Marine Geology 355 (2014) 202–217

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Marine Geology

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Provenance of Upper Miocene to Quaternary sediments in theYinggehai-Song Hong Basin, South China Sea: Evidence fromdetrital zircon U–Pb ages

Ce Wang a,b, Xinquan Liang a,⁎, Yuhong Xie c, Chuanxin Tong c, Jianxiang Pei c, Yun Zhou a,b, Ying Jiang a,b,Jiangang Fu a,b, Chaoge Dong a,b, Ping Liu c

a State Key Laboratory of Isotope Geochemistry, Guangzhou Institute of Geochemistry, Chinese Academy of Sciences, Guangzhou 510640, Chinab University of Chinese Academy of Sciences, Beijing 100049, Chinac China National Offshore Oil Corporation Ltd., Zhanjiang 524057, China

⁎ Corresponding author. Tel.: +86 20 85290113.E-mail address: liangxq@gig.ac.cn (X. Liang).

http://dx.doi.org/10.1016/j.margeo.2014.06.0040025-3227/© 2014 Elsevier B.V. All rights reserved.

a b s t r a c t

a r t i c l e i n f o

Article history:Received 22 November 2013Received in revised form 3 June 2014Accepted 4 June 2014Available online 14 June 2014

Keywords:U–Pb geochronologydetrital zirconprovenanceYinggehai-Song Hong BasinSouth China Sea

The Yinggehai-Song Hong (Y-SH) Basin, located on the northwestern shelf of the South China Sea, is one of theworld's largest pull-apart basins. In order to identify the provenance of the Upper Miocene to Quaternarysediments of the basin, ten sediment samples were collected from drill cores in the Dongfang gas field. U–Pbdating of detrital zircon grains extracted from the ten samples using a laser ablation inductively coupled massspectrometer (LA-ICP-MS) yields ages ranging from the Archean to Cenozoic (2898 ± 46 Ma to 26 ± 1 Ma).The zircon U–Pb age spectra of the Upper Miocene to Quaternary show a similar pattern with major peaksclustered at ca. 32 Ma, ca. 99 Ma, ca. 160 Ma, ca. 247 Ma, ca. 422 Ma and three “broad” age groups,600–1000Ma, 1700–2100 Ma and 2200–2800 Ma, suggestive of a wide range of igneous rock ages in the sourceareas. The detrital zircon ages provide diagnostic criteria for identification of the various source areas and revealthat the detritus was derived frommultiple sources. Comparison of the results with the rock types and their agessurrounding the potential source areas indicates that the clastic material was derived from three dominant agesources: (1) Yangtze Craton, (2) Hainan Island and (3) Indochina Block. The Yangtze Craton was a major andcontinuous source area contribution to the basin. Comparing the age characteristics and its source areas since10 Ma, the largely stable provenance also suggests that if the Red River capture ever existed it should havehappened before the Late Miocene.

© 2014 Elsevier B.V. All rights reserved.

1. Introduction

Provenance studies of sedimentary rocks are important to basinanalysis, oil and gas exploration. Traditional petrography, heavymineralanalysis and sequence stratigraphic methods cannot distinguish thesource area effectively, especially in the source complex regions. Inrecent years, sedimentary provenance technology has been improvedby single grain radiometric dating of grain populations, for exampledetrital zircon U–Pb dating (Cawood and Nemchin, 2000; Fonnelandet al., 2004; Morton et al., 2008; Beltrán-Triviño et al., 2013). Zircon asa kind of stablemineral canwithstand the effects of weathering, erosionand thermal alteration (Cherniak and Watson, 2001; Košler andSylvester, 2003), and possess a stable U–Pb isotopic system overa wide range of pressures, temperatures and fluid composition(Moecher and Samson, 2006; Zhao et al., 2013). The data of detritalzircon can provide more accurate and useful information of source

areas, which makes it a powerful tool for basin provenance analysisthat has been widely used all over the world in the last decade.

The provenance of the Yinggehai-Song Hong (Y-SH) Basin is inter-esting because of the importance in hydrocarbon exploration, but isalso a poorly understood provenance because of its complexity. Theunderstanding of sediment provenance and its transport routes is akey element in establishing reservoir presence in clastic petroleumsystems (Morton et al., 2001), because reservoir quality of sandstonesin sedimentary basins is significantly influenced by the detrital compo-sitions which mainly respond to the provenance distribution (e.g. Rossiet al., 2002). Valuable information about sedimentary direction duringdeposition is gained by reconstructing transport pathways, whichprovide useful knowledgewhen trying to locate hydrocarbon explorationtargets (Olivarius et al., 2014). Most published works on the provenanceof the Y-SH Basin have focused on the heavy minerals, sequence strati-graphic analysis, geochemistry and seismic profiles (Gong et al., 1997;Wu, 1997; Huang et al., 2003; Yan et al., 2007; Xie et al., 2008; Xie,2009; Xie and Fan, 2010; Lei et al., 2011; Wei et al., 2012). Gong and Li(1997) analyzed the sedimentary facies of the Y-SH Basin and suggestedthat Offshore Indochina and Hainan were important source areas since

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LateMiocene. Yan et al. (2007) used geochemical andNd isotopic analysisfor sedimentary rocks to constrain the provenance. The results show thatthe Huangliu to Ledong Formations were erosion of older continentalinterior sources, mostly from Indochina to the west of the South ChinaSea. Xie (2009) and Xie and Fan (2010) argued that the provenancewas changing since Late Miocene in Dongfang gas field using methodsof heavy mineral analysis and seismic profiles. They proposed that theHuangliu Formation was mainly from northern Vietnam (Red River),while the Yinggehai Formation was from Hainan Island and northernVietnam. Wang et al. (2013) suggested that the Huangliu Formation inDongfang gas field derived from central Vietnam by several drainages(e.g.MaRiver, Song River) based on seismic profiles and regional geology.All of these studies greatly enhance our understanding of the provenanceof theDongfang gasfield. However, the provenance of theUpperMioceneto Quaternary is still controversial because the basin involved a varietysources and lacks of precise geochronologic data to limit it. Up to now,only a fewzircon grains from the easternmargin of the basin have yieldedU–Pb ages of 90 to 110 Ma and 225 to 275 Ma, which revealed theprovenance of the Hainan Island, China (Yan et al., 2011a).

In this paper, we report the U–Pb isotopic compositions of detritalzircons by laser ablation inductively coupled plasmamass spectrometry(LA-ICP-MS) to provide an initial framework for understanding theprovenance of Upper Miocene to Quaternary sediments from theDongfang gas field in the Y-SH Basin. The objectives of this studyare to: (a) identify their source areas; (b) define the possible sedimen-tary supply routes; and (c) test the models for drainage evolution ineastern Asia.

Fig. 1. Geologic sketch map of the Yinggehai-Song Hong Basin region, (A) Modified after (TapModified after (Huang et al., 2005; Lei et al., 2011).

2. Geological setting

The Y-SH Basin, located on the continental shelf at water depths of50–200 m in the northwestern South China Sea (Fig. 1A), is one of thelargest Cenozoic pull-part basins in the world (Gong and Li, 1997;Huangetal.,2005;CliftandSun,2006). It covers an area of about 500 × 60 km2

(Zhang and Zhang, 1993; Luo et al., 2003) with the long axis orientednorth-northwest to south-southeast and bordered by Beibuwan andQiongdongnan basins on the north and east, respectively (Fig. 1B). Thebasin developed in response to the southeastward strike-slip faultsand clockwise rotation of the Indochina Block as a result of India–Asiacollision (Molnar and Tapponnier, 1975; Tapponnier et al., 1986; Guoet al., 2001; Sun et al., 2003; Yan et al., 2011a) (Fig. 1A).

The Y-SH Basin is characterized by its large volumes, subsidencerate, overpressures (Zhang et al., 1996; Luo et al., 2003; Huang et al.,2009a), andwidely developeddiapirs in the central YinggehaiDepressionwhich have been recognized by its great significance in gas explorationand production (Xie et al., 2001; Wang and Huang, 2008; Huang et al.,2009a; Lei et al., 2011) (Fig. 1C). The basin contains large thickness ofthe Paleogene toQuaternary sedimentary rocks, up to 17 km in the centerwhere the Pre-Paleogene crust thickness is estimated to be about 5 km,the bulk of which was deposited since 35 Ma (Gong et al., 1997; Yanet al., 2011a).

According to the conventional seismic stratigraphies and boreholesusing the method of back stripping, two stages of subsidence thatoccurred in central part of the basin have been recognized since theEocene: a Paleogene transtensional (Rangin et al., 1995) and a Neogene

ponnier et al., 1990; Leloup et al., 1995; Gilley et al., 2003; Zhu et al., 2009); (B) and (C)

Fig. 2. Interpreted seismic profile of the Y-SH Basin whose position is shown in Fig. 1. Modified after (Sun et al., 2003; Xie, 2009).

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post-rift thermal subsidence (Gong et al., 1997; Zhang and Hao, 1997;He et al., 2002; Huang et al., 2009a) (Fig. 2). The basin experiencedtwo inversion phases that occurred at ca. 34 and ca. 15.5 Ma (Rangin

Fig. 3. Regional stratigraphic columnar section of the Y-SH Basin, m

et al., 1995; Hoang et al., 2010), the former coincident with the onsetof motion on the Red River Fault Zone (Hoang et al., 2010) while thelater may have responded to the cessation of sea-floor spreading in

odified after (Gong et al., 1997; Huang et al., 2003; Xie, 2009).

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the South China Sea (Rangin et al., 1995). The sediment infill of thecentral Yinggehai depression by the Neocene to Quaternary clasticdeposits varies from lacustrine, coastal plain and neritic (before30 Ma), littoral to neritic (30–10 Ma) and littoral to neritic (10–5 Ma)environments (Fig. 3). The seismic reflection data show that thesedimentation rates of the basin increased from 29.5 to 21 Ma, fellfrom 21 to 15.5 Ma, and rose once more from 15.5 to 10.5 Ma withpeak sedimentation rates in the Plio-Pleistocene (Clift and Sun, 2006;Hoang et al., 2010).

Two gas fields, including the Dongfang field and Ledong field, and anumber of gas-bearing structures have been discovered since 1990(Gong et al., 1997; Xie, 2009). The Dongfang field is an important gasfield in the basin, includes the largest gas reserve DF1-1 gas field andseveral other gas-bearing structures (Fig. 1C). The gases accumulateprimarily in theUpperMioceneHuangliu Formation, Pliocene YinggehaiFormation and Quaternary Ledong Formation (Fig. 3). The HuangliuFormation is the main reservoir of the Dongfang gas field with amaximum thickness of 780 m and consists mainly of mudstone, siltymudstone, limestone and argillaceous siltstone. The Yinggehai Formationis composed by mudstone, siltstone, silty mudstone and argillaceoussandstone with a maximum thickness of 2200 m. The Ledong Formationconsists of gray clay, mud and gravel and debris with a maximumthickness of 1200 m (Fig. 3).

The sediments of the Y-SH Basin were delivered by several drainagesystems (such as Red River and Ma River in Vietnam, and ChanghuaRiver in Hianan, China) (Fig. 4), but the main input river is Red River(Song Hong) and its tributaries. The modern Red River, which drainsan area of 160 × 103 km2 (Milliman et al., 1995), is one of the majorcontinental discontinuities in Southeast Asia. The river originates inthe mountains of Yunnan Province, China, and flows about 1200 kmfrom southeast Tibet to the Tonkin Gulf, South China Sea. At present,the Red River consists of the major channel and two big tributaries:Chay/Lo and Da rivers (Fig. 4). The total sediment and water dischargeof the Red River is 100–130 million t/yr and 120 km3/yr (Millimanet al., 1995; Pruszak et al., 2002), respectively, and the average sediment

Fig. 4.Major geological blocks and drainage systems

concentration in the river is 1.08 kg/m3 (Tanabe et al., 2006). The RedRiver catchment now is composed of different geological blocks(Fig. 4) and can be consideredmuch larger if when used to be connectedto the Yangtze and other rivers (e.g. Clark et al., 2004; Clift et al., 2006a;Hoang et al., 2009). Modern Red River drains through the NNW strikeRed River Fault Zone (RRFZ) which located in south margin of theYangtze Craton (Fig. 1A). The RRFZ for about 1000 km from southeastTibet to the Tonkin Gulf is one of the major continental discontinuitiesin Southeast Asia. The sinistral strike-slip is in excess of 500 km,verified by the theoretical and experimental work of Tapponnieret al. (1982). Four main metamorphic belts that crop out along thelength of the fault zone are the Xuelong Shan (XLS), Diancang Shan(DCS) and Ailao Shan (ALS) in Yunnan, southern China, and theDav Nui Con Voi (DNCV) complex in northern Vietnam (Fig. 1A).Each metamorphic belt is very long and narrow (10–20 km wide)and bounded by strike-slip faults. The RRFZ has been affected by atleast two major metamorphic–orogenic events responding to theCaledonian and Indosinian which have been dated at ca. 430 Maand ca. 250 Ma, respectively.

3. Sampling and analytical methods

3.1. Sampling

Ten sedimentary rock samples in this study were collected fromthree marine drill cores of the Dongfang gas field (Fig. 1C) used todirectly constrain the sediment provenance of Upper Miocene toQuaternary in the Y-SH Basin. The sediments consist mainly of siltstone,sandstone, argillaceous sandstone and silty mudstone (Fig. 5). SampleDF1312-1 was collected from the Ledong Formation, DF1112-1,DF1313-1, DF1313-2, DF1312-2 and DF1312-3 were collected fromthe Yinggehai Formation, and DF1112-2, DF1313-4R, DF1312-9R andDF1312-10 were collected from the Huangliu Formation. The locationsand stratigraphic information are given in Table 1.

in SE Asia, modified after (Hoang et al., 2009).

Fig. 5. Stratigraphic column and sample position of DF1112, DF1312 and DF1313 wells in the Y-SH Basin with positions of samples marked. Positions of the core drill are shown in Fig. 1C.

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3.2. Zircon U–Pb geochronology

Zircon U–Pb dating analyses were performed on polished grainmounts by laser ablation inductively coupled plasma mass spectrometry(LA-ICP-MS). Zircons were separated by using heavy liquids and a Frantzmagnetic separator at the Langfang Regional Geological Survey, HebeiProvince, China. Following final purification by hand sorting zircon grainswere mounted in epoxy and polished down to near half sections toexpose internal structures.

Cathodoluminescence (CL) imaging of zircon grains was carried outusing a Mono CL3 detector (Gatan, U.S.A.) attached to an ElectronMicroprobe (JXA-8100, JEOL, Japan), to identify internal structures andselect target sites for laser ablation analyses. Zircons were dated usingLA-ICP-MS housed at the State Key Laboratory of Isotopic Geochemistry,Guangzhou Institute of Geochemistry, Chinese Academy of Sciences(GIGCAS). Sample mounts were placed in the two-volume sample cellflushed with He and Ar. The laser ablation was operated at a constantenergy 80 mJ and at 8 Hz, with a spot diameter of 31 μm. The ablated

Table 1Location and stratigraphic information of samples analyzed during this study. The well positions are shown in Fig. 1C.

Sample No Lithology Material Age Formation Well Depth

DF1112-1 Siltstone Core Pliocene Yinggehai DF1112 1370–1372 mDF1112-2 Siltstone Core Late Miocene Huangliu DF1112 2670–2674 mDF1313-1 Silty mudstone Core Chip Pliocene Yinggehai DF1313 1105 mDF1313-2 Siltstone Core Chip Pliocene Yinggehai DF1313 1350–1353 mDF1313-4R Sandstone Core Late Miocene Huangliu DF1313 2898 mDF1312-1 Sandstone Core Chip Quaternary Ledong DF1312 830 mDF1312-2 Argillaceous sandstone Core Chip Pliocene Yinggehai DF1312 1120–1122 mDF1312-3 Argillaceous sandstone Core Pliocene Yinggehai DF1312 2191–2193 mDF1312-9R Sandstone Core Late Miocene Huangliu DF1312 2600–2605 mDF1312-10 Sandstone Core Chip Late Miocene Huangliu DF1312 3140 m

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materialwas carried by theHe gas to theAglient 7500a ICP-MS. Elementcorrections were made for mass bias drift, which was evaluated byreference to standard glass NIST SRM 610. The Temora was used asthe age standard (206Pb/238U = 416.8 Ma) (Black et al., 2003). Trace-element concentrations were obtained by normalizing count rates foreach analyzed element to those for Si, and assuming SiO2 to be stoichio-metric in zircon. The details of precision, accuracy and analytical

Fig. 6. Cathodoluminescence images of selected detrital zircons of the samples from the Y-SH Bare 31 μm in length for scale.

procedure are described in Jackson et al. (2004), Yuan et al. (2004)and Liu et al. (2010).

Generally, 206Pb/238U ages aremore precise for younger ages, whereas207Pb/206Pb ages are precise for older ages. 206Pb/238U ages less than1000 Ma are used, and 207Pb/206Pb ages are selected if the 206Pb/238Uages are more than 1000 Ma. Ages which have more than ±10%discordance were rejected in this study. Isotopic ratios of U–Th–Pb were

asin. The spots and numbers indicate analytical sites and U–Pb ages respectively. The spots

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calculated using ICPMSDataCal (Liu et al., 2008; Liu et al., 2010). CommonPb was corrected by ComPbCorr#3_151 using the method of Andersen(2002). The age calculation and concordia age plots were made usingISOPLOT (Version 3.0) (Ludwig, 2003). Data points are displayed onconcordia age plots as filled error ellipses, with all errors reported at the68.3% (ca. 1σ) confidence level, which show the accuracy and analyticalprecision.

4. Results

The morphology of zircon grains from core samples in this studyshowed a wide range from prismatic crystals to oval- and irregular-shaped zircon with mostly rounded corners (Fig. 6), suggestive ofzircons from long distances. Some grains are incomplete which maymean that have been damaged during transport. Most grains are oscilla-tory growth zoning under CL (Fig. 6), someofwhich are opaque becausetheir Th and U content are too high. Among 740 zircon grains analyzed,686 were concordant or slightly discordant ( 10%). All but 33 measure-ments show Th/U 0.10 and another 653 zircons have Th/U ratios rangingfrom 0.10 to 3.40. These features indicate that the majority of theanalyzed zircons are of magmatic origin (Belousova et al., 2002; Corfuet al., 2003; Wu and Zheng, 2004; Li et al., 2012). Zircon grains in allsamples have a wide age range from the Archean to Cenozoic, suggestiveof awide range of igneous rock ages in the source areas (Choi et al., 2013).The oldest zircon age is 2898 ± 26 Ma and the youngest zircon grain is26 ± 1 Ma. Age data of each sample are shown on concordia age plotsand relative age probability diagrams (Fig. 7), and presented in detailin Appendix A.

5. Discussion

5.1. Potential sources for the sedimentary rocks

Source area surrounding the basin is a priori potential provenancefor the accumulated clastic material (Bruguier et al., 1997). The YangtzeCraton, Indochina Block and Hainan Island are all potential source areasfor the Y-SH Basin since the Late Miocene (Fig. 1A). The rock types andtheir ages are themost useful information on the potential source areas.U–Pb age data was summarized using existing data from differentpotential source areas and drainages surrounding the Y-SH Basin(Figs. 8 and 9). These diagrams compile a large volume of publisheddata. The distribution of igneous rocks surrounding the Y-SH Basin isshown in Fig. 10.

5.1.1. Southern Yangtze CratonThe South China Block is a composite terrane which was formed by

amalgamation of Yangtze and Cathaysia block in Proterozoic (Rowleyet al., 1989; Li et al., 1995;Wang et al., 2007; Li et al., 2009). The YangtzeCraton located in southwestern of China, and is separated from theCathaysia and Indochina by the Jiangnan suture and Song Ma Sutureto the east and south, respectively. The craton shows a wide-rangezircon age pattern (Fig. 8A). The basement rocks of the Yangtze Cratonare mainly of Early Proterozoic (1700–2100 Ma) and Archaean(2300–2800Ma) ages (e.g. Metcalfe, 2006). The Archaean is dominatedby sodium-rich granitoids of tonalite–trondhjemite–granodiorite (TTG)suites (Martin, 1987; Chen et al., 2013). A large part of the YangtzeCraton comprised by the Neoproterozoic dates termed the “JinningianMovement (700–1000 Ma)” (Chen and Jahn, 1998; Chen et al., 2001;Huang et al., 2009b). The mid-Neoproterozoic age between 750 and900 Ma is well established (Ling et al., 2003; Wang et al., 2007; Wanget al., 2010), which probably is associated with the breakup of Rodinia(Li et al., 2002; Ling et al., 2003; Yan et al., 2011a). Numerous data of

Fig. 7. U–Pb concordia age plots and relative age probability diagrams for detrital zircons fromPliocene Yinggehai Formation and (F)–(J): Upper Miocene Huangliu Formation. Data-point err

high-temperature shear and magmatism are available from the RedRiver Fault Zone which is located in the southern Yangtze Craton(Fig. 1A), and yield U–Pb ages between 20 and 60 Ma (Leloup et al.,1995; Zhang and Schärer, 1999; Liu et al., 2013).

5.1.2. Eastern Indochina BlockThe Indochina Block, individualized by the opening of different

branches of the Paleo-Tethyan ocean (Metcalfe, 1996; Lepvrier et al.,2008), is a Gondwana-derived terrane. The eastern margin of theIndochina is composed of the Truong Son Belt and Kontum massif(Fig. 1A). The Truong Son Belt mainly consists of Precambrian toMesozoic sedimentary rocks and the early Permian to Triassic granitoidsare widely distributed with age population from 202 to 276 Ma (Liuet al., 2012). The Kontum massif is mainly comprised of high grademetamorphic rocks and plutonic rocks. The granitoids of the massifyielded an age range from ca. 240 Ma to ca. 450 Ma (Carter et al.,2001; Nagy et al., 2001; Roger et al., 2007; Usuki et al., 2012). Theamphibolite facies igneous rocks from Kontummassif record amagmaticevent at ca. 451 Ma (Nagy et al., 2001; Roger et al., 2007), and granulitefacies terrain yield age clusters between 245 and 250 Ma (Roger et al.,2007). Age population of the block is shown in Fig. 8B.

5.1.3. Hainan IslandHainan Island, located in the southern end of the Cathaysia Block, is a

continental-type island (Xu et al., 2007b) (Fig. 1A). The island is domi-nated by Permain to Mesozoic granitoids, with rare Precambrian andPaleozoic rocks. The ca. 1430 Ma Precambrian volcaniclastic rockshave been discovered in Baoban area (Fig. 10) that may be associatedwith the Grenvillian Orogenic event (Xu et al., 2007a; Li et al., 2008).The Permain to Triassic A-type and I-type granitoids are developed inthe island, with U–Pb ages of 230–270 Ma (Li et al., 2006; Wen et al.,2013). The Cretaceous granitoids and volcanic rocks are mainly concen-trated in the south of Hainan Island, the ages of which range from 90 to110 Ma, with a peak at ca. 99 Ma to the dated detrital zircons (Wanget al., in press). The Late Early Cretaceous adakitic intrusive rocks yieldan age of 107 Ma in the Tunchang area (Jia et al., 2010).

5.2. Detrital zircon provenance analysis

The zircon U–Pb data from the Upper Miocene to Quaternary coresamples taken from boreholes drilled of the Dongfang gas field yield awide range in crystallization ages (2898 ± 46 Ma to 26 ± 1 Ma),which generally reveal a wide variety of sources. The zircon age distri-butions are subdivided into nine groups from Cenozoic to Archean(Table 2). Notably, the Ledong, Yinggehai and Huangliu Formationsshow strong similarities in age structure of their populations (Figs. 11and 12), indicative of similar provenance for the samples. Zircon U–Pbages of the total give eight age clusters with peaks at ca. 32 Ma, ca.99Ma, ca. 160Ma, ca. 247Ma, ca. 422Ma and three “broad” age groups:600–1000 Ma, 1700–2100 Ma and 2200–2800 Ma (Fig. 8D). Thesedimentology, geochemistry and seismic profile analysis have revealedthat the sediment sources are from the northwest, west and east of thebasin (Gong et al., 1997; Yan et al., 2007; Xie, 2009; Hoang et al., 2010;Xie and Fan, 2010), and delivered by many drainage areas. The maindrainages into the basin are from the Red River and its main tributaries(Da and Lo/Chay rivers) which developed in the southern margin of theYangtze Craton (Figs. 4 and 10).

The Cenozoic zircons (ca. 32Ma) in different samples imply a sourcefrom the Red River Fault Zone in southern Yangtze Craton with thehigh-grade metamorphic rocks, which have been dated in the range of20–60 Ma (Fig. 8A) (Zhang and Schärer, 1999; Leloup et al., 2001;Gilley et al., 2003). The age range and extremely narrow distribution

the Dongfang gas field sediment samples. (A): Quaternary Ledong Formation; (B)–(E):or ellipses are 1σ.

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of grains are related tomelting and exhumation triggered by motion onthe Red River Fault Zone (Hoang et al., 2009; Liu et al., 2013). TheCenozoic zircon grains are only minor in the age structure, suggeststhat the Red River Fault Zonewas not themajor provenance contributorto the basin even though there was deep exhumation.

The Late Jurassic–Cretaceous zircon grains coincide with the ages ofYanshanian granites which are mainly present on Hainan Island (Yanet al., 2011a). The zircon ages between 80 Ma and 170 Ma have beenrecognized in western Hainan (Wang et al., 1991; Wei et al., 2011),and are mainly exposed in southeast of Baisha Fault. Even though theCretaceous zircon ages had been found in the modern Red River, north-west of the basin, they are younger than 90 Ma (Clift et al., 2006b). TheYanshanian zircons (80–180 Ma) were likely derived from the adjoiningHainan Island, east of the basin.

Fig. 8. Zircon U–Pb age probability density plots of themajor potential source areas and summa1999; Ling et al., 2003; Nam et al., 2003; Zhou et al., 2006;Wang et al., 2007; Xiao et al., 2007; ZhIsland is from (Wang et al., 1991; Xie et al., 2005; Li et al., 2006; Xie et al., 2006; Xu et al., 2007a,for Indochina Block are from (Carter andMoss, 1999; Carter et al., 2001; Nagy et al., 2001; Cart2014).

Abundant ages of around 247 Ma were obtained from the Dongfanggas field strata among the detrital samples consistent with the ages ofthe “Hercynian–Indosinian Movements”. The highest age probability isrelated to Indochina and South China collision and subsequent lateralextrusion of Indochina (Şengör et al., 1988; Lu et al., 1999; Lepvrieret al., 2008; Hoang et al., 2009). However, there are some controversiesabout the provenance of the prominent ages. The main reason is thatthis range of ages is so ubiquitous (including Hainan Island, southernYangtze Craton and Indochina Block) that it has limited potential as adecisive source indicator. Zircon grains in this range were the predom-inant components of the basin which revealed that the Hercynian–Indosinian granites surrounding the basin existed widely and wereeroded. In spite of this, only Hainan Island and Indochina Block areconsistent with the age peak at ca. 247 Ma (Li et al., 2002; Xie et al.,

ry of the samples. Data for southern Yangtze Craton are from (Li, 1999; Zhang and Schärer,ou et al., 2007; Cao et al., 2011; Yang et al., 2012; Żelaźniewicz et al., 2013). Data for Hainanb; Li et al., 2008; Jia et al., 2010;Wang et al., 2011; Yan et al., 2011a;Wen et al., 2013). Dataer and Bristow, 2003; Roger et al., 2007; Liu et al., 2012; Roger et al., 2012; Kamvong et al.,

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2005, 2006; Wen et al., 2013) (Fig. 8). It is not easy to preciselydistinguish the Hercynian–Indosinian provenance among the sourceareas; however, we can easily draw an inference that Hainan Islandand Indochina Block make a significant contribution to the ages ofHercynian–Indosinian (220–270 Ma).

Fig. 9. Zircon U–Pb age probability density plots of the sedimentary rocks and modern sedimeet al., 2009); (B) Sediments from Modern Red River (Clift et al., 2006b; Hoang et al., 2009); (C2011a); (D) Sediments from modern revers in western Hainan (Wang et al., in press); (E) Tota

The age around 422Ma corresponds to the global tectonic–magmaticevent termed the “Caledonian Orogeny” which in Eastern Asia isexpressed by a number of Early Paleozoic magmatic events and meta-morphism that have been attributed to collision between North ChinaCraton and Yangtze Craton (Li, 1998; Lu et al., 1999; Hoang et al., 2009).

nts. (A) Upper Miocene sedimentary rock in Yen Bain Basin, Red River Fault Zone (Hoang) Middle Miocene to Pliocene sediments in eastern margin of the Y-SH Basin (Yan et al.,l of the samples.

Fig. 10. Regional igneous rocks distribution and possible provenance model of the Upper Miocene to Quaternary sediments for the Y-SH Basin. The arrows point to the direction ofprovenance.

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The Caledonian grains are rare and poorly understand in Hainan Island(the igneous rocks with the ages have not been found). Such ages in thesouthern Yangtze Craton and the Indochina Block range from 420 to520 Ma (with a peak at ca. 432 Ma) and 400 to 540 Ma (with a peak atca. 469 Ma), respectively (Fig. 8 and its references).

The Neoproterozoic ages (700–1000 Ma) coincided with“Jinningian Movement” in South China. The Eshan K-rich granitoidsyield ages of ca. 813 Ma (Li et al., 2003) and are present in centralYunnan, South China, which crops out over 200 km2 to the south ofEshan Country (Fig. 10), and the volcanic rocks along the southernto southeastern margin yield ages around 810 Ma (Li et al., 2003, 2005;Ling et al., 2003). The Neoproterozoic age range of 700–1000 Ma is rareor absent in other source areas and can be interpreted as a signature ofthe Yangtze Craton.

The “broad” age group of 1700–2100 Ma correspond to the tectonicevent termed the “Luliangian Movement” (Wang et al., 2007; Yanget al., 2012). A number of zircon U-Pb ages clustering around this periodhave been reported for sedimentary rocks in southern YangtzeCraton (Fig. 8A and its references). Another “broad” age group of2200–2800 Ma has been suggested to the basement sedimentarysequences of the Yangtze Craton (Chen and Jahn, 1998; Wang et al.,2007; Yan et al., 2011b) which could be obtained from southern YangtzeCraton through the Red River and its tributaries, northwest of the Y-SHBasin. The older age also can be observed in the Hainan Island andIndochina Block (Xu et al., 2007b; Li et al., 2008), but they do not account

for an important portion of the total. The most probable provenance ofthe two “broad” age group were derived from the Yangtze Craton.

Although Songpan-Garze fold belt as a distant source area has beenfound in the modern Red River, Hoang et al. (2009) believed that thematerial is mostly reworked via younger sedimentary rocks in themodern Red River. However, our data did not provide a valid indicatorto confirm the presence provenance of the Songpan-Garze.Most studieshave evidence to suggest that Red River drainage occurred by rivercapture and surface uplift in eastern Tibet that predated the LateMiocene (Clift et al., 2002; Clark et al., 2004, 2005; Clift et al., 2006a;Yan et al., 2011a), which means that if the provenance of theSongpan-Garze has existed in the samples, the most likely explanationis the clastic material from the Songpan-Garze to Y-SH Basin by thecontribution of input from recycled sources. The detrital zircon U–Pbages cannot distinguish between the first-cycle and the multi-cyclezircons so that we are unable to constrain the influence of the Songpan-Garze.

The Qiangtang Block is one of the largest HP metamorphic beltswithin Tibet (Fig. 4). The block is largely characterized by a populationcentered at ca. 210 Ma with a few older grains (800–1100 Ma and ca.2200Ma) (Clift et al., 2006b; Hoang et al., 2009). The younger Indosinianages have also been discovered in other blocks (e.g. Indochina), whichmeans that we can't directly use it to constrain the provenance of theQiangtang Block. Because the ages are very few in the samples of themod-ern Red River (Hoang et al., 2009), we infer that if the grains were

213C. Wang et al. / Marine Geology 355 (2014) 202–217

derived from the Qiangtang Block they were reworked via sedimentarybasins along the Red River.

The Cathaysia Block has awide range of ages, mostly in 800–1900Ma,with a large peak at ca. 1450Ma (Li et al., 1989, 2002; Hoang et al., 2009),the age of granitoids and felsic volcanic rocks were discovered in HainanIsland, which may be associated to the Grenvillian Orogenic event (Xuet al., 2007a; Li et al., 2008). The sedimentology and seismic profileanalysis reveal that there were no sediment sources from southeast andthe detrital material of the Cathaysia Block was blocked by the BeibuwanBasin located in the north boundary of the Y-SH Basin (Fig. 1B). It isunsurprising that there is absence of zircon ages around 1450 Ma in thesamples.

Linking the sequence stratigraphic, seismic profile (Gong et al.,1997; Xie, 2009; Lei et al., 2011) and detrital zircon age spectrum ofsamples from the Dongfang gas field in Y-SH Basin and surroundingsource areas, suggests the clastic material from three dominant agesources: (1) southern Yangtze Craton, (2) Hainan Island and (3)Indochina Block. These sources provide sediment from the northwest,west and east. The sediments derived from the southern Yangtze Cratonare characterized by a wide detrital zircon U–Pb age pattern with theage peaks at ca. 32 Ma, 263 Ma, 442 Ma and three “broad” age group,700–1000 Ma, 1700–2100 Ma and 2200–2800 Ma. The analyzed zirconages derived from Hainan Island show a narrow age pattern with agepeaks at ca. 100 Ma and 242 Ma. The Indochina Block-derived zirconsshow narrow-range age pattern with considerable Mesozoic andPalaeozoic components with peaks at ca. 247 Ma and 469 Ma.

Based on the above discussion, a possible provenance model of theLate Miocene to Quaternary sediments has been made for the Y-SHBasin (Fig. 9) and the contribution of those source areas will bediscussed in next section.

5.3. Sediment contributions

The zircon U–Pb ages from the Upper Miocene to Quaternarysediments yield a wide range of ages which suggest multiple sourcesand complicated erosion processes that contributed the clastic materialto the Y-SH Basin. The peaks are consistent with the ages of Archaean–Cenozoic movements: Luliangian (2100–1700 Ma), Jinningian(1000–700 Ma), Caledonian (600–400 Ma), Indosinian (270–220 Ma),Yanshanian (180–80 Ma) and Himalayan (b65 Ma).

From theHuangliu to Ledong Formation (since 10.5Ma), zircon ageshave a very small age peak of Cenozoic grains, reaching 1.5% of the total(Table 2 and Fig. 12), which suggest that minor input of clastic materialfrom Red River Fault Zone in southern Yangtze Craton since the LateMiocene. The provenance signature of Hainan Island is Yanshanianzircon ages, reaching 6.1% of the total, reflecting an eastern sedimentsource. The Caledonian ages came from the Indochina and YangtzeCraton and reached 14.1% of the total. Luliangian and Jinningian aswell as theArchean basement zircon grains as the significant age groupsof the southern Yangtze Craton reached 41.5% and thus represent themain source from northwest. Therefore, we can conclude that theYangtze Cratonwas the main source for the Y-SH Basin, and the HainanIsland and Indochina Block also contributed detritus to it.

Table 2Proportions of detrital zircon age groups in the Yinggehai-Song Hong Basin.

Strata Geologic time scale

Cenozoic Cretaceous–Jurassic

Triassic–Permian

Carboniferous–Devonian

Ledong (1.9 Ma topresent)

5.7% 2.3% 23.9% 5.7%

Yinggehai (5.5–1.9 Ma) 0.8% 5.9% 14.2% 4.6%Huangliu (10.5–5.5 Ma) 0.9% 8.0% 17.8% 5.3%Total (10.5 Ma topresent)

1.5% 6.1% 16.6% 5.0%

We compared the Y-SH Basin sediment data with U–Pb ages fromthe Upper Miocene sedimentary rocks in the Yen Bai Basin (Figs. 9Aand 10), RRFZ,which could be regarded as the LateMiocene provenanceof paleo-Red River. Apart from Cenozoic and early Paleozoic ages, theyhave many of the same characteristics and age peaks. There weremany Cenozoic grains in Yen Bai Basin during the Late Miocene thatcould indicate that the basin derived more local provenance fromRRFZ. The Caledonian grains in the Y-SH Basin were most likely erodedfrom Silurian granites in Lao Cai by Lo River or Truong Son Belt by GianhRiver (Fig. 10), central Vietnam. The age spectra collected from the Y-SHBasin have similar age peaks with themodern Red River (Fig. 9A). All ofthose strongly suggest that much of the sediment in the Dongfang gasfield were derived from erosion upstream of the Red River.

In contrast, zircon grains frombothmodern rivers inwesternHainanandMiddle Miocene–Pliocene sediments in eastern margin of the Y-SHBasin (Fig. 9) show simple age populations. Yanshanian ages around ca.100Ma and ca. 160Ma are consistentwith the range of ages in the Y-SHBasin. Hainanmight contribute Yanshanian and Indosinian grains to thebasin by several drainages in western Hainan (e.g. Changhua River,Fig. 10). Because of the lack of zircon age data of rivers in coastalVietnam, comparison with this area is restricted.

Research by Yan et al. (2011a) shows that the Red River and itscatchment could account for 80% of the sediment deposited in theY-SH Basin, and the residual 20% could be by contributions from theeastern margin of Vietnam and Hainan Island. The major sources ofthe sediment in Red River came from the Yangtze Craton (Clift et al.,2006b; Hoang et al., 2009) whichmeans Yangtze Craton play an impor-tant role in providing material to Y-SH Basin. Yan et al. (2011a) arguedthat Hainan was an important and continuous source of the Y-SH Basin.However, our data suggests that Hainanwas not the outstanding sourcearea contributing to the basin. Despite this, it is difficult to calculate thecontribution of source areas precisely for the basin; we can reach theconclusion that the southern Yangtze Craton was the major sourcearea since 10 Ma.

5.4. Constraining on drainage capture in SW China

The paleo-Red River system is considered to have been disrupted by aseries of drainage capture events which may correspond to the regionalsurface uplift of eastern Asia (Clark et al., 2004; Clift et al., 2006a; Zhenget al., 2013). The paleo-Red River was originally proposed to have moredendritic drainage that drained into the South China Sea, which includedthe headwaters of the modern Mekong, Salween, Changjiang andTsangpo (Clark et al., 2004). These rivers were lost from paleo-RedRiver as a result of surface uplift in a certain period of geological history.Other studies argue that the Mekong, Salween and Tsangpo were neverconnected to the paleo-Red River (e.g. Clift et al., 2006a; Hoang et al.,2009). Up to now, the time of drainage capture away from the paleo-Red River system is still controversial. Clark et al. (2004) argued thatpaleo-drainage occurred by river capture in eastern Tibet prior to orcoeval with the Miocene using the method of digital elevation modelanalyses. Clift et al. (2006a) suggested that the large-scale drainagecapture away from the RedRiver possibly happened during theOligocene(before ca. 24 Ma) based on mass balance between depths of erosion

Silurian–Cambrian

Neoproterozoic Mesoproterozoic Paleoproterozoic Archean

13.6% 27.3% 5.7% 14.8% 1.1%

15.5% 25.2% 13.9% 15.3% 4.3%9.8% 38.4% 14.2% 13.8% 1.3%

13.4% 26.5% 13.0% 14.7% 2.9%

Fig. 11. Different strata age probability diagrams for detrital zircons from the Dongfang gas field: (A) Ledong Formation, including sample DF1312-1; (B) Yinggehai Formation, includingsamplesDF1112-1, DF1312-2, DF1312-3, DF1313-1 andDF1313-2; (C) Huangliu Formation, including samples DF11122, DF1312-9R, DF1312-10 andDF1313-4R; (D) Total of the samples.Left side: total data, right side: 0–500 Ma detrital zircons only.

214 C. Wang et al. / Marine Geology 355 (2014) 202–217

relative to a regional planation surface and deposited rock volumes in theSouth China Sea basins. Clift et al. (2008) used Pb isotopes in K-feldsparsgrains in the Red River delta to show the Red River was connected withmiddle Yangtze in the Eocene and lost by the middle Miocene. Hoang

Fig. 12. The detrital zircon age distribution of different strata based on geological timefrom the Archean to Cenozoic.

et al. (2009) used zircon U–Pb dating and Hafnium isotope to test themodels that link drainage reorganization to Tibetan surface uplift, the re-sults show that large-scale headwater capture might occur earlier thanthe Late Miocene (ca.12 Ma). Richardson et al. (2010) argued on thebasis of thermochronological data that capture of the middle Yangtze bythe lower Yangtze, removing the Red River, took place in the Eocene.Yan et al. (2011a) proposed that an expanded drainage must havepredated the Oligocene based on detrital zircon U–Pb dating and a bed-rock thermochronological study. Zheng et al. (2013) argued that thetiming of the capture took place before 23Ma based on the geochronolo-gy data.

The use of the sedimentary record to constrain the time of drainagecapture has been demonstrated in many areas. Sedimentary rockspreserved in the sedimentary basin of southeastern Asia are crucial tounderstanding the tectonic change in this region. The Red River andits catchment was the main input river that contributed detritus to theY-SH Basin, which makes the detrital zircon data from the Y-SH Basinhave some constraints on drainage capture of the paleo-Red River. Thechange of regional drainage associatedwith river capture inevitably im-pacts on the provenance of the Y-SH Basin. However, this study showsthat the age spectrums from the Upper Miocene to Quaternary havestrong similarities in age structure (Figs. 11 and 12) and reveal that

215C. Wang et al. / Marine Geology 355 (2014) 202–217

the provenance was not changed since 10 Ma. Clift and Sun (2006) usethemarine stratigraphic record to identify the sedimentary and tectonicevolution of the Yinggehai Basin. Their study shows that the flux of RedRiver sediment to the basin reached its lowest point at 10.3Ma, and sug-gests that major drainage loss had occurred before that time. Althoughthe precise timeof drainage loss cannot be given by this study, the resultcould provide some constrains to be placed on the timing. The largelystable provenance of the Y-SH Basin since the Late Miocene (ca.10Ma) suggests that if the Red River capture ever existed it should pre-date that time, a result consistent with the elevation reconstruction ofSpicer et al. (2003), Schoenbohm et al. (2006) and Wang et al. (2012).

6. Conclusions

U–Pb geochronologic analysis of detrital zircon grains providescritical constraints on the provenance of the UpperMiocene to Quaternarysediments in the Y-SH Basin. The zircon U–Pb ages revealed that the sedi-ments of Dongfang gas field in the Y-SH Basin record a stable provenancesince the Late Miocene and give eight age clusters with peaks at ca.32 Ma, ca. 99 Ma, ca. 160 Ma, ca. 247 Ma, ca. 422 Ma and three “broad”age groups, 600–1000Ma, 1700–2100 Ma and 2200–2800 Ma, suggestiveof a wide range of igneous rock ages in the source areas. The sediments ofthe Y-SH Basin principally derived from Proterozoic, Early Paleozoic andMesozoic igneous rocks, corresponding to the Jinningian, Caledonian andIndosinian tectonic events. The detritus from the northwest of the basinshows a wide zircon U–Pb age pattern from the Archean to Cenozoic,and the Hainan Island and Indochina Block–derived zircons show narrowrange age patternwithMesozoic and Palaeozoic components, respectively.Comparison of the results with the surrounding potential source areasindicates that the clastic material of the Upper Miocene to Quaternarywas eroded mainly from the southern Yangtze Craton, Hainan Island andIndochina Block. The Yangtze Craton was a major and continuous sourcearea contribution to the basin since the Late Miocene. We also found thatthe provenance of the basin has not changed since the Late Miocene,which means that if the Red River capture ever existed it should predatethat time. The study shows that detrital zircon U–Pb dating is a usefuland powerful tool to identify provenance and understanding of geologicalhistory in structurally complex areas. Age information has been dated inthe potential source areas making the geochronological data fromsediments particularly significant. Detrital zircon U–Pb ages should havebroad application in the provenance study of sedimentary rocks.

Supplementary data to this article can be found online at http://dx.doi.org/10.1016/j.margeo.2014.06.004.

Acknowledgments

We kindly thank Tu Xianglin, Nie Guanjun, Zhang Xiaoqiong and NiYongjin for their assistance in LA-ICP-MS U–Pb dating in GuangzhouInstitute of Geochemistry, Chinese Academy of Sciences. Thanks toChina National Offshore Oil Corporation, Zhanjiang Branch for supplyingthe drilling core samples. We would like to express our sincere apprecia-tion to the anonymous reviewers for their insightful comments, whichhave greatly aided us in improving the quality of the paper. This workwas financially supported by the National Science and TechnologyMajor Project of China (No. 2011ZX05023-004-11) and the NationNatural Science Foundation of China (Nos. 41072081 and 40872080).

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