing Formations.The Lanling Formation is characterized by thick-

132

to medium-bedded, coarse- to medium-grained quartzose sandstone with low angle

133

bi-directional cross-beddings, probably indicating a tidal environment (Fig. 3a,b). The

134

thickness of the Lanling Formation ranges from <40 m in the basin margin to ~500 m

135

in the basin center (BGMRJ, 1987). The Xinxing Formation is conformable overlying

136

the Lanling Formation. It comprises light greenish/ yellowish thin-bedded carbonate

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mudstone, mixed carbonate-siliciclastic units, and sandstone interlayered to carbonate

138

(Fig. 3c). The Xinxing Formation is tens of meters thick at the basin margin up to

139

~500 m thick at the basin center. Previous studies suggested that the lower member of

140

the Xinxing Formation is formed in a carbonate ramp depositional system (Wang,

141

2009), succeeded by a basinal shoreface environment for the upper member (BGMRA,

142

1985; Wang, 2009). The maximum depositional age for the Xinxing Formation is ca.

143

1.12 Ga (Yang et al., 2012). 5

144

The Middle Huaihe Group is ~2,000 m thick and includes the siliciclastic and

145

carbonate succession of the Chengshan, Jiayuan, Zhaowei, Niyuan, Jiudingshan and

146

Weiji Formations (Fig. 2). The Chengshan Formation conformably overlies the

147

Xinxing Formation and is composed of medium-grained quartzose sandstone with

148

parallel and low-angle cross bedding at the base (BGMRJ, 1984), and alternating

149

medium to thin layers of mudstone, shale and sandstone to the top (Fig. 3d). The

150

Chengshan Formation is interpreted as formed in a tidal depositional system (BGMRJ,

151

1997; Wang, 2009). The conformably overlying Jiayuan Formation is ∼450 m thick

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and consists of silty limestone, carbonate mudstone and shale deposited in a deep

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carbonate ramp (Fig. 3e,f). The Zhaowei Formation conformably overlies the Jiayuan

154

Formation and is composed of carbonates with molar tooth structures and stromatolite

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in the lower part, and thin-bedded limestone with interbedded calcareous mudstone in

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the upper part, deposited in a carbonate ramp (Fig. 3g-h). The Niyuan, Jiudingshan,

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Zhangqu, and Weiji Formations are suggested to be deposited in carbonate platform

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(Wang, 2009; Ma, 2015). The Niyuan Formation consists of thick-bedded dolostone,

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dolomitic limestone. The Jiudingshan Formation is separated from the Niyuan

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Formation by a particular unit of intraclastic coarse-grained dolostone. The

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Jiudingshan Formation consists of thick-bedded stromatolitic dolostone. The

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succeeding Zhangqu Formation consists of one meter-thick intraclastic carbonate at

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the base, succeeded by thin-bedded mudstone and medium-bedded microcrystalline

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dolostone. The Weiji Formation conformably overlying the Zhangqu Formation,

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consists of medium-bedded dolostone succeeded by thick-bedded stromatolitic

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dolostone in the upper part (Cao et al., 1985).

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The Upper Huaihe Group is comprised by the Shijia and Wangshan Formations.

168

The Shijia Formation is characterized by siltstone (Fig. 3i), calcareouse shale, and

169

grainstone (Fig. 3j), deposited in a restricted shelf (Wang, 2009). The Wangshan

170

Formation consists of thin- to medium-bedded

171

with chert bands, stromatolites, and molar tooth structures, indicating an environment

172

of restricted carbonate platform (Fig. 3k, l). New detrital zircon U-Pb ages of

173

sandstone from the Shijia Formation has established a maximum deposition age of ca. 6

dolomiteic limestone and dolostone

174

950 Ma (He et al., 2017). Both the Shijia and Wangshan Formations are intruded by

175

abundant diabase sills and dikes with ages ranging from 918 to 890 Ma (Liu et al.,

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2006; Wang et al., 2012; Cai et al., 2018; Zhu et al., 2019). The age constraints

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indicate that deposition of the upper Huaihe Group occurred from ca. 950 to 900 Ma.

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A significant unconformity separates the Huaihe and Langan Groups (Fig. 3m).

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The Langan Group consists of the Jinshanzhai Formation and the Gouhou Formation

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(Wan et al., 2019). The Jinshanzhai Formation consists of cherty conglomerate in the

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basal part (Fig. 3m) succeeded by calcareous shale and mudstone interbedded with

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glauconitic quartzose sandstone in the lower member. The upper member of the

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Jinshanzhai Formation is comprised by reddish stromatolitic limestone (Fig. 3n) and

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greenish, thin to medium bedded carbonate shale at the topmost part (Fig. 3o). The

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Gouhou Formation is comprised of greenish/reddish sandstone and shale. The Langan

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Group was deposited in a tidal depositional system (BGMRA, 1985). There is no

187

general agreement regarding the depositional age of the Jinshanzhai and Gouhou

188

Formations. The youngest detrital zircon grains in the Jinshanzhai Formation

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sandstones have an average age of 925 ± 10 Ma (n = 8) and 825 ± 11 Ma (n = 4)

190

(Yang et al., 2012). Based on the chemo- and biostratigraphy, Xiao et al. (2014)

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suggested that the Gouhou Formation is deposited during the early-middle Tonian

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period and is chronocorrelated with the Bitter Springs δ 13 excursion (0.8-0.7 Ga,

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Macdonald et al., 2010; Rooney et al., 2014). Tang et al. (2015) reported the

194

occurrence

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Trachyhystrichosphaera aimikasome, in the Gouhou Formation. Recently, the

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Gouhou Formation was redefined as its traditional Lower Member, and the

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Middle-Upper members were included in the Houjiashan Formation based on

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youngest detrital zircon age population (Wan et al. 2019). In this study, the new

199

definition of Gouhou Formation proposed by Wan et al. (2019) is adopted.

of

early

Tonian

index

fossil,

acanthomorphic

acritarch

200 201 202

3.2 The Huainan region The sedimentary record in the Huainan region consist of the Huainan and Feishui 7

203

Groups (Xiao et al., 2014), which overlie the Paleoproterozoic Fengyang Group. The

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two groups are further subdivided into Caodian, Bagongshan, Liulaobei, Shouxian,

205

Jiuliqiao, Sidingshan Formations from the bottom up (Fig. 2).

206

The Huainan Group is dominated by siliciclastic strata. The Caodian Formation

207

is composed mainly of conglomerate (Fig. 4a) with minor massive coarse sandstone

208

(Fig. 4b) deposited in an alluvial depositional system. The Bagongshan Formation

209

consists of lower conglomerate succeeded by quartzose sandstone deposited in a

210

coastal depositional system (Wang, 2009; Fig. 4c). The Bagongshan Formation occurs

211

over the Fengyang Group and the Caodian Formation. The Liulaobei Formation

212

conformably overlies the Bagongshan Formation and is composed of thin- to

213

medium-bedded mudstone interbedded with calcareous shale succeeded by thin- to

214

medium-thick layers of calcareous shale, fine-grained quartzose sandstone (Fig. 4d),

215

and grainstone. The Liulaobei Formation is supposed to be deposited in a shelf

216

depositional system (Wang, 2009). The Bagongshan and Liulaobei Formations are

217

suspected to be lateral equivalents to the Lanling and Xinxing Formations,

218

respectively (Liu et al., 2005; Wang, 2007).

219

The Feishui Group consists of the Shouxian, Jiuliqiao, and Sidingshan

220

Formations. The Shouxian Formation conformably overlies the Liulaobei Formation

221

and consists of 20 to 190 m thick thin stratification of calcareous quartz sandstone and

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siltstone (Fig. 4e,f), which is suggestive of a shore depositional environment. The

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conformably overlying Jiuliqiao Formation is 26 to 119 m thick and consists of

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thin-bedded argillaceous limestone and calcareous mudstone, stromatolite with thin

225

siltstone interbeds. The overlying Sidingshan Formation is about 300 m thick and it is

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composed of stromatolitic dolostone with cherty bands and nodules (Cao et al., 1985).

227

Abundant columnar stromatolite is consistent with a carbonate platform depositional

228

environment (Xiao et al., 2014).

229

The Neoproterozoic sedimentary successions in Huainan region have been dated

230

on the basis of age diagnostic fossils, whole rock K-Ar method on glauconite grains,

231

and whole-rock Rb-Sr method on shale. Depositional age was suggested to be

232

constrained between ca. 1.0 and 0.6 Ga (BGMRA, 1985). Detailed descriptions of the 8

233

stratigraphy in the Huainan region have been given by BGMRA (1985).

234 235

4 Samples and analytical methods

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4.1 Samples

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Four samples were collected for detrital zircon grain concentration (sampling

238

locations are shown in Fig. 1b). Three samples are sanstones and one sample is a silty

239

mudstone. Samples were collected in the Dawushan area of the Huainan region and in

240

the Chulan-Langan area of the Huaibei region. Sample DWSH-2 is a coarse-grained

241

quartzose sandstone, collected from the Bagongshan Formation in the Dawushan

242

outcrop (Fig. 5a; coordinates N32°43′39.68″, E117°25′13. 97″). Sample XZZ-1 is a

243

fine-grained quartzose sandstone collected from the Shouxian Formation, ~2 km south

244

to the Guankou Reservoir (Fig. 5b; coordinates N32 ° 42 ′ 3.78 ″ , E117 ° 23 ′ 28.90 ″ ).

245

Sample PSH-1 is a silty-claystone collected from an interlayer of the Niyuan Formation,

246

east Houcheng Village (coordinates N33 ° 58 ′ 17.84 ″ , E117 ° 19 ′ 20.93 ″ ). Sample

247

P2-JSZ-1 is a medium-grained sandstone collected from the Jinshanzhai Formation,

248

north Jinshanzhai village (Fig. 5c; coordinates N33°54′59.08″, E117°17′3.48″).

249 250

4.2 Analytical methods

251

4.2.1 Zircon U-Pb isotopes

252

Fresh portions of the samples were powdered and sieved at 80-mesh. Minerals

253

were extracted using conventional heavy liquid and magnetic methods. Zircons were

254

handpicked under a binocular microscope and were subsequently mounted on

255

adhesive tape alongside standard zircon 91500. Samples were enclosed in epoxy resin

256

and polished 1/3 to 1/2. Cathodoluminescence images (CL) of zircons were obtained

257

to unravel internal structures and identification of suitable dating targets for

258

LA-(MC)ICP-MS analysis.

259

U-Pb zircon analyses were made by LA-ICP-MS at the Sample Solution

260

Analytical Technology Co., Ltd., Wuhan, China. Laser sampling was performed using 9

261

a GeolasPro laser ablation system that consists of a COMPexPro 102 ArF excimer

262

laser (wavelength of 193 nm and maximum energy of 200 mJ) and a MicroLas optical

263

system. An Agilent 7700e ICP-MS instrument was used to acquire ion-signal

264

intensities. The diameter of the spot and laser frequency were set to 24 µm and 5 Hz,

265

respectively. Each analysis incorporated a background acquisition of approximately

266

20 s followed by 50 s of sample data acquisition. GJ1, 91500, and TEM-Ⅱ zircons, as

267

well as glass NIST SRM 610, were used as external reference standards for U-Pb

268

dating. The 91500 standard was analyzed twice every 5-10 sample analyses. An

269

Excel-based software ICPMSDataCal 11.8 was used to perform off-line selection and

270

integration of background and analytic signals, time-drift correction, and quantitative

271

calibration for trace element analysis and U-Pb dating (Liu et al., 2010). Concordia

272

diagrams were constructed using Isoplot 3.7 (Ludwig, 2008). The U-Pb data with trace

273

element U and Th contents are listed in Supplementary Table 1.

274 275

4.2.2 Zircon Hf isotopes

276

In situ zircon Hf isotope analysis was carried out at the Sample Solution

277

Analytical Technology Co., Ltd., Wuhan, China, using a Geolas-193 laser-ablation

278

microprobe, attached to a Neptune Plus multi-collector (MC) ICP-MS. Spots for Hf

279

analysis were undertaken on the same CL domain and as closely as possible to the

280

U-Pb analysis spots. The ablation protocol employed a spot diameter of 32 µm. The

281

typical ablation time was about 30 seconds for 200 cycles of each measurement.

282

External calibration was performed by measuring zircon standard 91500, GJ-1, and

283

TEM-Ⅱ to evaluate the reliability of the analytical data. The standard sample zircon

284

91500 was analyzed twice every 5-10 sample analyses. The reference zircon (91500)

285

provided

286

agreement with the recommended value of 0.282305 (Wu et al., 2006). The reference

287

TEM-Ⅱ provided

288

with the recommended 176Hf/177Hf ratio of 0.282680±24 (2σ, Woodhead et al., 2004).

289

The TEM-Ⅱ instrumental conditions and data acquisition were described by Wu et al.

176Hf/177Hf

ratio of 0.2823033±17 (2σ, n=186). This value is in good

176Hf/177Hf

ratio of 0.282668±4 (2σ, n=46), which is in agreement

10

176Hf/177Hf

=0.282772 and

176Lu/177Hf

290

(2006). The present-day chondritic ratios of

=

291

0.0332 (Blichert-Toft and Albarède, 1997) were adopted to calculate εHf(t) values.

292

Raw data were processed using the ICPMSDataCal 11.8 (Liu et al., 2010).

293 294

5 Results

295

5.1 U-Pb zircon ages

296

370 U-Pb zircon ages were obtained. Individual zircon ages with less than 10%

297

discordance were used, the remaining were rejected. For zircon grains older than 1.0 Ga,

298

207Pb/206Pb

299

younger than 1.0 Ga.

ages are chosen; whereas

206Pb/238U

ages were chosen for zircon grains

300 301

5.1.1 Quartzose sandstone of the Bagongshan Formation (sample DWSH-2)

302

More than 800 zircon grains were separated from sample DWSH-2. They are

303

mainly ~100 μm in size. One hundred analytical spots on randomly selected grains were

304

analyzed. In CL images, most of them are elongated, subhedral, and rounded to

305

sub-rounded external shape. Zircon grains have oscillatory zoning internal structure

306

(Fig. 6a) indicating a magmatic source, along with the Th/U ratios between 0.22 and

307

1.53 (c.f. Koschek, 1993; Hanchar and Hoskin, 2003). Ninety-six zircon grains are

308

concordant. The ages are mainly late Archean and Paleoproterozoic, ranging from

309

2,787 Ma to 1,729 Ma (Fig. 7a,c). The main zircon age population is ca. 1.9 Ga (59% of

310

concordant grains) and the second is ca. 2.1 Ga (20%).

311 312

5.1.2 Quartzose sandstone of the Shouxian Formation (sample XZZ-1)

313

Zircon grains from Sample XZZ-1 are mainly ~50-100 μm in size. In CL images,

314

the zircons show oscillatory zoning, core-rim structure, and slab-like zoning (Fig. 6b).

315

Most of them are rounded and have some solution depressions. Their Th/U ratios range

316

from 0.28 to 1.50, with an average of 0.77, indicating a magmatic origin. A total of 87 11

317

zircon grains are concordant from 100 randomly analyzed. Zircon grains are aged from

318

2,739 Ma to 1,098 Ma (Fig. 7b,d). Zircon grains are mostly formed at ca. 1.5 Ga and

319

other secondary or inconspicuous populations are aged ca. 1.2 Ga, 1.65 Ga, 1.9 Ga, and

320

2.7 Ga.

321 322

5.1.3 Silty-mudstone of the Niyuan Formation (sample PSH-1)

323

The sizes of the zircon grains in Sample PSH-1 are relatively small, mostly at ~50

324

μm or smaller. They are well rounded and present solution depressions and cracks. (Fig.

325

6c). Eighty spots randomly selected from over 300 zircon grains were dated, and 75

326

spots are effective after filtration. Age population ranges from 2621 Ma to 936 Ma. The

327

Mesoproterozoic zircon grains exhibit six age populations close to 1.74 Ga, 1.56 Ga,

328

1.43 Ga, 1.29 Ga, 1.18 Ga, and 0.97 Ga (Fig. 7e,g),.

329 330

5.1.4 Quartzose sandstone of the Jinshanzhai Formation (sample P2-JSZ-1)

331

Zircon grains from sample P2-JSZ-1 are mainly ~100 μm in size. They are

332

rounded, stubby or subhedral with oscillating zonning (Fig. 6d), indicating a magmatic

333

origin. This interpretation is also confirmed by their high Th/U ratios (averaged 0.59).

334

83 of 90 randomly selected spots are selected. The grain ages occur in four main

335

populations, close to 1.02 Ga, 1.22 Ga, 1.55 Ga, and 2.04 Ga (Fig. 7f,h).

336 337 338 339

5.2 Zircon Lu-Hf isotopes The Hf isotope test was failed for Sample PSH-1 for too small sizes. The data of the other three samples are shown in Supplementary Table 2.

340

Zircons from the Bagongshan Formation (sample DWSH-2) have εHf(t) values

341

ranging from -12.5 to +6.0 (Fig. 8a)and TDMC(Hf) ages ranging from 2.3 Ga to 3.2 Ga

342

(Fig. 8d). Zircon grains can be divided into two groups: low εHf(t) values (-12.6 to -5.0)

343

for the ~1.9 Ga zircons with older TDMc(Hf) ages (2.8-3.0 Ga), and high εHf(t) values 12

344

(-5.0 to +1.2) for the older zircons with younger TDMc(Hf) ages (2.5-2.7 Ga).

345

Zircons from the Shouxian Formation show the εHf(t) values ranging from -8.2 to

346

+11.9 (Fig. 8b). Their TDMC ages range from 1.4 Ga to 3.3 Ga and are mainly at ~1.4 to

347

2.0 Ga and ~2.5 Ga (Fig. 8e). Most εHf(t) values of zircons are positive and close to the

348

evolution line of depleted mantle.

349

The εHf(t) values of the zircons from the Jinshanzhai Formation range from -12.8

350

to +10.6, mainly distributed between -5 and +8 (Fig. 8c). Zircon grains can be divided

351

into two groups. The εHf(t) values of the zircons with 1.0-1.5 Ga U-Pb ages are mainly

352

positive. However, the εHf(t) values of ~2.1 Ga zircons are mainly clustered at 0, with

353

TDMC ages clustered at ~2.5 Ga. Some grains also show evidence of TDMc(Hf) age >2.7

354

Ga (Fig. 8f).

355 356

6 Discussion

357

6.1 Depositional ages

358

Our new age results reveal the youngest zircon ages at ~0.97 Ga for the silty

359

argillite (Sample PSH-1, Fig. 9d) of the Niyuan Formation, which represents its

360

maximum deposition age. Besides, zircon ages from the sills within the Niyuan

361

Formation constrain a minimum depositional age of ca. 0.93 Ga (Gao et al., 2009).

362

Integration with published detrital zircon ages (Yang et al., 2012; He et al., 2017), it is

363

suggested that the Huaihe Group in the Huaibei region was successively deposited

364

during ~1.1-0.9 Ga, with the middle-upper portion (Niyuan-Wangshan Formations)

365

deposited during 0.97-0.9 Ga. The detrital zircon grains from the Jinshanzhai

366

Formation indicate a maximum depositional age of ~819 Ma (Fig. 9f). This indicates a

367

nearly 100 Ma sedimentary hiatus (unconformity) between the Wangshan Formation

368

(of the Huaihe Group) and the Jinshanzhai Formation (of the Langan Group).

369

The youngest zircon ages for the Bagongshan and Shouxian Formations in the

370

Huainan region are ~1.8 Ga and ~1.1 Ga, respectively (Fig. 9a,c). We take the ~1.1 Ga

371

age as a close estimation of the maximum deposition of the succession in the Huainan

372

region and relate the ~1.8 Ga zircon grains as a result of older provenance in the source 13

373

area. This agrees with the result of the stratigraphic analyses that the Huainan and

374

Feishui Groups in the Huainan region are equivalent to the Lower to Middle parts of

375

the Huaihe Group in the Huaibei section.

376 377

6.2 Provenance analysis

378

Ages of detrital zircons of the Bagongshan Formation (DWSH-2) are mainly

379

Neoarchean–Paleoproterozoic. Zircon ages are ~2.7-2.5 Ga, ~2.1 Ga, and ~1.9 Ga (Fig.

380

9a). Ages of the ~2.7-2.5 Ga is related to the major crustal growth events in the NCC

381

(Wilde et al., 2005; Lu et al., 2008). Ages of ~2.1 Ga and ~1.9 Ga represent the ages of

382

the Paleoproterozoic meta-volcanic rocks and granitic intrusions (Li et al., 2007; Yang

383

et al., 2009; Xie et al., 2014; Liu et al., 2015; Song et al., 2016). The

384

Neoarchean–Paleoproterozoic zircon grains, which are mainly documented in the

385

lower near-shore sandstone, are most likely derived from local basement. This is

386

further confirmed by their low εHf(t) values (c.f. Wan et al., 2015).

387

The most abundant zircon populations of the Shouxian Formation (XZZ-1) are

388

shifted to the Mesoproterozoic grains of 1.8-1.2 Ga in age, although with a few

389

Paleoproterozoic ages (Fig. 9c). The remarkable ~1.5 Ga age population is slightly

390

different from that of the Bagongshan Formation. The 1.8-1.6 Ga grains match the

391

~1.78 Ga Xiong’er volcanic rocks (Zhao et al., 2002; He et al., 2009; Zhao et al., 2009;

392

Wang et al., 2010) and Taihang dike swarms (Peng et al., 2005, 2007), as well as the

393

1.8-1.6 Ga anorogenic granites, diorites, and dikes in the southern NCC (Ren et al.,

394

2000; Lu et al., 2003; Zhao and Zhou., 2009; Cui et al., 2011, 2013; Deng et al., 2016a).

395

The 1.6-1.4 Ga aged rocks are locally found in the southern NCC (e.g. the ~1.60 Ga

396

Maping granite, Deng et al., 2015; ~1.53 Ga A-type granites, Deng et al., 2016b; and

397

~1.47 Ga Panhe syenites, Zeng et al., 2013). Consequently, the southern NCC was

398

likely an important provenance for the Xuhuai Basin.

399

In combination with the dataset from the literature, the Niyuan and Shijia

400

Formations show detrital zircon age groups between 1.8 Ga and 1.0 Ga with high

401

diversity but the ~2.1 Ga and ~1.9 Ga ages become rare (Fig. 9d, e). Taking the 14

402

continuity of the sedimentation into consideration, 1.8-1.4 Ga zircons could be also

403

sourced from the southern NCC. The 1.4-0.9 Ga magmatic rocks have been rarely

404

reported from the NCC, except a few 1.25-1.2 Ga granite body in North Korea (Zhao et

405

al., 2006; Park et al., 2016a) and some ~1.40 Ga tuff layers (Su et al., 2008, 2010) and

406

some ~1.35-1.30 Ga dikes/sills (Wang et al., 2014; Zhang et al., 2009, 2012, 2017) in

407

the Yanliao rift. However, they can hardly provide material to the basins because they

408

are either contained in strata or covered by the sedimentary rocks. The 1.40-0.97 Ga

409

zircon grains provenanceare seemly not from the NCC.

410

It is noteworthy that a drastic change in the provenance system occurred in the

411

Jinshanzhai Formation of the Langan Group. A sharp increase in ~2.1 Ga zircon grains

412

of the Jinshanzhai Formation indicates a change in source area (Fig. 9f), which is more

413

or less similar to the basal formation of the Huaibei Group (Fig. 9a). The ~2.1 Ga

414

zircons, with εHf(t) clustering around 0 (Fig. 8c), are highly consistent with local

415

Zhuangzili granite (Yang et al., 2009). It suggests that the zircons of the Jinshanzhai

416

Formation are all sourced from the NCC itself. This drastic provenance change between

417

the Huaihe Group and the Langan Group can be interpreted to have resulted from a

418

shift in provenance due to tectonic event(s).

419 420

6.3 Tectonic setting of the Xuahuai sequence

421

The depositional setting of the Xuhuai Basin has aroused big debate and led to

422

different interpretations, e.g., a syn-collisional basin (Dong et al., 2011, 2014), an

423

intracontinental rift (Lu et al., 2008; Peng et al., 2011a; Zhai et al., 2015), or a

424

back-arc basin (Li et al., 2003; Sun et al., 2010). Considering the new zircon U-Pb

425

ages of sedimentary rocks, we conclude that the deposition of the Xuhuai sequence

426

initiated at ~1.1 Ga, which is nearly synchronous with the global Grenvillian orogenic

427

processes. An accretion of the North Qinling Terrane along the southern NCC during

428

the transition of the Mesoproterozoic and the Neoproterozoic has long been proposed

429

and debated (Yang et al., 1993; Lu et al., 2003; Dong et al., 2011, 2014; Tang et al.,

430

2015; Zhang et al., 2015; Cao et al., 2016). Generally, sediments in the syn-collisional 15

431

basin are composed of coarsening upward cycles and form intraformational

432

unconformities (Condie, 1997; Spencer et al., 2014; Krabbendam et al., 2017). In

433

addition, in syn-collisional background, the detrital zircon ages are close to the

434

depositional age of the sediments (Sun et al., 2008; Cawood et al., 2012; Tang et al.,

435

2015). However, in the Xuhuai Basin, the sedimentary sequence consists of

436

conglomerate, sandstone, shale, and carbonate without any intraformational

437

unconformities. Furthermore, the detrital zircon ages of the Xuhuai sequence display

438

a wide age range from the Neoarchean to the early Neoproterozoic (Fig. 9). The above

439

scenarios are quite different from those in syn-collisional basins. On the other hand,

440

some researchers proposed that the Xuhuai sequence was a back-arc environment

441

based on geochemical studies (Li et al., 2003; Sun et al., 2010). In back-arc basins,

442

deposits are generally dominated by pelagic, hemipelagic clays, and biogenic

443

carbonate and silica sediments in deep-water facies setting (Klein, 1985; Ingersoll,

444

1988; Condie, 1997). In addition, siliciclastic strata in back-arc basin contain many

445

volcanic particles derived from the volcanic arc (Dickinson et al., 1983; Bhatia and

446

Crook, 1986; Sun et al., 2008; Du et al., 2013). In this study, the Xuhuai sequence

447

consists of alluvial-coastal coarse-grained clastic deposits to shallow-water platform

448

carbonates. The siliciclastic rocks are chiefly made up of cratonic crystallized quartz,

449

lacking volcanoclastic components (Fig. 5). Furthermore, there is a lack of evidence

450

to support a late Mesoproterozoic to early Neoproterozoic arc-related volcanic activity

451

throughout the NCC. Consequently, the above scenarios also argue against the

452

suggestion of back-arc basins for the Xuhuai basin.

453

In contrast, the ~0.93-0.89 Ga mafic intrusions were extensively distributed in

454

the central and southeast NCC (Liu et al., 2006; Gao et al., 2009; Peng et al., 2011a,

455

2011b; Wang et al., 2012; Zhu et al., 2019). A large-scale mafic intrusion is an

456

essential indicator for widespread continental lithospheric extension and a pointer of

457

continental rifting events (Halls, 1982; Ernst et al., 1995, 2003; Bleeker and Ernst,

458

2006; Hou et al., 2008a,b; Peng, 2010; Ernst, 2014; Zhang et al., 2017). In this

459

context, Peng et al. (2011b) proposed a large igneous province resulted from

460

sub-lithospheric mantle upwelling with the magmatic center situated in the Xuhuai 16

461

area. We speculate that the southeast NCC could have been under the extension

462

background at the transition of the Mesoproterozoic and the Neoproterozoic. The

463

lower part of the Huaihe Group, and its equivalent, Huainan Group in the Huainan

464

region, recorded a rapid change from terrigenous coastal sandstone of the Lanling

465

Formation to shelf shales of the Xinxing Formation (Fig. 10). This transition is

466

consistent with the early stages of a rift basin when the sea level rose rapidly, and the

467

basin was under-filled (Meng et al., 2011). The middle Huaihe Group recorded a

468

regression represented by the open carbonate platforms (Zhangqu, Jiuliqiao

469

Formations, and middle Wangshan Formation) and restricted carbonate platforms

470

(Niyuan, Weiji, Sidingshan Formations, Wang, 2009; Ma, 2015) while the

471

sedimentation area gradually shrunk toward the basin center. With an oscillation of

472

the Shijia-Wangshan Formation, it finally came to the unconformity between the

473

Wangshan and Jinshanzhai Formations. The Lower, Middle, and Upper Huaihe Group

474

all include a siliciclastic-carbonate succession, which represents a new sedimentary

475

phase. They are most likely associated with the creation of accommodation space

476

changes induced by intermittent, rapid subsidence and uplift in the basin, indicating

477

an active tectonic affected the sedimentation (Qiao et al., 1994; Pan et al., 2000). It is

478

consistent with an upwelling mantle plume event or the pre-magmatic uplift model

479

(Zhang et al., 2016). We suggest that the background of the Huaihe Group of the

480

Xuhuai basin could be a rift basin (Fig. 10).

481

The Langan Group was siliciclastic-carbonate sediments deposited on the

482

carbonate rocks of the Huaihe Group in the Huaibei section (Fig. 3m). The zircons of

483

the Jinshanzhai Formation are seemly all sourced from the NCC itself. However,

484

several episodes of younger tectonic events and the “Great Unconformity” perhaps

485

destroyed much of the stratigraphic record. The background of the Langan Group

486

needs further detailed study.

487 488 489

6.4 Implications for supercontinent reconstruction Peng et al. (2011a, b) reconstructed the sinistral displacement of the two blocks 17

490

on the opposite sides of the Tan-Lu fault, and consequently, the Xuhuai, Jiaolai,

491

Dalian and Pyongnam basins located side by side and are geographically connected.

492

Because of similar siliciclastic-carbonate successions and the synchronous ages, the

493

basin fill sequences have been considered to be comparable (Hong et al., 1992; Liu et

494

al., 2005; Wang, 2007). Furthermore, all of them have sills or dikes intruding at

495

similar ages. Peng et al. (2011a) proposed a Xuhuai-Dalian-Pyongnam proto-basin or

496

rift system during the early Neoproterozoic. Comparing the age population of these

497

equivalent sequences along the southeast NCC, it is notable that the provenances are

498

also similar: all of them contain plenty of zircons with middle to late Mesoproterozoic

499

ages that can’t be interpreted only by the NCC provenances (Lu et al., 2012; Hu et al.,

500

2012; Liu et al., 2017). The Mesoproterozoic zircon U-Pb ages of the Pyongnam

501

Basin exhibit two prominent peaks at ~1.2 and ~1.6 Ga (Fig. 11c). For the Xuhuai

502

Basin, it is evident that the ages exhibit high diversity with a more significant portion

503

for the 1.4-1.3 Ga ages (Fig. 11f). The Mesoproterozoic zircon grains of the Dalian

504

and Jiaolai basins show mixtures of the Xuhuai and Pyongnam patterns (Fig. 11d,e),

505

though some local influences exist. It is suggested that there possibly was an effective

506

source of 1.4-1.3 Ga neighboured the southeast NCC. Consequently, we propose that

507

the sedimentary sequences in the southeast NCC might have bidirectional

508

provenances, i.e., one from northeast and one from southwest (at present coordinates).

509

To investigate the position of the NCC in the Rodinia supercontinent, several

510

paleogeographic reconstructions were also proposed. Among many supercontinent

511

configurations related to the NCC, two groups of models are particularly interesting to

512

interpret the 1.8-0.9 Ga provenances of the Neoproterozoic successions in the Xuhuai

513

rift system: one is connecting the northern side of the NCC with Canadian shield or

514

Baltica (e.g., Hou et al., 2008a; Zhang et al., 2009; Kaur et al., 2013; Liu et al., 2017);

515

and the other is connecting the southeast side of the NCC with the São

516

Francisco-Congo Craton (e.g. Peng et al., 2011a; Peng, 2015; Cederberg et al., 2016;

517

Xu et al., 2017; Teixeira et al., 2017; de Oliveira Chaves et al., 2019). The first model

518

can explain the ~1.2-1.1 Ga provenances from the Grenville orogen (adjacent to the

519

Canadian and Baltic Shields) into the Xuhuai rift system from the north side (at 18

520

present coordinates). This model can thoroughly explain the observation that the

521

detrital zircon age spectrums of the early Neoproterozoic sediments from the western

522

Baltic and the Pyongnam basin are quite similar (Fig. 11a,c). The latter group of

523

models can provide 1.4-0.9 Ga provenances from the Kibaran belt and the

524

Mesoproterozoic ‘inliers’ in the southwest Congo craton into the Xuhuai rift system

525

from the south side (at present coordinates). This model can explain that the spectrum

526

of detrital zircon ages for the late Mesoproterozoic to early Neoproterozoic sediments

527

from the Xuhuai basin, i.e., which has diverse age models of 1.4-0.9 Ga (Fig. 11f-h).

528

Peng et al. (2011b), Peng (2015), and de Oliveira Chaves et al. (2019) proposed

529

that the NCC and the São Francisco-Congo Craton could be close neighbors based on

530

the reconstruction of the ~0.9 Ga large igneous province. This is further constrained by

531

a comparison of the Paleoproterozoic orogens in the two cratons (Teixeira et al., 2017),

532

as well as paleomagnetic studies (e.g., Cederberg et al., 2016; Xu et al., 2014, 2017).

533

From the distinctive crystallization ages, the volcanic rocks, dioritic, granitic intrusions,

534

and ortho-gneisses of 1.5-1.0 Ga in the Kibaran Belt in the east Congo craton and its

535

southwest extensions, the Mesoproterozoic basement ‘‘inliers’’ within the

536

Neoproterozoic Damara/Kaoko belts in the southwest Congo craton, were identified

537

(e.g. ~1.37 Ga Kibaran bimodal volcanic, Kokonyangi et al., 2004; Tack et al., 2010,

538

Debruyne et al., 2015; ~1.2 Ga A-type granites and volcanic, ~1.0 Ga tin-granites,

539

Becker et al., 2006; Tack et al., 2010; ~1.1 Ga tholeiites, Becker et al., 2006; 1.0-0.9 Ga

540

Zandian and Mayumbian volcanic rocks and granites, Tack et al., 2001; 1.5-1.1 Ga

541

pinkish granitic and trondhjemitic plutons, Kröner et al., 2015, 2017). The 1.5-1.0 Ga

542

zircon grains of the Xuhuai Basin are highly consisitent with these ages. The São

543

Francisco-Congo craton have also undergone intraplate rift evolution in the early

544

Neoproterozoic (Martins-Neto, 2009; Rodrigues et al., 2010, 2012; Matteini et al.,

545

2012).

546

Based on these several lines of evidence, we propose that the Huaihe Group in the

547

Xuhuai basin in the southeastern NCC might have had a early Mesoproterozoic

548

provenance from the southern NCC and a middle to late Mesoproterozoic provenance

549

from the southwest Congo Craton (Fig. 12). The Early Neoproterozoic Xuhuai rift 19

550

system along the southeast NCC, the upper Espinhaço rift system in the east São

551

Francisco Craton, and the coeval basins in the Brasilia belt and the west Congo Craton,

552

could belong to a unified rift system (Fig. 12). This model can explain the correlated

553

detrital zircon spectrums among the above basins (Fig. 11).

554 555

7. Conclusion remarks

556

1) The Xuhuai basin is an extensional rifting basin. It shows a transgression

557

process in the Huaihe Group and a regional uplifting represented by the 0.9-0.8 Ga

558

unconformity between the Wangshan and Jinshanzhai Formations. A comparison of

559

regional basin formation suggests that the Xuhuai, Jiaolai, Dalian, and Pyongnam

560

basin could belong to the same rift system (the Xuhuai rift system).

561

2) There was a distinct provenance change from ~2.7-2.5 Ga, ~2.1 Ga and ~1.9

562

Ga rocks (zircon ages) at the bottom formation, to ~1.8-1.0 Ga rocks in the

563

Middle-Upper Huaihe Group in Huaibei region and the Huainan and Feishui Groups

564

in Huainan region, and back to ~2.7-2.5 Ga, ~2.1 Ga and ~1.9 Ga rocks in the Langan

565

Group. The ~2.7-2.5 Ga, ~2.1 Ga, ~1.9 Ga, and ~1.8-1.4 Ga rocks could be from the

566

NCC, while the 1.4-1.3 Ga rocks were possibly from a paleocontinent, which

567

neighbored the NCC before 0.9 Ga.

568

3) A North China-São Francisco-Congo connection hypothesis is supported, in

569

which the Early Neoproterozoic basins such as the Xuhuai rift basins along the

570

southeastern margin of the NCC, the coeval basins along the eastern and western

571

margin of the São Francisco craton, as well as those along the southwest margin of the

572

Congo craton comprise the same rift system during 1.1-0.9 Ga.

573 574 575

Acknowledgements This study was financially supported by the NFSC Project (41890833, 41772192)

576

and the Key Research Project of CAS Frontier Research Project Scientific

577

(QYZDB-SSW-DQC04281712250). Peng P thanks Prof Wilson Teixeira, Prof Elson 20

578

P Oliveira, Prof Farid Chemale Jr, Prof Taiping Zhao, Prof Xixi Zhao, Dr Huiru Xu,

579

Dr Lei Zhao, Dr Yanyan Zhou and Dr Tiago J Girelli for their help during the field

580

trip in Brazil and their thoughtful ideas.

581 582 583

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584

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and Hf isotopic compositions of Paleoproterozoic Granites from the eastern part

936

of Liaoning Province and their tectonic significance. Acta Geologica Sinica, 90,

937

2620-2636 (in Chinese with English abstract).

938

Spencer, C.J., Roberts, N.M., Cawood, P.A., Hawkesworth, C.J., Prave, A.R.,

939

Antonini, A.S., Horstwood, M.S., 2014. Intermontane basins and bimodal

940

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941

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942

Su, W.B., Zhang, S.H., Huff, W.D., Li, H.K., Ettensohn, F.R., Chen, X.Y., Yang,

943

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944

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945

subdivision of the Meso- to Neoproterozoic history of the North China Craton.

946

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947

Su, W.B., Li, H.K., Warren, D.H., Ettensohn, F.R., Zhang, S.H., Zhou, H.Y., Wan,

948

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949

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950

Su, X.D., Peng, P., Wang, C., Sun, F.B., Zhang, Z.Y., Zhou, X.T., 2018. Petrogenesis

951

of a ~900 Ma mafic sill from Xuzhou, North China: Implications for the genesis

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Sun, L.H., Gui, H.R., Chen, S., Ma, Y.P., Wang, G.L., 2010. Provenance and tectonic

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setting of the Neoproterozoic diamictites from Jiayuan Formation in northern

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957

Sun, W.H., Zhou, M.F., Yan, D.P., Li, J.W., Ma, Y.X., 2008. Provenance and tectonic

958

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959

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960

Tack, L., Wingate, M.T.D., Liégeois, J. P., Fernandez-Alonso, M., Deblond, A., 2001.

961

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962

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963

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964

Tack, L., Wingate, M.T.D., De Waele, B., Meert, J., Belousova, E., Griffinf, B., Tahon, 33

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966

Prominent emplacement of bimodal magmatism under extensional regime.

967

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968

Tang, L., Santosh, M., Dong, Y.P., Tsunogae, T., Zhang, S.T., Cao, H.W., 2015.

969

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971

Tang, Q., Pang, K., Yuan, X., Wan, B. & Xiao, S., 2015. Organic-walled microfossils

972

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973

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Teixeira W, Oliveira EP, Peng P, Dantas EL, Hollanda MHBM, 2017. U-Pb

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geochronology of the 2.0 Ga Itapecerica graphite-rich supracrustal succession in

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Wan, B., Tang, Q., Pang, K., Wang, X. P., Bao, Z. A. and Zhou, C. M., 2019.

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986

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Wang, L.J., 2009. Stratigraphic division, correlation and sedimentary environment

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analysis of the Neoproterozoic in Xuhuai region. A thesis for Master degree. 34

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Shandong University of Science and Technology, 80-92 (in Chinese with English

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Wang, Q.H., Yang, D. B., Xu, W. L., 2012. Neoproterozoic basic magmatism in the

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1001

Wang, Q. H., Yang, H., Yang, D. B., Xu, W. L., 2014. Mid-Mesoproterozoic (∼1.32

1002

Ga) diabase swarms from the western Liaoning region in the northern margin of

1003

the North China Craton: Baddeleyite Pb-Pb geochronology, geochemistry and

1004

implications for the final breakup of the Columbia supercontinent. Precambrian

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Wang, X.L., Jiang, S.Y., Dai, B.Z., 2010. Melting of enriched Archean subcontinental

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lithospheric mantle: Evidence from the ca, 1760 Ma volcanic rocks of the

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Xiong’er Group, southern margin of the North China Craton. Precambrian Res.

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Wilde, S.A., Zhao, G.C., 2005. Archean to Paleoproterozoic evolution of the North China Craton. Journal of Asian Earth Sciences, 24, 519-522.

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analysis with an excimer laser, depth profiling, ablation of complex geometries

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and concomitant age estimation. Chem. Geol., 209:121-135.

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Wu, F.Y., Yang, Y.H., Xie, L.W., Yang, J.H., Xu, P., 2006. Hf isotopic compositions

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of the standard zircons and baddeleyites used in U-Pb geochronology. Chemical

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Geology, 234, 105-126.

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Neoproterozoic carbonate successions in North China. Precambrian Res. 246,

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Y.S., 2014. SHRIMP U-Pb dating of detrital zircons from the Fenzishan Group

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in eastern Shandong, North China craton. Acta Petrol. Sin. 30, 2989-2998(in 35

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1026

Xu, H.R., Yang, Z.Y., Peng, P., Meert, J.G., Zhu, R.X., 2014. Paleo-position of the

1027

North China Craton within the supercontinent Columbia: constraints from new

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Xu, H.R., Yang, Z.Y., Peng, P., Ge, K.P., Jin, Z.M., Zhu, R.X., 2017. Magnetic

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fabrics and rock magnetism of the Xiong'er volcanic rocks and their implications

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for tectonic correlation of the North China Craton with other crustal blocks in the

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Paleoproterozoic K-feldspar granites in Bengbu uplift: Constrains from

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petro-geochemistry, zircon U-Pb dating and Hf isotope. Earth Science-Journal of

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China University of Geosciences, 34(1), 148-164 (in Chinese with English

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and Hf isotope data from detrital zircons in the Neoproterozoic sandstones of

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northern Jiangsu and southern Liaoning Provinces, China: implications for the

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1070

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1098

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1099

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1100

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1101

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Zhu, R.Z., Ni, P., Wang, G.G., Ding, J.Y., Fan, M.S., MaY.G., 2019. Geochronology,

1103

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1104

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1105

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1106 1107 1108 1109 1110 1111 1112 1113 1114 1115 1116 1117 1118 38

1119 1120 1121 1122

Figure Captions

1123 1124

Fig. 1 (a) Archean-Paleoproterozoic basement and Meso-Neoproterozoic cover

1125

of the North China Craton (Modified after Peng et al. (2011a); (b) Geological map of

1126

the late Mesoproterozoic to early Neoproterozoic Xuhuai sequence in the Huaibei and

1127

Huainan regions and locations of the sections shown in the Fig. 10 (modified from

1128

Yang et al. (2012); Xiao et al. (2014).

1129 1130

Fig. 2 Simplified lithostratigraphic columns of the late Meso- to early

1131

Neoproterozoic Xuhuai sequence in the Huainan and Huaibei regions (modified from

1132

BGMRJ (1984); BGMRA (1985). The paleocurrents are after BGMRJ (1997).

1133 1134

Fig. 3 Outcrops of the late Meso- to early Neoproterozoic Xuhuai sequence in

1135

the Huaibei region. (a) Bedded sandstone overlying the reddish coarse-grained

1136

sandstone with low angle cross beddings, Lanling Formation; (b) Low angle

1137

bi-directional cross-beddings, the Lanling Formation; (c) Thin layers of marls, the

1138

Xinxing Formation; (d) Thealternating shales and fine-grained sandstone, upper

1139

Chengshan Formation; (e) Alternating layers of calcareous shales and limestones, the

1140

Jiayuan Formation; (f) Laminated limestone, Jiayuan Formation. (g) Medium-thick,

1141

dark gray limestone with very thin calcareous shale interlayers, the Zhaowei

1142

Formation; (h) Thick-bedded micritic limestone with stromatolite interlayers, the

1143

Zhaowei Formation; (i) Light reddish fine-grained sandstone, Shijia Formation; (j)

1144

Cross-laminated sandy limestone, Shijia Formation; (k) Light gray limestone with

1145

cherty bands, the Wangshan Formation; (l) Molar tooth structures, the Wangshan

1146

Formation; (m) The unconformity between the dolostone of Wangshan Formation and 39

1147

the cherty breccia of the Jinshanzhai Formation (yellow line); (n) Reddish columnar

1148

stromatolite, the Jinshanzhai Formation; (o) The boundary and conformity between

1149

the Jinshanzhai Formation and the lower Cambrian: the yellowish shale of the

1150

topmost part of the Jinshanzhai Formation (left part) and the reddish calcareous shale

1151

of the lower Cambrian (right part).

1152 1153

Fig. 4 Outcrops of the late Meso- to early Neoproterozoic Xuhuai sequence in

1154

the Huainan region. (a) Poorly to moderately sorted, clast-supported conglomerate,

1155

the Caodian Formation; (b) Massive coarse-grained sandstone, the Caodian Formation;

1156

(c) Thick pure quartzose sandstone, the Bagongshan Formation; (d) Interlayers of

1157

shales and sandstone, Liulaobei Formation; (e-f) Thin straitification of gray

1158

calc-quartzose sandstone, Shouxian Formation.

1159 1160 1161

Fig. 5 Petrological characters of the samples. a. DWSH-2; b. XZZ-1; c. P2-JSZ-1.

1162 1163

Fig. 6 Representative CL images of selected zircons from the samples. Solid

1164

circles show the locations for LA-ICP-MS U-Pb analyses (spot size of 24 μm). Dotted

1165

circles show the locations for LA-MC-ICP-MS Hf analyses (spot size of 32 μm).

1166 1167 1168

Fig. 7 U-Pb concordia and relative probability plots of detrital zircons of the samples from the Xuhuai Sequence. Ages are in Ma and ellipses show 1σ errors.

1169 1170 1171

Fig. 8 Hafnium isotope characteristics of zircon grains from the Xuhuai Sequence. 40

1172 1173 1174

Fig. 9 Relative probability plots of detrital zircon ages from different formations of the Xuhuai sequence.

1175 1176 1177

Fig. 10 (a) Schematic stratigraphic sections of the Xuuhai sequence in the

1178

Huainan and Huaibei regions (modified from BGMRA, 1985; BGMRJ, 1997). ○1 -○4

1179

are sections in the Huaibei region; ○5 -○7 are sections in the Huainan region. The

1180

Locations of the sections are indicated in the Fig. 1b. (b) Cartoon showing the

1181

stratigraphic correlation of reconstructed Xuhuai basin (Modified from BGMRJ,

1182

1997).

1183 1184

Fig. 11. Binned frequency histograms of detrital zircon ages from different late

1185

Mesoproterozoic to early Neoproterozoic sequences in the southeastern NCC, Baltic

1186

and São Francisco-Congo. a. Data from Kirkland et al. (2008), Bingen et al. (2011),

1187

Agyei-Dwarko et al. (2012) and Spencer et al. (2014); b. Data from Matteini et al.

1188

(2012), Rodrigues et al. (2010) and Rodrigues et al. (2012); c. Data from Hu et al.

1189

(2012) and Park et al. (2016b); d. Data from Luo et al. (2006), Gao et al. (2010), and

1190

Yang et al. (2012); e. Data from Zhou et al. (2008), Chu et al. (2011), Hu et al. (2012)

1191

and Lu et al. (2012); f. Data from Yang et al. (2012), He et al. (2017) and this study; g:

1192

Data from Delpomdor et al. (2013); Konopasek et al. (2014), Konopasek et al. (2017),

1193

Kuchenbecker et al. (2015); h: Data from the Ribeiro et al. (2013), Santos et al.

1194

(2013), De Castro et al. (2019).

1195 1196

Fig. 12 A speculation of paleogeographic reconstruction of the NCC at early

1197

Neoproterozoic (modified from Peng et al., 2015). The Kibaran orogen is after Tack

1198

et al. (2010). The position of Mesoproterozoic “inliers” in the southwest Congo are

1199

after Gray et al. (2006), Kröner et al. (2017). The rift basins are modified from Peng

1200

et al. (2011a), De Castro et al. (2019). The dyke swarms follow Peng et al. (2011b), 41

1201

Correa-Gomes and Olivera (2000), Evans et al. (2010, 2016) and Kouyate et al.

1202

(2013). The Ganjila-Mayumbian magmatism follows Tack et al. (2001).

1203

Highlights:

1204 1205 1206



Xuhuai Basin comprises the Huaihe (1.1-0.9 Ga) and Langan (<0.8 Ga) Groups.

1207



Upper Huaihe Group (Niyuan-Wangshan Fm.) deposited at 0.97-0.89 Ga.

1208



Upper Huaihe Group records a provenance from the Grenvillian orogens

1209 1210



1.1-0.9 Ga basins of the North China and São Francisco-Congo cratons are correlated.

1211 1212

Conflict of interest statement

1213 1214

We declare that we have no financial and personal relationships with other

1215

people or organizations that can inappropriately influence our work. There is no

1216

professional or other personal interest of any nature or kind in any product,

1217

service and/or company that could be construed as influencing the position

1218

presented in, or the review of, the manuscript entitled.

1219 1220 1221 1222 1223

1224 42

1225

On behalf of all the co-authors

1226

_______________________________________________________

1227

Institute of Geology and Geophysics, Chinese Academy of Sciences

1228

19 Beitucheng Xilu Street, Beijing, China 100029

1229 1230 1231

Tel: 86-10-82998530; e-mail: [email protected] Homepage: http://sourcedb.igg.cas.cn/cn/zjrck/200907/t20090713_2065446.html

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