Multiple provenance of rift sediments in the composite basin-mountain system: Constraints from detrital zircon U-Pb geochronology and heavy minerals of the early Eocene Jianghan Basin, central China

    Multiple provenance of rift sediments in the composite basin-mountain system: Constraints from detrital zircon U-Pb geochronology and heavy minerals of the early Eocene Jianghan Basin, central China Lulu Wu, Lianfu Mei, Yunsheng Liu, Jin Luo, Caizheng Min, Shengli Lu, Minghua Li, Libin Guo PII: DOI: Reference:

S0037-0738(16)30299-8 doi:10.1016/j.sedgeo.2016.12.003 SEDGEO 5144

To appear in:

Sedimentary Geology

Received date: Revised date: Accepted date:

13 October 2016 9 December 2016 11 December 2016

Please cite this article as: Wu, Lulu, Mei, Lianfu, Liu, Yunsheng, Luo, Jin, Min, Caizheng, Lu, Shengli, Li, Minghua, Guo, Libin, Multiple provenance of rift sediments in the composite basin-mountain system: Constraints from detrital zircon U-Pb geochronology and heavy minerals of the early Eocene Jianghan Basin, central China, Sedimentary Geology (2016), doi:10.1016/j.sedgeo.2016.12.003

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ACCEPTED MANUSCRIPT Multiple

provenance

of

rift

sediments

in

the

composite

basin-mountain system: Constraints from detrital zircon U-Pb

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geochronology and heavy minerals of the early Eocene Jianghan

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Basin, central China

Lulu Wu a, Lianfu Mei a*, Yunsheng Liu b, Jin Luo b, Caizheng Min a, Shengli Lu a, Minghua Li b,

Key laboratory of Tectonics and Petroleum Resources of Ministry of Education, China

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a

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Libin Guo b

University of Geosciences, Wuhan 430074, China

Research Institute of Exploration and Development of Jianghan Oilfield, SINOPEC, Wuhan

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b

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430000, China

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*Corresponding author: Lianfu Mei, E-mail: [email protected]

Abstract

Zircon U-Pb geochronology and heavy minerals are used in combination to provide valuable insights into the provenance of the early Eocene Jianghan Basin, central China. Five samples for zircon U-Pb dating and eighty-five samples for heavy mineral analysis were collected from drill cores or cuttings of the Xingouzui Formation. Most analyzed zircons are of magmatic origin, with oscillatory zoning. Detrital zircons from sample M96 located on eastern basin have two dominant age groups of 113-158 Ma and 400-500 Ma, and the other samples located on southern basin have three prominent age populations at 113-158 Ma, 400-500 Ma and 700-1000 Ma. Samples on 1

ACCEPTED MANUSCRIPT different parts of the basin show distinct differences in heavy mineral compositions and they apparently divide into two groups according to the content of rutile (higher or lower than 4%). The

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spatial variations of zircon-tourmaline-rutile (ZTR) indices are marked by some noticeable

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increasing trends from basin margins to the inner part of the basin. Compared with the potential source areas, this study clarifies the multiple source characteristics of the Jianghan basin in the composite basin-mountain system. The majority of clastic material was supplied from the north

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source area through rift-trough sediment-transport pathways, and the eastern, southern and

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northwestern source areas also contributed detritus to the basin. This clastic material is broadly dispersed in the basin. The early Eocene paleogeography implies that rift architecture and rifting

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process had an important influence on sediment dispersal. This study shows that integrated zircon

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sediment provenance.

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U-Pb geochronology and heavy mineral analysis is a useful and powerful method to identify

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Keywords: zircon U-Pb geochronology; heavy minerals; multiple provenance; composite basin-mountain system; Early Eocene; Jianghan Basin.

1. Introduction Provenance analysis is an important component of basin analysis, helping to understand basin development by linking sediment supply to exhumation episodes and tectonic evolution (e.g., Japsen et al., 2007; Kelty et al., 2008; Olivarius et al., 2014; Sun et al., 2016) and reconstructing sediment transport routes (Rossi et al., 2002; Olivarius et al., 2014; Wang et al., 2014a). Rift basins are always surrounded by mountains and massifs, covered by various types of rocks, 2

ACCEPTED MANUSCRIPT resulting in sediment input from multiple sources, which has been discussed extensively in published works (e.g., Fonneland et al., 2004; Morton et al., 2005, 2009; Weibel et al., 2010; Shen

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et al., 2012a; Wang et al., 2014a, 2015b; Jiang et al., 2015; Nielsen et al., 2015; Liu et al., 2016a;

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Shao et al., 2016). The multiple source features are generally characterized by sediments with similar and /or different compositions (zircon and heavy mineral compositions) derived from multiple directions. This study introduces the concept of a “composite basin-mountain system”

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proposed by Wu et al. (2006) and Shen et al. (2007), to define the source to sink relations of rift

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basin. Rift basins in the composite basin-mountain system tend to have more complex source to sink relations than in the single basin-mountain system where sediments were usually derived

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from one source and/or direction (e.g., Decou et al., 2011; Yang et al., 2013; Sun et al., 2016).

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Therefore, provenance studies in rift basin settings in a composite basin-mountain system are

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invariably difficult and challenging.

The early Eocene Xingouzui Formation is an important hydrocarbon exploration target

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stratum of the Jianghan Basin (e.g., Yuan, 2010). Studies on the provenance of the Xingouzui Formation have focused on field outcrops, heavy minerals, seismic facies, sand-bearing ratios and sedimentary facies (Rui, 2009; He, 2009; Yang, 2010; Yuan, 2010; Xie et al., 2011a; Wan et al., 2011; Fang, 2012). The provenance models suggest that sediments were derived from northwestern, northern and eastern margins and these studies provide abundant information on the provenance of the early Eocene Jianghan Basin. However, due to the absence of data in the southern basin and no precise geochronologic and isotopic data, some questions remained unsolved, such as whether there is southern source and how sediments derived from multiple sources disperse. In the past few years, quite a number of sandbodies and oil pools of the 3

ACCEPTED MANUSCRIPT Xingouzui Formation have been discovered in the southern Jianghan Basin (Liu, 2015b; Liu et al., 2016b). The contiguous development of reservoir sandbodies in the southern basin may be not

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supported by the previous provenance model. Therefore, further study on the early Eocene

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provenance and sediment routing system of the Jianghan Basin is urgently needed. However, there is still no precise zircon U-Pb data to constrain it, let alone the combination of zircon U-Pb geochronology and heavy minerals. This has hindered a better understanding of provenance and

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oil exploration in the Jianghan Basin, as well as the source to sink relations of rift basin settings in

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a composite basin-mountain system

Various methods are applicable for provenance analysis (Weltje and von Eynatten, 2004;

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Olivarius and Nielsen, 2016), including detrital zircon geochronology, heavy mineral analysis and

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bulk rock geochemistry. In this paper, detrital zircon U-Pb geochronometry and heavy mineral

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analysis are used integratedly for their individual advantages. Detrital zircon U-Pb data can provide accurate and useful information of source areas, as zircon can possess an inherently stable

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U-Pb isotopic system under the effect of weathering, erosion, multiple episodes of transportation, and thermal alteration (Bruguier et al., 1997; Cherniak and Watson, 2000; Fedo et al., 2003; Košler and Sylvester, 2003). These advantages make it a reliable tool for basin provenance analysis and paleogeographic reconstruction (e.g., Dickinson and Gehrels, 2003; Moecher and Samson, 2006; Zhao et al., 2013a; Albardeiro et al., 2014; Wang et al., 2014a; Yao et al., 2015; Bradley et al., 2016; Li et al., 2016; Xie, 2016). Heavy minerals, on the other hand, can give an indication of the source directions and sediment transport distance (Morton and Hallsworth, 1999; Bassist et al., 2016; Olivarius and Nielsen, 2016) and many minerals have specific geneses that can provide important provenance information (Morton and Hallsworth, 1994, 1999). The 4

ACCEPTED MANUSCRIPT combined use of these two methods can effectively identify source areas with similar characteristics and sediment routing systems (Morton et al., 2001; Olivarius et al., 2014), even in

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the composite basin-mountain system (Cao et al., 2015a; Jiang et al., 2015).

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In this study, we carried out a comprehensive analysis of detrital zircon U-Pb geochronometry and heavy minerals, in order to (1) identify the source areas, (2) establish a spatial framework of sediment dispersals, and (3) outline the paleogeography of the early Eocene

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Jianghan Basin in the composite basin-mountain system.

2. Geological setting

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The Jianghan Basin located in the Yangtze Block (Wang et al., 2006) (Fig. 1A, B) is a large

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Mesozoic-Cenozoic petroliferous rift basin, with a total area of 28 000 km2. It is bound by the

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Qinling Orogen Belt in the north, the Dabie Terrance and Edong fold-thrust belt in the northeast and east (Fig. 1B). Its southern part is adjacent to the Jiangnan Orogen and the western part

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borders the Shennongjia-Huangling massif and Xiang’exi fold-thrust belt. The present geographic features were mainly formed during the late Jurassic to early Cretaceous when the surrounding orogens and massifs had an intensive uplift related to the intracontinental orogeny in eastern China (e.g., Hu et al., 2006; Mei et al., 2010; Shen et al., 2012a; Li et al., 2013b; Ge et al., 2013; Ji et al., 2014; Liu et al., 2015a). In addition, there are also some other contemporary sedimentary basins nearby, such as the Nanxiang and Dongting Basin (Fig. 1B). The Jianghan basin evolved on the Yanshanian folded basement by reactivating pre-existing structures, forming a series of NW-SE to NNW-SSE-trending rift troughs (grabens and half-grabens) in the north of the basin (Wang, 2006; Li et al., 2008; Liu and Wang, 2008; Mei et 5

ACCEPTED MANUSCRIPT al., 2008; Shi et al., 2013; Liu et al., 2015a) (Figs. 1B ,2A). The basin experienced three-stage rifting during the late Cretaceous to Paleogene (Figs. 2B, 3): the late Cretaceous, the Paleocene to

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early Eocene, and the middle Eocene to Oligocene, forming thick of sediments with several sets of

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saliferous strata and source-reservoir-cap assemblages (Liu et al., 2008b; Wu et al., 2012; Luo et al., 2013). The stratigraphic units deposited in the Jianghan Basin (Fig. 3) consist of the Honghuatao and Yuyang Formations in the 1st rifting phase, the Shashi and Xingouzui Formations

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in the 2nd rifting phase, and the Jingsha, Qianjiang and Jinghezhen Formations in the 3rd rifting

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phase. In contrast to the syn-rift stage, the subsidence rate during the post-rift stage was very low and the deposits only have a maximum thickness of 1050 m (Fig. 3). The Xingouzui Formation

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with a maximum thickness of 1200 m lies conformably above the Shashi Formation. The

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Xingouzui Formation is mainly composed of mudstones, gypsiferous mudstones, siltstones and

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sandstones, with a few argillaceous dolomites and basalts. The well-developed dark mudstones are one of the major source rocks of the basin (Li et al., 2015).

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Up to now, many oil fields have been found in the reservoirs of the Xingouzui Formation (e.g., Tuoshi, Laoxin and Shashi oil fields; He, 2009; Liu et al., 2016b). Salt diapirs (Fig. 2B) are widely developed in the basin, and have been recognized by their great significance in hydrocarbon exploration (Xie et al., 1983; Yang, 2004; Huang and Yuan, 2013). Studies suggested that the movement and diapirism of salt in the underlying Shashi Formation initiated during the deposition of the Jiangsha Formation in the middle Eocene (Yang, 2004; Huang and Yuan, 2013). Therefore, although salt diapirism has important influences on the sediment transport pathways (e.g., Matthews et al., 2007; Venus et al., 2015), it has no effect on the Xingouzui sediments (Fig. 3). 6

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3. Sampling and analytical methods

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3.1 Sampling

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The Research Institute of Exploration and Development of Jianghan Oilfield (RIEDJO) has analyzed a certain amount (55 samples) of heavy mineral assemblages of the Xingouzui Formation in the Jianghan Basin. These unpublished data are used in this study. Another 19

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samples were added to cover the whole basin. Together with the published data from Yuan (2010),

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a total of 85 samples were selected for heavy mineral analysis and their locations are displayed in Fig. 4. The photomicrographs of part of these samples are shown in Fig. 5. Sample Hu2 is

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characterized by grains with moderate sorting and roundness, and dominated by quartz (~42%),

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plagioclase (~15%) and authigenic minerals (~32%) (Fig. 5A). Sample Ch8 is characterized by

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grains with moderate sorting and roundness, and dominated by quartz (~46%), plagioclase (~20%) and authigenic minerals (~21%) (Fig. 5B). Sample T20 is characterized by well sorted,

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sub-angular to sub-rounded grains, and dominated by quartz (~48%), plagioclase (~18%) and authigenic minerals (~26%) (Fig. 5C). Sample C2 is characterized by grains with moderately poor sorting and roundness, and dominated by quartz (~38%), plagioclase (~15%) and authigenic minerals (~31%) (Fig. 5D). Antigenic minerals in these sandstones mainly include anhydrite, dolomite and muscovite. Other detailed sample information is given in Table B (Supplementary data). Since the selected samples for heavy mineral analysis are mainly located on the northwestern and northern parts of the Jianghan Basin and previous works have been primarily focused on these areas (Section 1), we selected 7 representative samples for zircon U-Pb geochronology analysis on 7

ACCEPTED MANUSCRIPT the southern and eastern basin (Fig. 4). Among them, 6 samples are used to constrain the sediment provenance of the Xingouzui Formation in the southern basin and one sample is used to constrain

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the provenance of the Xingouzui Formation in the eastern basin. The sampled well-sections

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consist primarily of mudstones with interbedded gypsum, siltstones and sandstones (Fig. 6), suggesting deltaic front or beach-bar deposition. The three samples collected from Yao2, Yao1 and Yao1x-1 are analyzed as a whole, mainly because (1) the three wells are located nearby (Fig. 4)

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and their stratigraphic columns show similar petrographic features to each other (Fig. 6), and (2)

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these sediments maybe belong to the same sand body (Liu et al., 2016b). Other sample information is given in Table A.1 (supplementary data). Samples in this study were all collected

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3.2 Analytical methods

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from the core library of RIEDJO, in Guanghua, China.

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3.2.1 Zircon U-Pb geochronology

Zircons were separated by standard magnetic and density methods from ≥ 1.5 kg samples.

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Following final purification by hand sorting, zircon grains were mounted in epoxy and polished down to near half sections to expose internal grain structures. Cathodoluminescence (CL) imaging and U-Pb dating analysis was undertaken at the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Wuhan. Detailed operating conditions for the laser ablation system and the ICP-MS instrument and data reduction are the same as description by Liu et al. (2010b). Laser sampling was performed using a Geolas 2005. An Agilent 7500a ICP-MS instrument was used to acquire ion-signal intensities. Nitrogen was added into the central gas flow (Ar+He) of the Ar plasma to decrease the detection limit and improve precision (Hu et al., 2008). Each analysis incorporated 20 s of gas blank follow by 50 s of data acquisition. 8

ACCEPTED MANUSCRIPT Zircon 91500 with an age of 1065.4±0.6 Ma (Wiedenbeck et al., 1995) was used as external standard for U-Pb dating, and was analyzed twice every six analyses. The spot diameter was 32

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μm and isotopic ratios of U-Th-Pb were calculated using the ICPMSDatacal program (Liu et al.,

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2008a, 2010b).

The concordia test was performed for each analytical spot from

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Pb/238U and

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Pb/235U

ratios using the function in the software package Isoplot/Ex3.00 (Ludwig, 2003). Percentage of

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discordance has been calculated as {[1 - (206Pb/238U/207Pb/235U age)] × 100}. Zircon ages which 206

Pb/238U

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have more than 10% discordance were rejected in this study (Black et al., 2003). The

ages are used for the grains with ages younger than 1000 Ma, while the 207Pb/206Pb ages are used

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for the grains with ages older than 1000 Ma (Dickinson and Gehrels, 2003). The Isoplot program

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was also used to calculate the weighted mean ages and draw concordia diagrams and probability

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density plots.

3.2.2 Heavy mineral analysis

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To perform the heavy mineral analysis, the samples (0.5-1.0 kg each) from the Xingouzui Formation were first crushed by a jaw crusher and then ground by a vibratory disc mill. Subsequently, the fractions smaller than 250 μm were separated by dry sieving and acid digestion was applied to remove carbonate materials. The heavy mineral fractions were separated using heavy liquids (2.85 g/cm3). About 500 grains from each sample were counted under a petrographic microscope. Identification was made on the basis of optical properties, as described for grain mounts by Mange and Maurer (1992). All the separation and identification of heavy minerals above were completed in RIEDJO.

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ACCEPTED MANUSCRIPT 4. Results A total of 520 detrital zircon analyses was undertaken, with 473 results considered adequate

are

presented

in

Table

A.2

(supplementary

data).

Representative

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compositions

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(discordance ˂10%) for the purpose of evaluating provenance, and zircon U-Pb isotopic

cathodoluminescence (CL) images of the detrital zircons together with U-Pb ages are given in Fig. 7. The detrital heavy mineral percentages of 85 samples are given in Table B.1 (supplementary

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data). The ratios are presented as averages when more than one sample were analyzed in the same

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well. Mica minerals and authigenic minerals were excluded in this study.

4.1 U-Pb geochronology of detrital zircons

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4.1.1 Sample M96

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In sample M96, zircons consist mainly of prismatic euhedral grains or fragments, with a few

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of sub-rounded grains. The majority of zircons presents a regular not perturbed oscillatory zoning (Fig. 7), characteristic of magmatic growth (Rubatto, 2002; Corfu et al., 2003; Fornelli et al.,

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2015). A total of 100 analyses was performed in sample M96. Of this total, 97 results gave concordant ages, which plot on or near concordia (Fig. 8A).The concordant ages range between 114 Ma and 2529 Ma. Most concordant results fall into the two following groups: 114-158 Ma (30%) and 408-487 Ma (34%) (Fig. 8A; Table 1). The probability plot shows two distinct peaks at 139 ± 4 Ma and 440 ± 8 Ma. However, the ages greater than 500 Ma show a dispersed distribution (Fig. 8A). Zircons with ages greater than 400 Ma have a larger proportion of sub-rounded to rounded grains than the remaining grains. 4.1.2 Sample Yx2-Y1-Y1x-1 The majority of the zircons from sample Yx2-Y1-Y1x-1are prismatic euhedral crystals or 10

ACCEPTED MANUSCRIPT fragments, and a small proportion are sub-rounded to rounded grains. Almost all the grains show well-developed oscillatory zoning (Fig. 7). In total, 196 measurements was obtained and 174 of

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them are ages concordant within 90 to 99% (Fig. 8B). The concordant ages yield three major age

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populations at 113-158 Ma (26%), 401-439 Ma (28%), and 722-999 Ma (14%) (Fig. 8B; Table 1). The first and second groups have distinct peaks at 140 ± 3 and 435 ± 6 Ma, respectively. The third group shows two weak peaks at 779 ± 19 and 932 ± 25 Ma. The oldest zircon grain is 3207±29

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Ma, and the youngest zircon grain is 113±1 Ma. Zircons with ages greater than 400 Ma are more

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likely to show sub-rounded and rounded morphologies than the younger (< 400 Ma) grains (Fig. 7).

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4.1.3 Sample Jx9

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In sample Jx9, zircons are mainly prismatic, with a few of sub-rounded to rounded grains.

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The internal textures of these zircons show mainly simple oscillatory zoning (Fig. 7). For sample Jx9, 94 individual detrital zircon grains were analyzed for their U-Pb isotopic compositions. Of

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these, 90 zircon ages are concordant ranging between 117 and 3337 Ma (Fig. 8C). They fall into three age groups: 117-155 Ma (26%) with a peak at 137 ± 4 Ma, 419-489 Ma (23%) with a peak at 443 ± 8 Ma, and 722-992 Ma (27%) with a weighted mean age of 860 ± 33 Ma (Fig. 8C; Table 1). The oldest zircon in this sample has an age of 3337 ± 29 Ma. Zircons with ages greater than 400 Ma have a larger proportion of sub-rounded to rounded grains than the younger (< 400 Ma) grains. 4.1.4 Sample CC-1 For sample CC-1, zircons consist mainly of prismatic euhedral grains or fragments of grains, with a few sub-rounded to rounded grains. CL images reveal that most grains have magmatic zoning (Fig. 7). Only 42 analyses were performed on the detrital zircon grains, of which 32 were 11

ACCEPTED MANUSCRIPT valid ages. The concordant results range between 126 and 2417 Ma (Fig. 8D). Major age groups occur at 126-155 Ma (19%) with a major peak at 143 ± 10 Ma, 425-499 Ma (28%) with a peak at

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445 ± 19 Ma, and 770-996 Ma (19%) with a major peak at 822 ± 58 Ma (Fig. 8D; Table 1). The

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oldest grain yielded an age of 2417 ± 37 Ma. Again, due to the small number of analysed grains, the age populations derived from this sample are simply indicative and maybe have no real statistical meaning.

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4.1.5 Sample H12

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The majority of the zircons from sample H12 are prismatic enhedral crystals or fragments with oscillatory zoning (Fig. 7). In total, 88 zircon grains were analyzed for U-Pb ages and 8

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analyseswere discarded for their discordant ages. The remaining 80 ages that range between 117

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and 2499 Ma have three groupings: 117-147 Ma (28%) with a peak at 136 ± 3 Ma, 411-483 Ma

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(13%) with a peak at 432 ± 17 Ma, and 718-997 Ma (24%) with two peaks at 747 ± 20 and 905 ± 30 Ma (Fig. 8E; Table 1). The ages greater than 1000 Ma show a dispersed distribution. The

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proportion of sub-rounded to rounded zircons in the older (> 400 Ma) group is larger than the younger (< 400 Ma) group.

4.2 Heavy minerals The detrital heavy mineral percentages of the analyzed samples are given in Fig. 9. The heavy mineral suites are dominated by magnetite (41.66% on average) and leucoxene (19.01% on average), followed by zircon with an average of 11.93%. However, the contents of these three minerals show no immediately recognizable trend. The other identified assemblages in decreasing abundance (average of all samples) were: hematite and limonite (8.66%), rutile (7.22%), garnet (3.73%), tourmaline (3.14%), anatase (1.55%), chlorite (1.46%), epidote (0.5%), amphibole 12

ACCEPTED MANUSCRIPT (0.55%). Other identified minerals, with an abundance of 0.59%, were sphene, zoisite and staurolite. As the early Eocene Jianghan Basin is divided into four parts (Fig. 4) based on the basin

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architecture, we tentatively divide these samples into four groups. The samples from the

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northwestern and northern basin show no remarkably difference in heavy mineral compositions (Fig. 9). Comparing with these two groups, sediments from the eastern and southern basin have a higher content of the ultra-stable set of zircon-tourmaline-rutile (ZTR) (Fig. 9). A small part of

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samples (sample T18, T26, T20 and T34) in the northern basin are abnormally abundant in ZTR,

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likely due to their locations close to the eastern basin. The samples from the southern basin have the lowest content of magnetite (25.07% on average) among the four groups. The other heavy

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minerals, such as leucoxene and hematite-limonite, show relatively even distributions in the four

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groups, without obvious diversity. The rutile and ZTR indices are chosen for detrital provenance

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in this study, for their noticeable trends in content. Rutile is one of the most stable heavy minerals in the sedimentary cycle (Meinhold, 2010).

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Although it can be found in many types of rocks (Meinhold, 2010), it can be used as an indicator for detrital sources under specific geological backgrounds (the Jianghan Basin). Fig. 10A shows the spatial variations of the content of rutile. The samples apparently divide two groups. The samples located in the northern basin are distinguished by lower contents of rutile than samples on the other part of the basin. Most of the samples in the former group display an abundance lower than 4%, and only several samples show an abundance higher than 4%. On the contrary, rutile is more abundant in the latter group, in which samples generally display an abundance higher than 4% (Fig. 10A). The ZTR index is the percentage of the combined zircon, tourmaline, and rutile grains among 13

ACCEPTED MANUSCRIPT the transparent heavy minerals omitting micas and authigenic minerals, which increases as sediments become progressively more quartzose (Hubert, 1962). This index often serves as an

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index to reflect the maturity of detrital rocks and sediment input direction (Cao et al., 2013; Bassis

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et al., 2016). The ZTR indices of the 85 selected samples are shown in Fig. 10B. Their spatial variations show some immediately recognizable trends, increasing from very low values on the basin or sag margin to relatively higher values in the inner basin. In the northern and western basin,

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the samples on the basin (sag) margin display relatively low ZTR indices (between 0 and 30%),

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but the ZTR indices increase to 30% to 100% in the inner part of the basin. Regardless of the limited exploration drillings and samples in the southern and eastern basin, similar trends are still

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observed (Fig. 10B). Some exceptions, such as samples G1, Hu1 and Hu2, are inconsistent with

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these trends.

5. Interpretation and discussion

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5.1 Characterization of potential source areas The orogens and massifs surrounding the Jianghan Basin are all potential sources for the Xingouzui Formation. We tentatively divide them into four areas (Fig. 1B) based on the geographic features and drainage systems. Because the deformations of these tectonic units are complex and the same type of rocks with similar ages which belong to different tectonic units are distributed closely, such as the late Jurassic to early Cretaceous magmatic rocks in the Daye area and those in the Dabie Terrane (Zhang et al., 2008, 2010a; Li et al., 2012b, 2014a). U-Pb age data of the four different potential source areas were summarized using the published data (Fig. 11). 5.1.1 The northern source area 14

ACCEPTED MANUSCRIPT The northern source area is part of the South Qinling Belt (Fig. 1B), mainly including the North Dabashan zone and Wudang terrane. The North Dabashan zone is dominated by Paleozoic

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sedimentary rocks, with a little Precambrian rocks and the Neoproterozoic granites with U-Pb ages

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of 704-797 Ma (Li et al., 2012a; Yang et al., 2012). The Paleozoic sedimentary rocks are a series of carbonate sediments, in addition to the Silurian to Ordovician clastic sedimentary rocks. A series of NW-SE-trending mafic dykes (Wang et al., 2009) are widely distributed in the North

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Dabashan zone with U-Pb age population from 422-443 Ma (Wang et al., 2009; Zou et al., 2011;

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Chen et al., 2014; Cao et al., 2015b; Wang et al., 2015a), indicating back-arc extension in the Silurian (Wang et al., 2015a). The Wudang terrane is mainly composed of the Neoproterozoic

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Wudang and Yaolinghe Volcanic-sedimentary sequences, which are intruded by mafic rocks

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(651±5 Ma, Zhu et al., 2015). The late Triassic granites emplaced at ca. 210 Ma (e.g., Xiao et al.,

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2014) are developed in west of the North Dabashan zone. Zircon age patterns of the northern source area is displayed in Fig. 11A. The northern source area mainly contains 400-500 Ma and

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700-1000 Ma zircons and are a likely source of this aged detritus of the Xingouzui Formation. 5.1.2 The eastern source area The eastern source area consists of the eastern part of the South Qinling Belt, the Dabie Terrane and the Daye region (Fig. 1B). The area is mainly comprised of the Neoproterozoic low-grade metasedimentary rocks and the late Jurassic to early Cretaceous magmatic rocks. The Neoproterozoic rocks define two major age populations: 700-900 and 1800-2100 Ma (Li et al., 2010; Xue and Ma, 2013; Liu et al., 2014; Yang et al., 2015, 2016). Paleoproterozoic to Archean ages can be found in the Dabie Terrane (Wu et al., 2008). The late Jurassic to early Cretaceous intrusive and volcanic rocks were formed on the background of the large-scale extension and 15

ACCEPTED MANUSCRIPT magmatism in eastern China driven by the subduction of the Paleo-pacific plate (e.g., Li et al., 2012c, 2014b). The magmatic rocks yielded an age range from 118 to ca. 150 Ma (Zhang and Ma,

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2008; Chen et al., 2009; Li et al., 2009; Xie et al., 2011b). The Dabie Terrane is known for its

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ultrahigh-pressure metamorphic rocks with zircon U-Pb ages of 218-239 Ma (Liu et al., 2007; Wu et al., 2008; Zhou et al., 2011). Age populations of this source area are shown in Fig. 11B and it may mainly contribute 113-158 and 700-1000 Ma detritus to the early Eocene Jianghan Basin.

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5.1.3 The southern source area

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The southern source area, located in the northern margin of the Jiangnan orogen, includes the Huarong granitoids and Mufushan massif (Fig. 1B). The Huarong granitoids are composed of the

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Taohuashan and Xiaomoshan plutons. The emplacement age of Taohuashan and Xiaomoshan

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plutons range from 127 ± 1 to 117 ± 1 Ma (Shen et al., 2012b). The granitoids in the Mufushan

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Massif intruded episodically from ca. 154 to ca. 146 Ma (Wang et al., 2014b). The zircon U-Pb age spectra of the Neoproterozoic meta-sandstones and Paleozoic clastic sedimentary rocks from

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the Mufushan Massif show a major peak at 831 Ma and two sub-peaks at 2007 and 2475 Ma (She, 2007; Yan et al., 2015). Age distributions of the southern source area is shown in Fig. 11C. Sources of 113-158 and 700-1000 Ma zircons from the selected samples are likely derived from this source area. 5.1.4 The northwestern source area As the fold and thrust belt in west of the Jianghan basin is mainly covered by Paleozoic carbonate sediments, the northwestern source area only includes Shennongjia-Huangling massif (Fig. 1B). The Huangling massif is characterized by the Neoproterozoic granitoids that have been deeply incised by the Yangtze River and the zircon U-Pb ages range from 794 to 837 Ma (Ling et 16

ACCEPTED MANUSCRIPT al., 2006; Gao and Zhang, 2009; Zhang et al., 2009). The core of the Huangling massif is the Archean-Paleoproterozoic Kongling complex, unconformably overlain by Neoproterozoic-Early

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Paleozoic strata which contains one major age group of 740-890 Ma and two minor groups of

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1900-2100 and 2400-2550 Ma (Cui et al., 2014). The Shennongjia region located northwest of the Huangling massif consists of the Shennongjia Group in the core and late Neoproterozoic to Phanerozoic strata along its rim. Age populations of the massif give five age clusters with peaks at

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ca.1120, 1600, 1837, 2060 and 2680 Ma, ranging from 1040 Ma to 3360 Ma (Qiu et al., 2011;

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Xiao, 2012; Li et al., 2013a). Age distributions of the northwestern source region are presented in Fig. 11D. The 700-1000 Ma detritus of the early Eocene sediments are likely derived from this

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source area.

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5.2 Provenance analysis

Detrital zircons from seven sedimentary samples in this study have three mainly age

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populations, namely, 113-158, 400-500 and 700-1000Ma (Fig. 11E). The late Jurassic to early Cretaceous ages ranging of 113-158 Ma are consistent with the ages of magmatic rocks widely distributed in the eastern and southern source areas. This suggests that the eastern and/or southern source areas contributed magmatic detritus to the basin. Zircons at 113-158 Ma are mainly prismatic grains implying short-distance transportation from these source regions. The age group of 400-500 Ma is important for consideration of source areas, because it can be interpreted as a signature of the northern source area (Fig. 11A). These zircons at 400-500 Ma were mainly derived from the Silurian to Ordovician clastic sedimentary rocks and the mafic dykes in the northern source area, the North Dabashan zone to be exact, which defines a major age population 17

ACCEPTED MANUSCRIPT of 400-500 Ma (Wang et al., 2009; Duan, 2010; Zou et al., 2011; Chen et al., 2014; Cao et al., 2015b; Wang et al., 2015a). It is unclear where the third age population (700-1000 Ma) was

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derived from just based on the comparison in Fig. 11, since the Neoproterozoic low-grade

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metasedimentary and sedimentary rocks are ubiquitous in all the four potential source areas. Zircons with ages greater than 400 Ma have a larger proportion of sub-rounded to rounded grains than the 113-158 Ma grains, indicating input from these recycle sedimentary sources.

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The proportions of zircon age groups of the selected samples are shown in Table 1. The

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proportions of ages from 400-500 Ma progressively decreased from north to south: 34% in sample M96, 13% in sample H12 and 23%-28% in the samples located between them. This further

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indicates that the Paleozoic ages were mainly derived from the northern margin of the Jianghan

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Basin. The Neoproterozoic ages ranging from 700 to 1000 Ma are in response to the “Jinningian

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Movement” in the Yangtze and Cathaysia Block and may be associated with the breakup of the Rodinian supercontinent (Li et al., 2002). These ages are more abundant in the samples near the

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southern source area (Table 1). This is also shown in Fig. 8, and there are concentrated age distributions between 700 and 1000 Ma in all the samples apart from sample M96. Linking the early Eocene basin architecture (Fig. 4), the zircons with ages of 700-1000 Ma were mainly supplied by the southern source area. The Triassic zircons (200-250 Ma) are the signature of the northern and eastern source areas (Fig. 11A, B), but they are rare in our samples (Fig. 8). It may be because that their source rocks are locally distributed and not exposed widely (HBGMR, 1990). The significant differences of heavy minerals compositions of the analyzed samples (Fig. 9) may be also a result of input from multiple sources. As granitoids are widely distributed in the surrounding source areas except for the north source area, we tentatively attribute the spatial 18

ACCEPTED MANUSCRIPT differentiation of the abundance of rutile (Fig. 10A) to the input of granitoid sources from the eastern, southern and northwestern source areas. The input of granitoid sources from the eastern

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and southern margins of the basin is further evidenced by the occurrence of zircons with ages of

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113-158 Ma. The spatial variations of ZTR indices are marked by some noticeable increasing trends (Fig. 10B), which are confirmed by the variation of the abundance of zircons at 400-500 and 700-1000 Ma (Table 1). We infer that these trends reflect the sediment input directions (Figs.

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10B, 11). Based on the heavy mineral analysis, sources for zircons with ages of 113-158 Ma were

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accurately identified, as well as the northwestern source. In addition, the petrographic features of sandstones in Fig. 5 also provide evidence for these conclusions. Sample C2 is characterized by

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grains with much poorer sorting and roundness and less quartz content than the samples located on

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the northern basin, implying sediment input from the southern margin of the basin. Sample T20 is

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characterized by grains with better sorting and higher content of quartz than samples Hu2 and Ch8, which is in accordance with the spatial variations of ZTR indices.

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Based on the above analysis, we conclude that the early Eocene Jianghan basin has a multiple source system and the provenance of the sediments changes from one part of the basin to another (Fig. 12). The dominant provenance was from the northern margin of the Jianghan Bsain, and the northwestern, eastern and southern source areas also contributed detritus to the basin. The paleogeography and its tectonic implications will be discussed in next section.

5.3 Discussion on paleogeography Detrital zircons and heavy minerals from the Xingouzui Formation in the Jianghan Basin provide abundant information for paleogeographic reconstruction, such as sediment provenance and transport routes. Based on the results of this study and combined with the published works 19

ACCEPTED MANUSCRIPT (Yuan, 2010; Wan et al., 2011; Huang and Yuan, 2013; Li et al., 2015b; Liu, 2015b, 2016b), a provenance model showing the paleogeography of the early Eocene Jianghan basin is made (Fig.

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13).

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During the Xingouzui stage, large-scale deltas and beach and bar systems widely developed in shallow lakes (Wan et al., 2011; Li et al., 2015b; Liu et al., 2016b) (Fig. 13). The northern provenance is imputed through the north rift-troughs, covering nearly half area of the basin.

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However, with increased distance, the northern source diminishes, which is consistent with the

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decrease in the number of zircons with ages from 400-500 Ma (Table 1) and the increase of ZTR indices (Fig. 9B). The sources from east, south which are identified by the distribution of zircons

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of age groups of 113-158 Ma and 700-1000 Ma, provided a minor input of clastic material to the

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basin. Their spatial distributions are further identified by the distributions of heavy minerals

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assemblages, rutile content and ZTR index. The surrounding ranges all contributed detritus to the Jianghan Basin, showing the multiple-sources to sink relations of rift basin in the composite

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basin-mountain system (Wang et al., 2014a, 2015b; Jiang et al., 2015; Liu et al., 2016a; Shao et al., 2016). Furthermore, the early Eocene paleogeography implies that basin architecture and evolution have important influence on sediment dispersal (Fig. 13). The NW-SE to NNW-SSE-trending rift-troughs are the outstanding architecture characteristics of the Jianghan Basin, which acted as sediment-transport pathways. During the second phase of rifting, fault activity decreased markedly during the Xingouzui stage (Fig. 2B, C). The relatively thin and slightly reduced thickness of the Xingouzui Formation (Fig. 12) indicated that the lake water was shallow and broadly extended. The low dip and subdued topography may have promoted long-distance sediment transport, so it is possible that the surrounding sources, 20

ACCEPTED MANUSCRIPT especially the northern source, were transported a long distance within the basin (Figs. 12, 13). By contrast, most areas of the basin were covered by salt, gypsum and mud deposits during the Shashi

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stage when rifting was intensive (Huang and Yuan, 2013). It is obvious that the high salinity of the

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lake water during the Xingouzui stage (Fig. 3) had limited influence on sediment transport, for lake water was more salty during the Shashi stage. Therefore, under the background of steady erosion of the surrounding ranges (Hu et al., 2006; Shen et al., 2012b; Ji et al., 2014), the rift

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architecture and rifting process had an important influence on sediment dispersal of the Xingouzui

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Formation in the Jianghan Basin.

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6. Conclusions

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Multiple source characteristics of the early Eocene Jianghan basin in the composite

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basin-mountain system have been clarified by the combined provenance analysis of detrital zircon U-Pb geochronology and heavy minerals from the Xingouzui Formation. The sediment input was

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from multiple directions and the provenance change from one part of the basin to another. The dominant provenance was from the northern margin of the Jianghan Basin through the north rift-troughs, and the eastern, southern and northwestern source areas also contributed detritus to the basin. The detrital sediments of the Xingouzui Formation are broadly dispersed in the basin. The early Eocene paleogeography implies that rift architecture and rifting process had an important influence on sediment dispersal. This study shows that integrated study on zircon U-Pb geochronology and heavy minerals is a useful and powerful method to identify sediment provenance.

21

ACCEPTED MANUSCRIPT Acknowledgements We are grateful to Jasper Knight, Aitor Cambeses and Annamaria Fornelli for their

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constructive comments and suggestions. We are grateful to Pro. Zhaochu Hu and doctoral

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candidate Tao Luo for their assistance in LA-ICP-MA analysis at the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Wuhan. This work was financially supported by Natural Science Foundation of Hubei Province (2016CFA084), Research

Project

of

China

Petroleum

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Scientific

and

Chemical

Corporation

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(31400032-14-ZC0613-0031) and the Major National Science and Technology Programs, China

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(2016ZX05002-006).

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Fig. 1. Geologic and tectonic sketch maps of the Jianghan Basin region, (A) modified after Chen

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et al. (2013); (B) modified after Mei et al. (2008) and Zhang et al. (2015).

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Fig. 2. Interpreted seismic profiles of the Jianghan Basin, (A) modified after Li et al. (2008). The locations of the seismic profiles are shown in Fig. 1B. Fault active rate = stratigraphic thickness of (footwall-hangingwall) / sedimentation time.

Fig. 3. Basin filling evolution and stratigraphic column for the Jianghan Basin, modified after Wang et al. (2006). The salinity data are from Fang (2006).

Fig. 4. Map showing the locations of selected samples for zircon U-Pb dating and heavy mineral analysis. The new data from Research Institute of Exploration and Development of Jianghan 42

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Fig. 5. Representative photomicrographs of selected samples for heavy mineral analysis. Q, quartz; Pl, plagioclase; Mus, muscovite; Dol, dolomite; Anh, anhydrite; Tou, tourmaline. A, sample Hu2;

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Fig. 6. Stratigraphic columns of the sampled well-sections for zircon U-Pb dating of the

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Xingouzui Formation. The well locations are shown in Fig. 4.

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Fig. 7. Representative Cathodoluminescence (CL) images showing internal structure and morphology of detrital zircons from the Xingouzui Formation. The circles represent U-Pb

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analytical sites and their diameters are 32 μm.

Fig. 8. U-Pb Concordia age plots and relative age probability diagrams for detrital zircons from the Xingouzui Formation. Data-point error ellipses are 1σ.

Fig. 9. Heavy mineral assemblages of samples from the Xingouzui Formation from the Jianghan Basin.

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zircon-tourmaline-rutile. The zircon U-Pb studied samples are highlighted in bold character. 43

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Fig. 10. Spatial variations of the content of rutile and zircon-tourmaline-rutile (ZTR) index of the

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Fig. 11. Zircon U-Pb age probability density plots of the potential surrounding source areas and summary of the samples. Data for the northern source area are (from Cai et al., 2007; Wang et al.,

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2009; Duan, 2010; Ling et al., 2010; Zhang et al., 2010b; Zou et al., 2011; Li et al., 2012a; Yang et

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al., 2012; Hu, 2013; Chen et al., 2014; Cao et al., 2015b; Xiao et al., 2014; Wang et al., 2015a; Zhu et al., 2015). Data for the eastern source area are (from Ma et al., 2004; Xue et al., 2004; Liu

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et al., 2009; Li et al., 2009, 2010, 2012b, 2014a; Liu et al., 2010a; Wang et al., 2010; Zhang et al.,

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2010a; Xie et al., 2011b; Zhou et al., 2011; Hu et al., 2012; Jian et al., 2012; Xu et al., 2012; Xue and Ma, 2013; Liu et al., 2014; Yang et al., 2015, 2016 ). Data for the southern source area are

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(from She, 2007; Shen et al., 2012b; Wang et al., 2014b; Yan et al., 2015). Data for the northwestern source area are (from Xiong et al., 2008; Jiao et al., 2009; Zhang et al., 2009; Qiu et al., 2011; Xiao, 2012; Cen et al., 2012; Li et al., 2013a; Zhao et al., 2013b; Cui et al., 2014).

Fig. 12. Possible provenance directions and sediment routing system of the Jianghan Basin during the early Eocene. The sequential isopach map shows original stratigraphic thickness of the Xingouzui Formation. Different coloured arrows represent different source areas.

Fig. 13. Simplified paleogeographic and dynamic model of the Jianghan basin during the early 44

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Table 1 Proportions of detrital zircon age groups of the selected samples.

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Age group (Ma) Sample 399-172

500-400

689-501

1000-700

M96

0.30

0.05

0.34

0.03

0.10

0.18

100%

Yx2-Y1-Y1x-1

0.26

0.06

0.28

0.04

0.14

0.22

100%

Jx9

0.26

0.07

0.23

0.01

0.27

0.17

100%

CC-1

0.19

0.06

0.28

0.03

0.19

0.25

100%

H12

0.28

0.08

0.13

0.08

0.24

0.21

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Detrital zircon U-Pb geochronology and heavy mineral analysis are used in combination.

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Spatial framework of sediment dispersal is identified.

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Multiple source characteristics of rift sediments in the composite basin-mountain system are clarified.

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Rift architecture and rifting process have an important influence on sediment dispersal.

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