Geology of the Fuding Inlier in Southeastern China: Implication for Late Paleozoic Cathaysian Paleogeography

Gondwana Research 22 (2012) 507–518

Contents lists available at SciVerse ScienceDirect

Gondwana Research

journal homepage: www.elsevier.com/locate/gr

Geology of the Fuding inlier in southeastern China: Implication for late Paleozoic Cathaysian paleogeography

Xiumian Hu a,⁎, Zhicheng Huang a, Jiangang Wang a, Jinhai Yu a, Keding Xu b, Luba Jansa c, Wenxuan Hu a a State Key Laboratory of Mineral Deposits Research, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093, PR China b Zhejiang Branch of Oil and Gas Exploration, SINOPEC, Hangzhou, 310013, China c Geological Survey of Canada-Atlantic, Dartmouth, N.S. Canada article info abstract

Article history: The age and composition of the basement rocks underlying the Mesozoic volcanic rocks in southeastern Received 28 February 2011 China have been long debated. New field investigation, stratigraphical and sedimentological studies of the Received in revised form 27 July 2011 Fuding inlier in eastern Cathaysian block have identified the presence of three stratigraphic units. The Accepted 5 September 2011 Upper Carboniferous carbonate unit, composed of silicified limestone, deposited on carbonate platform in a Available online 19 October 2011 continental shelf environment. The Lower Permian siliciclastic unit, consisting of slate and phyllite with minor arenites, deposited on shallow semi-restricted shelf. The third unit is a suite of Jurassic conglomerates Keywords: Late Paleozoic and sandstones deposited in alluvial fan environment. Provenance data indicate that the Fuding inlier was Cathaysia part of the Wuyishan terrane in the eastern Cathaysian block. The U–Pb age and Hf isotope of detrital zircons Fuding inlier indicate that extensive magmatic activity happened during 280–360 Ma in the source area. The εHf values of Paleogeography detrital zircons point to magmatic mixing of juvenile material and Precambrian crust. The similarities in rock compositions and detrital zircon ages among the Yeongnam massif in the Korean Peninsula, the Tananao complex in Taiwan and the Fuding inlier have led to the conclusion that these three regions most likely belonged to the Wuyishan terrane, eastern Cathaysia during the late Paleozoic. © 2011 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved.

1. Introduction clastic sedimentary rocks in the Fuding inlier are flysch type and were deposited in a deep-water environment. Consequently, this More than 90% of the surface area of the eastern Cathaysian block area was interpreted to present the late Paleozoic “Fu-Shan Trough” (Zhejiang and Fujian provinces, southeastern China) (Fig. 1) is cov- by Wang (1986) and this viewpoint was widely accepted. Although ered by late Mesozoic volcanic rocks (Gilder et al., 1996; Wang and the Upper Paleozoic sedimentary rocks are exposed in the Fuding in- Zhou, 2002; Zhou, 2007). The age and composition of the basement lier, their stratigraphy, sedimentology and sedimentary sources for rocks underlying these Mesozoic volcanic rocks are poorly known. A the strata remain uncertain. few Upper Paleozoic sedimentary rocks are exposed in the eastern We investigated the stratigraphy and sedimentology of the Fuding Cathaysian block, such as strata in the Fuding inlier in Fujian province inlier (Fig. 2) and carried out provenance analysis of the clastic rocks (Shi and Liu, 1980; Wu and Li, 1990; Ying et al., 1994) and in the based on detrital modes of the sandstones, Nd isotopes of the fine- Qingtian inlier in Zhejiang province (Zhu et al., 1994). Paleozoic strata grained clastic sediments and U–Pb age and Hf isotopes of the detrital in the Fuding inlier were first reported as a suite of low-grade meta- zircons. The new data allow us to examine and comment on the late morphic rocks by the Zhejiang Regional Geological Survey Team Paleozoic palaeogeography of the eastern Cathaysian block. (1975). The presence of the fusulinid Pseudostaffella sphaeroidea in the silicified limestone indicates the Late Carboniferous age (Zhejiang 2. Geological setting Regional Geological Survey Team, 1975), while conodonts from the microcrystalline limestones indicate the Early Carboniferous–Early The South China block (SCB) consists of the Yangtze block to the Permian (Ying et al., 1994). Shi and Liu (1980) suggested that the northwest and the Cathaysian block to the southeast (Fig. 1). The present boundary between these two blocks is the northeasterly trending Jiang-Shao fault in the east, but the southwestern extension of this boundary is unclear (e.g. Charvet et al., 1994; Fig. 1). The timing of the amalgamation between the Yangtze and Cathaysian blocks remains ⁎ Corresponding author at: School of Earth Sciences and Engineering, Nanjing controversial. The predominant view was an early Neoproterozoic age University, Hankou Road 22, Nanjing 210093, PR China. Tel.: +86 25 8359 3002; fax:+862583686016. for the amalgamation, ca. 900 to 880 Ma (Li et al., 2007, 2009)toca. E-mail address: [email protected] (X. Hu). 800 Ma (Zhao and Cawood, 1999; Wang et al., 2007, 2010a). The

1342-937X/$ – see front matter © 2011 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved. doi:10.1016/j.gr.2011.09.016 508 X. Hu et al. / Gondwana Research 22 (2012) 507–518

0 300 600 km CentralAsian Orogenic Belt

NM Yongyang IB NORTH Beijing GM OB CHINA Seoul T Tans-North YM China Orogen Su-Lu UHPBelt

Q inli Tan-Lu Fault ng-D abie Nanjing UHP Belt

Yangtze Block n roge nan O Fig. 2 Jiang Wuyishan SOUTH terrane Fuzhou Taipai CHINA Cathaysia Block Tainanao Nanling-Yunkai complex terrane Guangzhou

Fig. 1. Tectonic framework of the eastern China and Korea Peninsulas (simpliﬁed from Yu et al., 2009, 2010). Abbreviation: NM—Nangrim massif, GM—Gyeonggi massif, YM—Yeongnam massif, IB—Imjingang orogenic belt and OB—Okcheon orogenic belt. T—Taebaeksan basin.

Proterozoic crust of the Cathaysian block can be separated into two dis- al., 2010b); 3) The Indosinian orogeny, which extended from the tinct tectonic domains, the Wuyishan terrane to the northeast and the Late Permian to the Middle Triassic, was a result of the collision Nanling-Yunkai terrane to the southwest (e.g. Yu et al., 2010). The between the Indochina block and South China (Carter et al., 2001; Wuyishan terrane is characterized by dominant Paleoproterozoic Cai and Zhang, 2009); 4) Late Mesozoic magmatism along the south- (approximately 1.86 Ga) and lesser Neoarchean basement, which eastern coast of South China (Charvet et al., 1994; Wang et al., suffered strong Neoproterozoic and early Paleozoic tectono-thermal 1995; Gilder et al., 1996; Zhou and Li, 2000; Griffin et al., 2002), reworking. By contrast, the Nanling-Yunkai terrane contains abundant which represents an active continental margin. Neoarchean and Grenvillian-aged magmatism (approximately The Fuding inlier is located at approximately 20 km northwest of 1.0 Ga). Fuding town in Fujian province. The Fuding inlier is about 20 km2 in During the Phanerozoic time, the Cathaysian block experienced size, and is in fault contact with the surrounding Cretaceous volcani- four main tectonic events. 1) The Kwangsian orogeny (Ting, 1929), clastic rocks comprised mainly by volcaniclastic sandstones and tuffs which is traditionally called the Chinese Caledonian orogeny (Huang (Fig. 2). et al., 1980; Ren, 1991; Shu, 2006), is characterized by the angular unconformity that separates the Devonian-Permian cover from strongly deformed pre-Devonian strata (Huang et al., 1980) as well 3. Stratigraphy and sedimentology as syn-deformational metamorphism and subsequent anatexis (e.g. Li et al., 2010). It is generally considered to be an early Paleozoic intra- Due to extensive faulting, it was not possible to find a continuous continental orogen (Shu, 2006; Faure et al., 2009; Charvet et al., 2010; sedimentary succession in the study area (Fig. 4a). However, we could Li et al., 2010); 2) Late Paleozoic extensional rifting, which probably define three stratigraphic units in the field based on our geological started in the Devonian (Zeng et al., 1993; Zhao et al., 1996; Wang et mapping (Fig. 3). X. Hu et al. / Gondwana Research 22 (2012) 507–518 509

Dam 500 m

K1 Housuntan K1 74 K1 Luowu 238

27°21.5' C2 72 High way 73 Shizhukeng 251 70 J P1 Sijiaoping 69 7171 Qukeng Guanyingtang K 241 1 P1 240 239 252 Lingjiao 242 253 68 243 244 27°21' 254 67 245 K1 255 66 Fig.5a 246 257 P1 237 Chaishanshan 247 256 Nanxi reservoir C2 Nanxi P 1 Nanxi lake 249 K1 230 139.3±1.2 Ma

27°21.5' K1 231 236 248 232 250 J Silicified oolitic Kengli Legend limestone 235 Micritic Conglomerate limestone 233 P1 233 234 Sandstone GPS point K1 Slate and phyllite Main fault

120°06' 120°07'

Fig. 2. Simpliﬁed geological map of the Fuding inlier. GPS point information can be found in the Appendix A.

3.1. Upper Carboniferous carbonate unit 3.2. Lower Permian siliciclastic unit

The Upper Carboniferous carbonate unit in the study area is more The Lower Permian unit is comprised by black carbonaceous slate, than 35 m thick and is comprised of three different types of lime- silty slate and phyllite, occasionally interbedded with lithic arenites stones (Fig. 3): and microcrystalline limestones (Fig. 3). 1) The black slate, silty slate and phyllite (Fig. 4d) are partially silici- 1) Partially or completely silicified gray thin-bedded microcrystalline fied and enclose plant debris. The total organic carbon (TOC) in limestone (Fig. 4b), enclosing silicified sponge spicule (up to 10% the slates varies from 0.34 to 2.5% in weight (Zhejiang Petroleum in weight) and crinoidal debris (Fig. 5a). The limestone was Exploration Department, 1991). Shi and Liu (1980) suggested most likely deposited in a deep carbonate shelf environment. that these sediments in the Fuding inlier have flysch-type charac- 2) Partially or completely silicified grayish-yellow thin-bedded bioclastic teristics. However, we did not find any turbiditic structures during limestone. The bioclastic debris includes echinoderm, fusulinid, the field survey, such as the Bouma sequence, flute cast and nor- algae and brachiopod. The bioclasts indicate deposition in an open mal graded beds, etc. The black color of slates and the increased carbonate platform environment. organic carbon content indicate at least a dysoxic depositional 3) Gray thick-bedded silicified oolitic limestone (Fig. 4c), replaced by environment and increased surface productivity at that time. silica with some residual oolitic structure preserved (Fig. 5b). The The depositional environment of this unit was most probably ooids are approximately 0.3 to 0.8 mm in diameter and have a semi-restricted continental shelf. radial fabric. A minor amount of crinoid debris and few bioclastic 2) Thin-bedded sandstone layers occur sporadically within the slate- shells is also present. The sparry calcite cement filling the inter- dominated strata (Figs. 4eand5c). Sandstones are mainly fine- granular pores was replaced by silica. This rock may have been grained lithic arenites (Fig. 6). Clastic grains are angular to subangular deposited in a high energy, very shallow-water environment, in shape and are poorly sorted with a diameter of 0.06 to 0.2 mm probably as oolitic shoal on a carbonate platform. (Fig. 5c). The matrix is formed by illite. One bed of lithic arenite, located near a quartz vein (Fig. 4e), contained epidote and plagioclase Fossils reported from these limestones include fusulinids (Pseu- (up to 10% in weight), resulting from local thermal metamorphism dostaffella sphaeroidea, Beedeina sp. and Profusulinella), brachiopods (Fig. 5e). The siltstone is dominated by lithic grains (60%) and quartz (Neospirifer sp.) and conodonts (Idiognathodus delicates)(Wu and Li, (40%), which are poorly sorted and poorly rounded. The matrix 1990; Ying et al., 1994), which indicates the Bashkirian–Moscovian comprises up to 25% of the siltstones. We suggest that these sand- (Late Carboniferous) age of the strata. stones and siltstones were probably deposited in a prodelta setting. 510 X. Hu et al. / Gondwana Research 22 (2012) 507–518

Lithological description Fossils/Age Sedimentary facies Age Bed Lithology Zircon sample (m) v v v Volcaniclastic sandstones NX18 NX18: 139.3±1.2 Ma Volcanics K1 8 and tuff Lower Fault

Cretaceous

Conglomerate, sandy

0 NX23 J 1-2 7 conglomerate and coarse Alluvial fan

Jurassic sandstone

M1-17

C C

5 C 6 9

> C P 1 C C

C 5 5 C Conodonts: Streptognathodus fuchenensis,S. elongatus C Carbonaceous slate, silty slate (Ying et al., 1994) C C and phyllite, occasionally C interbedded with lithic arenites Continental shelf C and microcrystalline limestones -prodelta C C

Lower Permian M1-1 C

0 C 4 0 2 C C

C C C

C NX12 C C Fault

3 10~15 Fault Silicified oolitic limestone platform marginal shoal 2 5 Silicified bioclastic limestone Open carbonate platform C 2 Upper Gray, thin-bedded, microcrystalline 1 >15 limestone, partially or completely silicified Carbonate shelf

Carboniferous

Fig. 3. Composite stratigraphic column of the Fuding inlier. Legends as in Fig. 2.

3) Microcrystalline limestones, intercalated within the slate succes- 4. Sampling and methods sion, are thin-bedded and contain crinoid debris replaced with silica. We interpret them as being deposited on a deep carbonate shelf. Over 50 samples were collected in the Fuding inlier (Fig. 2,Appendix A). More than 30 polished thin sections were prepared from sandstones and fine-grained conglomerates for the petrographic analysis. Four 3.3. Jurassic coarse grained siliciclastic unit sandstone samples were selected for modal analysis with approximately 400 framework grains counted per thin section. To minimize the effect A suite of siliciclastic rocks over 100 m thick is exposed in the central of grain-size variations, the rock fragments were counted using the part of the Fuding inlier (Fig. 2). The lithology of the unit consists of Gazzi–Dickinson method (Dickinson and Suczek, 1979; Ingersoll et al., conglomerates, sandy conglomerates and coarse sandstones, which 1984). unconformably overlie the late Paleozoic sedimentary successions. Four slate samples from the Lower Permian were collected for the Conglomerates have sandy matrix (Fig. 4g) and are comprised by a Sm–Nd isotopic analysis. Approximately 100 mg of powder for each variety of gravels and pebbles, including slate, phyllites, gneiss, volcanic sample was dissolved in a mixture of HF and HNO3 in Teflon beakers. rocks, granites, sandstones and silicified limestones (Fig. 5f). The Sm and Nd were then separated and purified by conventional cation- pebbles are several to over 10 cm in diameter and are angular to exchange techniques. The isotopic measurements of the purified Sm well-rounded in shape. Clasts of dark-colored slate and phyllite litho- and Nd solutions were performed on a Finnigan Triton TI thermal clasts in the conglomerate are considered to have been derived from ionization mass spectrometer (TIMS) at the State Key Laboratory of the erosion of the underlying Lower Permian. The sandstones include Mineral Deposits Research, Nanjing University. The mass fractionation lithic arenites, subarkoses and arkosic arenites. Lithic grains within correction for the Nd isotopic ratios was based on 146Nd/144Nd= − the sandstones are dominated by volcanic grains, phyllites, minor 0.7219. The blanks for Sm and Nd were 5×10 11 g. A two-stage schists and slates. The feldspars are mainly K-feldspars with minor model age calculation is used because the Nd model age results are plagioclases. Large-scale cross-stratification and normal grading correlated with the Sm/Nd ratio (Miller and Harris, 1989). were observed in the strata. We interpret this lithologic suite as Two Lower Permian litharenite samples (08M1–1 and 08NX12) being deposited in alluvial fan environment. The age of this unit is and two Jurassic pebbly sandstone samples (08M1–17 and 08NX23) poorly constrained, but it is most likely of the Jurassic age based were selected for the detrital zircon U–Pb geochronology analysis. on regional geologic considerations (Fujian Bureau of Geology and The zircons were randomly selected from heavy mineral concentrates. Mineral Resources, 1997). The selected zircons were then encased in epoxy mounts and polished X. Hu et al. / Gondwana Research 22 (2012) 507–518 511

Fig. 4. Field photos at the Fuding inlier. (a) Panoramic photo of Early Permian strata along the main road in the southwestern part of the Fuding inlier. (b) Upper Carboniferous silicified microcrystalline limestone, GPS site 73. (c) Upper Carboniferous silicified oolitic limestones in tectonic contact with Lower Permian slates. GPS site 256. (d) Close-up view of the Lower Permian black slates, GPS Site 66. (e) Thin-bedded sandstone layers within the Lower Permian slate. The whitish band is a quartz vein near the sandstone. Sample 08M1–1 was taken from this sandstone. GPS site 257. (f) Lower Permian sandstones beds sampled (08NX12) at GPS site 244. (g) Jurassic conglomerate showing abundant black lithoclasts of slate and phyllite, GPS site 231. to expose their cores. The U–Pb dating of the detrital zircon was display discordance greater than 10%. For zircon ages that are concordant performed by laser ablation–inductively coupled plasma–mass spec- or slightly discordant (discordanceb10%), we use 206Pb/238Uagesfor trometry (LA–ICP–MS) at the State Key Laboratory for Mineral Deposits grains younger than 1 Ga and 207Pb/206Pb ages for grains older than 1 Ga. Research, Nanjing University, China, and at the State Key Laboratory of The Hf isotope analyses of detrital zircons were performed using a Lithosphere Evolution, Institute of Geology and Geophysics, Chinese Neptune multiple collector inductively coupled plasma mass spec- Academy of Sciences, following a previously described method (Jackson trometry (MC–ICP–MS) that was equipped with a 193 nm laser and et al., 2004). The results and isotopic rates were calculated using the housed at the State Key Laboratory of Lithosphere Evolution, Institute program GLITTER 4.4 (Van Achterbergh et al., 2001). Common Pb of Geology and Geophysics, Chinese Academy of Sciences. The details corrections were carried out using method described by Andersen about the instrumental conditions and data acquisition can be found in (2002). The age calculations and plotting of concordia diagrams Wu et al. (2006). In this study, the 176Hf/177Hf ratio of standard zircon were performed using ISOPLOT v.2.49 (Ludwig, 2001). Detrital zircon (91500) was 0.282265±11 (2 SD; n=18). To enable comparison age interpretations are complicated by Pb loss, which produces discor- among the laboratories, all of the Hf isotopic data were corrected by dance for the zircons in the approximately 1.8–2.5 Ga age range from adjusting the 176Hf/177Hf ratio of 91,500 to 0.282305. During the calcu- 176 177 the Fuding inlier. Fortunately, the patterns of discordance by Pb loss lation, we adopted a depleted mantle model with ( Hf/ Hf)DM= 176 177 are recognizable on U–Pb concordia diagrams as an array that projects 0.28325 and ( Lu/ Hf)DM=0.0384 (Griffinetal.,2000), chondrite 176 177 176 177 from a greater than 1.8 Ga upper intercept to a very young lower inter- with ( Hf/ Hf)CHUR=0.282772 and ( Lu/ Hf)CHUR =0.0332 cept (Fig. 8). In this study, we use 207Pb/206Pb ages for zircons that (BlichertToft and Albarede, 1997) and an average continental crust 512 X. Hu et al. / Gondwana Research 22 (2012) 507–518

Fig. 5. Photomicrographs of rocks in the Fuding inlier. (a) Microcrystalline limestone, showing siliciﬁed sponge spicule, Upper Carboniferous, sample 08M1–14. (b) Siliciﬁed oolitic limestone, Upper Carboniferous, sample 08M1–7. (c) Lithic arenites, showing abundant volcanic grains and angular to subangular quartz grains, Lower Permian, sample 08NX12. Lv—volcanic grain, Q—quartz. (d) Lithic arenites, showing abundant felsic volcanic grains, sample 08NX12. (e) Lithic arenites with epidote and plagioclase due to pyrometasomatism from a quartz vein, Lower Permian, sample 08M1–1. Ep—epidote, Pl—plagioclase. (f) Gravelly sandstone, showing phyllite grain, Jurassic, sample 08NX23.

176 177 with ( Lu/ Hf)C =0.015 (Grifﬁnetal.,2002). We used a decay diagram (Fig. 7), these samples plot within the evolution zone of the constant of 1.867×10−11 for 176Lu (Soederlund et al., 2004). Paleoproterozoic crust of South China (Shen et al., 2003, 2009). Further- All the analytical results are given in Appendices B to F. more, the Nd model ages of these slates are all older than 2.0 Ga, most probably derived from the basement rocks of the Cathaysian block 5. Provenance analysis rather than those of the southern Yangtze block (Shen et al., 2009).

5.1. Nd isotopes of slate 5.2. Detrital modes of sandstones As shown in Appendix C, the Lower Permian slate in the Fuding inlier have old Nd model ages, ranging from 2.05 to 2.23 Ga (averaging Lower Permian sandstones in the Fuding inlier are classiﬁed as 2.14 Ga), which is approximately 1.7 Ga older than its depositional lithic arenites with averaged Q–F–L ratios of 43:0:57 (Appendix B age. This result indicates that the Lower Permian slates were mainly and Fig. 6). Monocrystalline quartz grains dominate the grain frame- derived from the erosion of the ancient Paleoproterozoic crust. The work with the quartz content being 34 to 53%. Lithic grains (47–66%)

εNd(t) values of those Early Permian slate (calculation refers to Appendix are dominated by felsic volcanic grains (Fig. 5d), and subordinate are B) are −14.7 to −12.4 (averaging −13.5). On the εNd(t)–t(strata) lithoclast of shale and siltstones. No feldspar grains were observed. X. Hu et al. / Gondwana Research 22 (2012) 507–518 513 a Q Fuding (this study) Qm b

Jangseong Fm (S. Korea)

Craton Interior Quartzose Recycled Recycled Orogen Transitional Provenance ContinentMixed Transitional

Recycled

Dissected Arc

RecycledLithic Magmatic Arc Provenance Continental Block Provenance Transitional Arc

F L Undissected Arc Lt

Fig. 6. Q–F–L (a) and Qm–F–Lt (b) plots for the detrital modes of the Lower Permian sandstones from the Fuding inlier and the Taebaeksan basin (data from Lee and Sheen, 1998; Ko et al., 1999). The provenance ﬁelds are from Dickinson (1985).

5.3. Detrital zircon U–Pb ages sedimentsweresourcedfromthelatePaleozoicstrata.Theyoungest ages from the Jurassic sample are 281±4, 287±3, 301±5 and 307± Totally 72 zircons (sample 08NX12) and 138 zircons (sample 5 Ma. A lack of Late Permian–Jurassic zircons might indicate a magmatic 08M1–1) were analyzed for U–Pb ages from the Lower Permian lithic quiescence period in the source area. arenites. Some zircons show discordance due to Pb losses (Fig. 8). The We also analyzed zircons from the Cretaceous volcaniclastic rocks zircon ages from sample 08NX12 form three age populations clustered that surround the Paleozoic strata in the Fuding inlier. Sample 08NX18 at 285 to 482 Ma (27%), 1.45–1.91 Ga (35%) and 2.07 to 2.63 Ga (38%) gave a weighted average age of 139.3±1.2 Ma (n=14, MSWD=0.31) with peak ages at 311 Ma, 1.76, 1.78, 2.35 and 2.47 Ga. Sample 08M1– (Fig. 10), conﬁrming an Early Cretaceous age. 1 exhibits a similar age distribution with three age groups of 279 to 447 Ma (58%), 1.46 to 1.89 Ga (24%) and 2.18 to 2.59 Ga (17%) and 5.4. Detrital zircon Hf isotopes major peaks at 315 Ma, 1.77, 1.85, 2.4 and 2.49 Ga (Table 1 and Fig. 9). Carboniferous–Permian zircons (ca 360–280 Ma) from these Zircons (n=131) from two Lower Permian sandstones (08NX12 samples are abundant and comprise 22% to 52% of the total grains. and 08M1–1) were submitted to Hf isotopic analysis. On the εHf(t) The youngest zircon ages of 279±4, 283±4, 285±4 and 285± vs. U–Pb age diagram, the zircons are distributed into three distinct

3 Ma, provide the maximum age constraint for the deposition. groups (Fig. 11). Zircons of ca. 2.2 to 2.6 Ga age have εHf(t) values of C Samples 08M1–17 and 08NX23 are Jurassic pebbly sandstones. A −8.7 to +6.6 with two-stage Hf model ages (TDM) between 2.7 Ga total of 118 zircon ages were obtained for the provenance analysis. and 3.5 Ga, which indicate that the host magma of these zircons The zircon ages have two predominant populations at 281 to 404 Ma was derived from Meso- to Neoarchean crustal materials. Zircons of

(39%) and 1.31 to 2.05 Ga (52%) as well as a subordinate cluster at ca. 1.6 to 1.9 Ga have εHf(t) values of −15.5–+0.4 with Hf model 2.24 to 2.52 Ga (8%) (Table 1 and Fig. 9). The broad similarity in ages of 2.5 to 3.4 Ga similar to 2.2–2.6 Ga zircons. This suggests that the detrital zircon age spectrum between the Lower Permian and Jurassic clastic rocks suggests that they have the same source or that the Jurassic 08NX12 2400 5

U 2000 2400 CHUR 0 Pb/ 08NX23 1600 2000 2400 -5

1200 1600 2000 2400 -10 Evolutional region of aProterozoic 800 Nd(t) hin n South C 1200 1600 2000 ε crust i

-15 800 1200 1600 this study

-20 Shen et al.,2003 800 1200 Shen et al.,2009 08M1-1 08NX12, Permian sandstone, n=72; -25 800 0 100 200 300 400 500 600 08M1-1, Permian sandstone, n=138; t /Ma 08NX23, Jurassic conglomerate, n=60; 08M1-17, Jurassic conglomerate, n=57. 0 Fig. 7. εNd(t) vs. age (Ma) plot of the Lower Permian slate from the Fuding inlier, with 08M1-17 Pb/ U comparison to the εNd(t) values from other areas in eastern Cathayian block by Shen et al. (2003, 2009). Fig. 8. U–Pb concordia diagram of the detrital zircon from the Fuding inlier. 514 X. Hu et al. / Gondwana Research 22 (2012) 507–518

Table 1 Detrital zircon U–Pb age distribution in the Fuding inlier.

Age Sample Zircon Major age ranges (Ma) Major age peaks (Ma) Percentage of the numbers Paleozoic zircons

Jurassic 08M1–17 and 118 281–373 (n=45), 1732–1897 (n=54), 306 (n=3), 333 (n=25), 368 (n=6), 1760 (n=5), 39% (48 grains) 08NX23 2240–2521 (n=9). 1860 (n=46), 2335 (n=3), 2485 (n=3) Permian 08M1–1 138 279–366 (n=74), 1709–1894 (n=28), 292 (n=18), 315 (n=31), 337 (n=9), 351 (n=7), 58% (80 grains) 2274–2592 (n=21). 362 (n=4), 1738 (n=6), 1775 (n=7), 1855 (n=10), 2318 (n=4), 2399 (n=4), 2428 (n=4), 2488 (n=5), 2571 (n=3) Permian 08NX12 72 285–360 (n=16), 1611–1911 (n=24), 300 (n=5), 311 (n=6), 319 (n=5), 340 (n=3), 28% (20 grains) 2291–2494 (n=21). 1629 (n=5), 1685 (n=3), 1723 (n=4), 1757 (n=5), 1778 (n=5), 2295 (n=3), 2355 (n=6), 2394 (n=4), 2467 (n=4)

their host magma was derived from the same sources. Zircons of ca. Ying et al. (1994) found the conodonts Streplogmathodus fuchenensis,

280 to 400 Ma are characterized by negative εHf(t) values that vary S. elongates and Gondolella sp. from interbedded limestones within C from −34.3 to −3.1 and TDM between 1.5 Ga and 3.5 Ga. A wide the slates, which gave an age of the Middle Carboniferous to Early range of εHf(t) values indicates that the host melt of these zircons Permian for this unit. It is generally accepted that the youngest probably originated from the mixed sources of an old continental concordant detrital zircon age can be used to constrain the maximum crust, similar to the source of Neoarchean to Paleoproterozoic zircons, depositional age. In this study, the youngest detrital zircons (Appendix and juvenile magma or young crust (ca. 1.5 Ga) to different extent. D) from thin-bedded sandstones (samples 08NX12 and 08M1–1) in the Fuding inlier are approximately 280–285 Ma (Fig. 9), indicating that 6. Discussion their depositional ages could not be older than the Artinskian stage (Early Permian, according to the time scale of Gradstein et al., 2004). 6.1. Constrain on the depositional age of the siliciclastic unit Therefore, we suggested that the siliciclastic unit would be most probably Early Permian in age. The age of the siliciclastic unit in the Fuding inlier is poorly constrained because of the general lack of fossils. In the siliciclastic unit, 6.2. Fuding inlier was part of the northern Wuyishan terrane

Geologically, the Fuding inlier locates on the northeast of the 30 (a) 08M1-17&08NX23 (Jurassic, Fuding) Cathaysian block and belongs to the northern part of the Wuyishan n=117 terrane (Fig. 1). Moreover, the Nd isotopes and detrital zircon geo- 10 chronology from the Permian clastic sediments suggests that the Fuding inlier is tectonically part of the Wuyishan terrane (Fig. 9). The 60 – (b) 08M1-1&08NX12 Early Permian slates have Nd model age of 2.05 2.23 Ga, indicating (Permian, Fuding) existence of ancient Paleoproterozoic crust in the source area. In fact, n=211 the Paleoproterozoic basement rocks have been widely documented 20 in the Wuyishan terrane (e.g., the Badu Group, Li, 1997; Wan et al., 2007; Yu et al., 2009, 2011). In this study, the detrital zircon U–Pb (c) Eastern Yangtze ages from the Lower Permian sandstones shows two age peaks of (Paleozoic strata) 30 n=364 Paleoproterozoic–Neoarchean magmatism at 1.6–1.9 Ga and 2.2–2.6 Ga, (Wang et al., 2010) respectively. The late Paleoproterozoic (1.6–1.9 Ga) magmatism was 10 widely developed in the northern Wuyishan subterrane (Gan et al., 1995; Li, 1997; Wan et al., 2007; Xu et al., 2007; Yu et al., 2009), including (d) Nanling-Yunkai 90 (Paleozoic strata) n=1022 0.026 (Wang et al., 2010; Xiang et al., 2010; Yao et al., 2011) Sample 08NX18 160 30 Cretaceous volcanics

Relative age probability 139.3±1.2 Ma (2σ) (e) Taebaeksan basin 0.024 MSWD=0.31 9 (Permian, Korea) 150 n=47 (Li et al., 2009) 3 U

238 140 30 0.022

(f) Western Gyeonggi massif Pb/ (Paleozoic, Korea) n=114 206 (Cho et al., 2010) 10 130 144

)

0.020 a

0 500 1000 1500 2000 2500 3000 ( 140

Zircon U-Pb age (Ma) g 120 A 136 Fig. 9. U–Pb age distributions of detrital zircon from the Jurassic conglomerate (a), Lower Permian sandstones (b) in the Fuding inlier, SE China, with comparisons 0.018 with the detrital zircons from Paleozoic strata (c) from eastern Yangtze (Wang et al., 0.12 0.15 0.18 2010b) and Nanling-Yunkai terrane (d) (Wang et al., 2010b; Xiang and Shu, 2010; 207Pb/235U Yao et al., 2011), Carboniferous–Early Permian Manhang Formation (e) in the Taebaeksan basin (Li et al., 2009) and Paleozoic strata (f) from the western Gyeonggi massif, Korea Fig. 10. Zircon U–Pb concordia diagram of Cretaceous volcanic rock in the Fuding inlier (Cho et al., 2010). and the 206Pb/238U weighted age. X. Hu et al. / Gondwana Research 22 (2012) 507–518 515

and central Wuyishan and the Nanling–Yunkai terranes are not Depleted mantle recorded in the detrital zircons from the Fuding inlier (Fig. 9). Also, 10 the detrital zircons from Early Permian sandstones in Fuding inlier show different age patterns with those from eastern Yangtze terrane 0 Chondrite (Fig. 9), while the latter has abundant detrital zircons of ~1.1 Ga and~0.86–0.78 Ga (Wang et al., 2010b). Therefore, we suggested that (T)

Hf the detrital zircons in the Fuding inlier were most probably sourced

ε -10 from the northern part of the Wuyishan terrane.

Fuding inlier (this study) -20 Basement rocks of the Wuyi- 6.3. Source rocks and tectonic setting induced from clastic sediments shan terrane (Yu et al., 2010) Tananao complex and Eocene strata in Taiwan (Lan et al., 2009) Detrital modes of the Lower Permian sandstones in the Fuding 0 0.5 1.0 1.5 2.0 2.5 3.0 3.5 inlier are dominated by lithic grains (mainly felsic volcanic, shales Zircon ages (Ga) and siltstones) and monocrystalline quartz grains. On the QFL ternary diagram (Fig. 6; Dickinson, 1985), these sandstones are located in the ‘ ’ ﬁ Fig. 11. εHf vs. U–Pb age plot of detrital zircons from the Lower Permian sandstones in recycled orogen provenance eld. However, there is no geological the Fuding inlier. Data from basement rocks of the Wuyishan terrane and the Tananao evidence for a late Paleozoic orogenic event in the Cathaysian block. complex and Eocene strata in Taiwan are from Yu et al. (2010) and Lan et al. (2009), Alternatively, occurrence of volcanic grains and abundant Carboniferous respectively. to Early Permian detrital zircons points to a volcanic provenance. Felsic volcanic grains in the sandstones could have been derived from the the Paleoproterozoic granites and metamorphic rocks of the Badu and volcanic rocks, while lithoclasts of clay and siltstones and some of Tianjinping groups in southern Zhejiang and northern Fujian (Fig. 12). quartzes may be recycled from the basement or sedimentary covers. The early Paleoproterozoic–Neoarchean (2.2–2.6 Ga) zircons were Detrital zircons from the sandstones indicate that the volcanism in observed in the northern and central Wuyishan subterranes the source area was active with peaks at ca 330 Ma and ca 310 Ma. (Fig. 12) as inherit zircons and considered to represent possibly However, regional correlation shows that late Paleozoic magmatism Archean basement rocks (Yu et al., 2011). Detrital zircon Hf isotopes was rarely reported from the Cathaysian block (Wang and Liu, 1986; also support their sources from the northern Wuyishan terrane. On Charvet et al., 1994; Zhou et al., 2006), with only a small amount of the εHf(t) vs. U–Pb age diagram (Fig. 11), zircons from the basement granites from Hainan (267–262 Ma, Li et al., 2006) and rare basalts rocks in the northern Wuyishan terrane (Yu et al., 2010) overlap signif- from southwestern Fujian (Early Carboniferous, Huang, 1982). This result icantly with those Paleoproterozoic–Neoarchean detrital zircons in the leads us to question where the magmatism has occurred. The Early Fuding inlier, which may indicate that the clastics of these sedimentary Permian paleogeographic maps of South China (Chen et al., 1994; Liu rocks are mainly from the northern Wuyishan terrane itself. and Xu, 1994; Wang and Jin, 2000) show that the land was situated The widespread Neoproterozoic (0.72 to 0.82 Ga ) magmatic activity in the eastern and northern parts of the Cathaysian block during this in the central and southern parts of the Wuyishan terrane (Wanquan period, and the west Cathaysian block was covered by a widespread Group, Mamianshan Group, Mayuan Group, Taoxi Group) (Li et al., sea (Grabau, 1924; Chen et al., 1994; Liu and Xu, 1994; Wang and 2005; Yu et al., 2006; Wan et al., 2007; Yu et al., 2010)(Fig. 12). In the Jin, 2000). Therefore, we speculate that the Carboniferous–Early Permian Nanling–Yunkai terrane, the Grenvillian period (ca 1.0 Ga) and the magmatism as well as the source area of sandstones located either mid-Proterozoic magmatism are widely distributed (Wang et al., northern or eastern side of the depositional area.

2008; Yu et al., 2009, 2010; Wang et al., 2010b; Xiang and Shu, 2010; The εHf(t) values of the Carboniferous–Early Permian zircons varies Yao et al., 2011)(Fig. 9). Those magmatic ages both in the southern greatly from −34.3 to −3.1, indicating mixed sources of old Precam- brian basement and juvenile crust material (Fig. 11). Thus, the tectonic

(a) Permian sandstones setting in the source area should account for continuous magmatism (this study) and magmatic mixing. Two possibilities may be considered: rifting- n=211 related magmatism or subduction-related magmatism. Geologically, the South China block experienced extensional rifting during late Paleozoic (Zeng et al., 1993; Zhao et al., 1996). Those volcanic clastics can come from rifting-related volcanic rocks near the Fuding inlier. (b) Northern Wuyishan n=71 Meanwhile, the possibility of subduction-related magmatism cannot be ruled out. Mesozoic igneous activity in east Cathaysia was suggested to be related to the initiation and activation of subduction of the Pacific Ocean lithosphere (Gilder et al., 1996; Wang and Zhou, 2002). Unfortu- (c) Central Wuyishan nately, little is known about when Pacific Ocean lithosphere began to be n=135 subducted under the Asian continent. As a lack of geochemical and isotopic data from these volcanic grains in the sandstones, we cannot confirm the tectonic setting in the source area.

Relative age probability (d) Southern Wuyishan n=87 6.4. Relationships with the Yeongnam massif in the Korean Peninsula and the Tananao metamorphic complex in the Taiwan

The Korean Peninsula can be subdivided into ﬁve tectonic units or 0 500 1000 1500 2000 2500 3000 terranes (Fig. 1). From the south to the north, these are: Yeongnam Zircon U-Pb age (Ma) massif, Okcheon (Ogcheon) Belt, Gyeonggi (Kyonggi) massif, Imjingang Belt and Nangrim massif/Pyeongnam basin (Chough et al., 2000). The Fig. 12. Zircon U–Pb age probability diagrams for different areas in the Wuyishan Qinling–Dabei–Sulu Belt, which represents the suture between South terrane of the Cathaysian Block. Age data sources: (a) Fuding inlier (this study); (b)northernWuyishan(Yu et al., 2009); (c) central Wuyishan (Wan et al., China and North China (Yin and Nie, 1993), extends into Korea either 2007); (d) southern Wuyishan (Yu et al., 2010). along the Imjingang Belt (Ree et al., 1996) or the Hongseong–Odesan 516 X. Hu et al. / Gondwana Research 22 (2012) 507–518

Early Permian North China 30°N (~280Ma) Japan

Baltica North Korea Yeongnam

Late Paleozoic A Fuding volcanism E

C 0°

Tananao O South

C China I

PALEOTETHYAN F

OCEAN C

Indochina P PANGEA 30°S Sibumasu Indonesia Iran Lhasa Africa Malaysia Arabia Qiangtang

Greater Australia India 60°S

Fig. 13. An Early Permian (~280 Ma) paleogeographical map (modified after Golonka and Fork, 2000; Zhu et al., 2010), illustrating that the Fuding inlier was most possibly derived from a volcanic source developed on the eastern margin of the South China block. We suggest that the Fuding inlier, the Yeongnam massif and the Tananao complex belonged to the Wuyishan terrane, eastern Cathaysia during the Early Permian. belt within the Gyeonggi massif (Oh et al., 2005; Kim et al., 2011a, b). (Fig. 6b). Together, our data further support that Yeongnam massif was The southernmost terrane, the Yeongnam massif, is mostly correlated part of the Wuyishan terrane of the Cathaysian block and suggests that with the Cathaysian block (Metcalfe, 2006). Recently, Yu et al. (2009, the Early Permian Taebaeksan basin of the Yeongnam massif and the 2011) found that the Yeongnam massif shares similar geological Fuding inlier might be connected and share the same sources (Fig. 13). features with the Wuyishan terrane, such as: 1) Paleoproterozoic The pre-Cenozoic Tananao metamorphic complex in the Central magmatism at 1.91 to 1.83 Ga, which appears in the Wuyishan terrane Range of Taiwan consists of voluminous schist and marble as well as as well as in the Yeongnam massif (Chough et al., 2000; Lee et al., 2000; of scattered bodies of granitic rocks and amphibolite. A few fusulinids Sagong et al., 2003); 2) basement rocks in both areas have similar Nd and corals, possibly of the Late Permian age (Yen, 1953), and Jurassic model ages of 2.75 to 2.84 Ga (Lee et al., 2000; Sagong et al., 2003); to Early Cretaceous dinoflagellates (Chen, 1989) were discovered and 3) Triassic medium- to high-grade metamorphism and granitic from the Tananao Complex. U–Pb zircon dating of meta-granites magmatism are widely distributed in both terranes (Wang et al., and gneisses show two stages of magmatism at 190 to 200 Ma and 1995). All of these observations suggest that the crustal evolution of 85 to 90 Ma (Jahn et al., 1986; Yui et al., 2009). The Tananao complex the Yeongnam massif is comparable with the Wuyishan terrane of the was considered to represent an exposed portion of the Asian continental Cathaysian block from the Paleoproterozoic up to the Triassic. crust (Ho, 1986), with rocks originating from the Permian to Cretaceous Interestingly, the Early Permian clastic rocks in the Fuding inlier periods, and exhumed during late Cenozoic arc-continent collision show similar geological features to the Early Permian strata in the (Beyssac et al., 2007). Recently, Lan et al. (2009) reported detrital Taebaeksan basin, located between the Gyeonggi and Yeongnam zircons older than 2.3 Ga from the Tananao complex and Eocene massifs in South Korea. Detrital zircon ages from the Manhang Formation rocks of the Central Range of Taiwan and documented a major (Carboniferous–EarlyPermian)showtwomainageclustersat288– age group of 2.3 to 2.6Ga (Fig. 11). Both the age population and Hf 358 Ma and 1.78–1.89 Ga, respectively, with major peaks at 305 Ma and isotopic compositions of those detrital zircons are very similar to 1.87 Ga (Li et al., 2009). The detrital zircon age distribution is very similar the Paleoproterozoic to late Neoarchean zircons from the Wuyishan to that we have found in the Fuding inlier (Fig. 9), but different to the terrane (Figs. 9 and 11). Considering that Permian fusulinids and detrital zircons from the western Gyeonggi massif where have four major corals and similar 2.3–2.6 Ga detrital zircons were found in the Tananao age components of ~2.5–2.4 Ga, 1.0–0.9 Ga, ~820–750 Ma, ~430 Ma (Cho complex, we speculate that at least the Late Paleozoic part of the et al., 2010)(Fig. 9). In addition, the detrital modes of the Lower Permian Tananao complex may have being the eastern part of the Cathaysian Jangseong Formation in the Taebaeksan basin (Lee and Sheen, 1998; Ko et block during the Permian period (Fig. 13). al., 1999) are also similar to those in the Fuding inlier (Fig. 6a). Sand- stones from both places comprises poorly sorted, angular to sub- 7. Conclusion rounded quartz and lithic fragments, without feldspar grains. The much greater proportion of lithic grains in the Early Permian sandstones Field investigation, petrological, sedimentological and geochrono- in Fuding may be ascribed to different criteria in grain-counting. We logical studies identified three lithostratigraphic units in the Fuding count the microcrystalline felsic detritus as lithic grains whereas other inlier, which is located in the northern Fujian province of China. The researchers (e.g., Lee and Sheen, 1998) count as polycrystalline quartzes Upper Carboniferous carbonate rocks are composed of silicified X. Hu et al. / Gondwana Research 22 (2012) 507–518 517 microcrystalline limestone, bioclastic limestone and oolitic limestone, Chen, C.H., 1989. A preliminary study of the fossil dinoflagellates from the Tananao Schist, Taiwan. M.S. thesis, National Taiwan University, 89 pp. in Chinese. which were deposited on shallow carbonate shelf and in carbonate Chen, H.M., Wu, X.H., Zhang, Y., Liu, B., 1994. Carboniferous lithofacies paleogeography shoal environments. The Lower Permian siliciclastic unit is comprised and mineralization in south China. Geological Publishing House, Beijing. (124pp. in of black organic-carbon-enriched slate, silty slate and phyllite, which Chinese). Cho, M., Na, J., Yi, K., 2010. SHRIMP U–Pb ages of detrital zircons in metasandstones of are occasionally interbedded with lithic arenites and microcrystalline the Taean Formation, western Gyeonggi massif, Korea: tectonic implications. Geos- limestones. This sequence was deposited on moderately deep, ciences Journal 14, 99–109. semi-restricted shelf and in prodelta environments, with high surface Chough, S.K., Kwon, S.T., Ree, J.H., Choi, D.K., 2000. Tectonic and sedimentary evolution – bioproductivity. Jurassic coarse clastic rocks, represented by a suite of of the Korean peninsula: a review and new view. Earth-Science Reviews 52 (1 3), 175–235. conglomerates and coarse-grained sandstones, were deposited in fluvial Dickinson, W.R., 1985. Interpreting provenance relations from detrital modes of sand- or alluvial fan environments. stones. NATO ASI Series, Series C Mathematical and Physical Sciences 148, – The Nd isotopes and detrital zircon U–Pb–Hf isotopes indicate that 333 361. Dickinson, W.R., Suczek, C.A., 1979. Plate tectonics and sandstone compositions. AAPG the late Paleozoic Fuding inlier was part of the Wuyishan terrane of Bulletin 63, 2164–2182. the Cathaysia continental block. A group of detrital zircons from sand- Faure, M., Shu, L.S., Wang, B., Charvet, J., Choulet, F., Monie, P., 2009. Intracontinental stones shows that the main age peak extends from approximately subduction: a possible mechanism for the early Palaeozoic orogen of SE China. Terra Nova 21 (5), 360–368. 280 to 360 Ma, indicating prolonged magmatic activity in the source Fujian Bureau of Geology and Mineral Resources, 1997. Lithostratigraphy of Fujian area through the Carboniferous to Early Permian. The εHf(t) values province. Geological Publishing House, Beijing. (216pp. in Chinese). of these zircons vary from −34.3 to −3.1, suggesting mixing of the Gan, X., Li, H., Sun, D., Jin, W., Zhao, F., 1995. A geochronological study on early Prote- rozoic granitic rocks, southeastern Zhejiang. Acta Petrologica and Mineralogica 14 magma sourced from juvenile material and melted Precambrian base- (1), 1–8 (in Chinese). ment rocks. Gilder, S.A., Gill, J.B., Coe, R.S., Zhao, X.X., Liu, Z.W., Wang, G.X., Yuan, K.R., Liu, W.L., The similarities in the rock compositions and the detrital zircon Kuang, G.D., Wu, H.R., 1996. Isotopic and paleomagnetic constraints on the Meso- zoic tectonic evolution of south China. Journal of Geophysical Research 101 (B7), ages among the Yeongnam massif in the Korean Peninsula, the Tananao 16137–16154. complex in Taiwan and the Fuding inlier have led us to conclude that all Grabau, A.W., 1924. Stratigraphy of China, Part 1, Paleozoic and Older. Peking, pub- three regions were likely part of the Wuyishan terrane, Cathaysian lished by Geological Survey, Ministry of Agriculture and Commerce, China block during the late Paleozoic. (528pp.). Golonka, J., Ford, D., 2000. Pangean (Late Carboniferous-Middle Jurassic) paleoenviron- ment and lithofacies. Palaeogeography, Palaeoclimatology, Palaeoecology 161, Acknowledgements 1–34. Gradstein, F.M., Ogg, J.G., Smith, A.G., Bleeker, W., Lourens, L.J., 2004. A new geologic time scale, with special reference to Precambrian and Neogene. Episodes 27 (2), This study benefited greatly from discussions with Professor Dezi 83–100. Wang. We appreciate Professor Fuyuan Wu for his help with the zircon Griffin, W.L., Pearson, N.J., Belousova, E., Jackson, S.E., van Achterbergh, E., O'Reilly, S.Y., Shee, S.R., 2000. The Hf isotope composition of cratonic mantle: LAM-MC-ICPMS Hf isotope analysis. We thank Dr. Thomas Frank for his English revision. analysis of zircon megacrysts in kimberlites. Geochimica et Cosmochimica Acta Constructive comments from Prof. J. Charvet and two anonymous 64 (1), 133–147. reviewers are greatly appreciated. This study was financially supported Griffin, W.L., Wang, X., Jackson, S.E., O'Reilly, S.Y., Xu, X.S., Zhou, X.M., 2002. Zircon by the State Key Laboratory for Mineral Deposits Research (no. 2008-I- chemistry and magma mixing, SE China: in-situ analysis of Hf isotopes, Tonglu and Pingtan igneous complexes. Lithos 61 (3–4), 237–269. 01), Nanjing University and the SINOPEC Cathaysian project. Ho, C.S., 1986. A synthesis of the geologic evolution of Taiwan. Tectonophysics 125, 1–16. Huang, G.Z., 1982. Early–Middle Carboniferous volcanic rocks in southwest Fujian. Monograph of Institute of Geology, Chinese Academy of Sciences 3 (2), 86–100 Appendix A. Supplementary data (No. 12, in Chinese). Huang, J., Ren, J., Jiang, C., Zhang, Z., Qin, D., 1980. The Geotectonic evolution of China. Appendix A GPS points in the Fuding inlier. Science Publishing House, Beijing. (124 pp. in Chinese). Ingersoll, R.V., Fullard, T.F., Ford, R.L., Grimm, J.P., Pickle, J.D., Sares, S.W., 1984. The ef- Appendix B The detrital modes of the Lower Permian sandstones fect of grain size on detrital modes; a test of the Gazzi–Dickinson point-counting from the Fuding inlier. method. Journal of Sedimentary Research 54, 103–116. Appendix C Sm-Nd isotopic compositions of the Lower Permian Jackson, S.E., Pearson, N.J., Griffin, W.L., Belousova, E.A., 2004. The application of laser ablation–inductively coupled plasma–mass spectrometry to in situ U–Pb zircon slates from the Fuding inlier. geochronology. Chemical Geology 211 (1–2), 47–69. Appendix D Detrital zircon U-Pb isotope data measured by LA- Jahn, B.M., Martineau, F., Peucat, J.J., Cornichet, J., 1986. Geochronology of the Tananao ICPMS from the Fuding inlier. schist complex, Taiwan, and its regional tectonic significance. Tectonophysics 125 – – Appendix E Detrital zircon Hf-isotope data measured by MC-LA- (1 3), 103 124. Kim, S.W., Santosh, M., Park, N., Kwon, S., 2011a. Forearc serpentinite mélange from the ICPMS from the Fuding inlier. Hongseong suture, South Korea. Gondwana Research 20, 852–864. Supplementary data to this article can be found online at doi:10. Kim, S.W., Kwon, S., Koh, H.J., Yi, K., Jeong, Y.-J., Santosh, M., 2011b. Geotectonic frame- 1016/j.gr.2011.09.016. work of Permo-Triassic magmatism within the Koran Peninsula. Gondwana Re- search 20, 865–889. Ko, J., Yu, K.M., Rhee, B.K., Lee, J.Y., Shin, J.B., 1999. Sandstone petrology of the Pyeongan References Supergroup, Taebaeksan region, Korea; implications for the Carboniferous–Triassic tectonic history of East Asia. Journal of Sedimentary Research 69 (3), 711–719. Andersen, T., 2002. Correction of common lead in U–Pb analyses that do not report Lan, C.Y., Usuki, T., Wang, K.L., Yui, T.F., Okamoto, K., Lee, Y.H., Hirata, T., Kon, Y., Oriha- 204Pb. Chemical Geology 192, 59–79. shi, Y., Liou, J.G., 2009. Detrital zircon evidence for the antiquity of Taiwan. Geos- Beyssac, O., Simoes, M., Avouac, J.P., Farley, K.A., Chen, Y.-G., Chan, Y.-C., Goffe, B., 2007. ciences Journal 13 (3), 233–243. Late Cenozoic metamorphic evolution and exhumation of Taiwan. Tectonics 26, Lee, Y.I.I., Sheen, D.H., 1998. Detrital modes of the Pyeongan Supergroup (Late Carbon- TC6001. doi:10.1029/2006TC002064. iferous–Early Triassic) sandstones in the Samcheog coalfield, Korea: implications BlichertToft, J., Albarede, F., 1997. The Lu–Hf isotope geochemistry of chondrites and for provenance and tectonic setting. Sedimentary Geology 119, 219–238. the evolution of the mantle–crust system. Earth and Planetary Science Letters Lee, S.R., Cho, M., Yi, K., Stern, R.A., 2000. Early Proterozoic granulites in central Korea: 148 (1–2), 243–258. tectonic correlation with Chinese cratons. Journal of Geology 108 (6), 729–738. Cai, J.X., Zhang, K.J., 2009. A new model for the Indochina and South China collision Li, X.H., 1997. Timing of the Cathaysia Block formation: constraints from SHRIMP U–Pb during the Late Permian to the Middle Triassic. Tectonophysics 467 (1–4), 35–43. zircon geochronology. Episodes 20, 188–192. Carter, A., Roques, D., Bristow, C., Kinny, P., 2001. Understanding Mesozoic accretion in Li, W.X., Li, X.H., Li, Z.X., 2005. Neoproterozoic bimodal magmatism in the Cathaysia block Southeast Asia: significance of Triassic thermotectonism (Indosinian orogeny) in of South China and its tectonic significance. Precambrian Research 136, 51–66. Vietnam. Geology 29 (3), 211–2014. Li, X.H., Li, Z.X., Li, W.X., Wang, Y.J., 2006. Initiation of the Indosinian Orogeny in South Charvet, J., Lapierre, H., Yu, Y.W., 1994. Geodynamics significance of the Mesozoic vol- China: evidence for a Permian magmatic arc on Hainan Island. Journal of Geology canism of southeastern China. Journal of Southeast Asian Earth Sciences 9 (4), 114 (3), 341–353. 387–396. Li, Z.X., Wartho, J.A., Occhipinti, S., Zhang, C.L., Li, X.H., Wang, J., Bao, C.M., 2007. Early Charvet, J., Shu, L., Faure, M., Choulet, F., Wang, B., Lu, F., Le Breton, N., 2010. Structural history of the eastern Sibao Orogen (South China) during the assembly of Rodinia: development of the Lower Paleozoic belt of South China: genesis of an intraconti- new mica 40Ar/39Ar dating and SHRIMP U–Pb detrital zircon provenance con- nental orogen. Journal of Asian Earth Sciences 39, 309–330. straints. Precambrian Research 159 (1–2), 79–94. 518 X. Hu et al. / Gondwana Research 22 (2012) 507–518

Li, Z., Peng, S.T., Xu, C.W., Han, Y.X., Zhai, M.G., 2009. U–Pb ages of the Paleozoic sand- Wang, Y., Zhang, F., Fan, W., Zhang, G., Chen, S., Cawood, P.A., Zhang, A., 2010b. Tectonic stone detrital zircons and their tectonic implications in the Tabeaksan basin, Korea. setting of the South China Block in the early Paleozoic: resolving intracontinental Acta Petrologica Sinica 25 (1), 182–192 (in Chinese). and ocean closure models from detrital zircon U–Pb geochronology. Tectonics 29, Li, Z.X., Li, X.H., Wartho, J.A., Clark, C., Li, W.X., Zhang, C.L., Bao, C.M., 2010. Magmatic TC6020. doi:10.1029/2010TC002750. and metamorphic events during the early Paleozoic Wuyi–Yunkai orogeny, south- Wu, Q., Li, X.M., 1990. Carboniferous stratigraphy and tectonic environment in Fuding, eastern South China: new age constraints and pressure–temperature conditions. Fujian. Regional Geology of China 4, 327–333 (in Chinese). Geological Society of America Bulletin 122 (5–6), 772–793. Wu, F.Y., Yang, Y.H., Xie, L.W., Yang, J.H., Xu, P., 2006. Hf isotopic compositions of the Liu, B., Xu, X. (Eds.), 1994. Atlas of Lithofacies and Paleogeography of South China. Sci- standard zircons and baddeleyites used in U–Pb geochronology. Chemical Geology ence Publishing House, Beijing (188pp. in Chinese). 234 (1–2), 105–126. Ludwig, K.R., 2001. User's manual for Isoplot/Ex rev. 2.49, a geochronological toolkit for Xiang, L., Shu, L.S., 2010. Pre-Devonian tectonic evolution of the eastern South China Microsoft Excel. Berkeley Geochronology Center Special Publications 1, 1–55. Block: geochronological evidence from detrital zircons. Science in China, Series – Metcalfe, I., 2006. Palaeozoic and Mesozoic tectonic evolution and palaeogeography of D: Earth Sciences 53, 1427 1444. fi East Asian crustal fragments: the Korean Peninsula in context. Gondwana Research Xu, X.S., O'Reilly, S.Y., Grif n, W.L., Wang, X.L., Pearson, N.J., He, Z.Y., 2007. The crust of 9(1–2), 24–46. Cathaysia: age, assembly and reworking of two terranes. Precambrian Research – Miller, J.F., Harris, N.B.W., 1989. Evolution of continental crust in the Central Andes; 158, 51 78. – constraints from Nd isotope systematics. Geology 17, 615–617. Yao, J.L., Shu, L.S., Santosh, M., 2011. Detrital zircon U Pb geochronology, Hf-isotopes — Oh, C.W., Kim, S.W., Choi, S.G., Zhai, M.G., Guo, J.H., Krishnan, S., 2005. First finding of and geochemistry new clues for the Precambrian crustal evolution of Cathaysia – eclogite facies metamorphic event in South Korea and its correlation with the Block, South China. Gondwana Research 20, 553 567. Dabie–Sulu collision belt in China. Journal of Geology 113 (2), 226–232. Yen, T.P., 1953. On the occurrence of the late Paleozoic fossils in the metamorphic com- – Ree, J.H., Cho, M., Kwon, S.T., Nakamura, E., 1996. Possible eastward extension of Chi- plex of Taiwan. Bulletin of Geological Survey in Taiwan 4, 23 26 (in Chinese). nese collision belt in South Korea: the Imjingang belt. Geology 24 (12), 1071–1074. Yin, A., Nie, S.Y., 1993. An indentation model for the north and south China collision Ren, J., 1991. On the geotectonics of southern China. Acta Geologica Sinica 4 (2), and the development of the Tan-Lu and Honam fault systems, eastern Asia. Tecton- – 111–130 (in Chinese). ics 12 (4), 801 813. Sagong, H., Cheong, C.S., Kwon, S.T., 2003. Paleoproterozoic orogeny in South Korea: Ying, Z.E., Ding, B.L., Bi, Z.Q., 1994. Discovery of Mid-Late Carboniferous conodonts in “ ” evidence from Sm–Nd and Pb step-leaching garnet ages of Precambrian basement the Nanxi Tectonic window in Fuding County, Fujian. Volcanology and Mineral – rocks. Precambrian Research 122 (1), 275–295. Resources 15 (3), 43 48 (in Chinese). Shen, W.Z., Yu, J.H., Zhao, L., Chen, Z.L., Lin, H.C., 2003. Nd isotopic characteristics of Yu, J.H., Wei, Z.Y., Wang, L.J., Shu, L.S., Sun, T., 2006. Cathaysia block: a young continent post-Archean sediments from the Eastern Nanling Range: evidence for crustal evo- composed of ancient materials. Geological Journal of China Universities 12, – lution. Chinese Science Bulletin 48 (16), 1679–1685. 440 447 (in Chinese). fi Shen, W.Z., Ling, H.F., Shu, L.S., Zhang, F.R., Xiang, L., 2009. Sm–Nd isotopic composi- Yu, J.H., Wang, L.J., O'Reilly, S.Y., Grif n, W.L., Zhang, M., Li, C.Z., Shu, L.S., 2009. A Paleo- tions of Cambrian–Ordovician strata at the Jinggangshan area in Jiangxi Province: proterozoic orogeny recorded in a long-lived cratonic remnant (Wuyishan ter- – – tectonic implications. Chinese Science Bulletin 54 (10), 1750–1758. rane), eastern Cathaysia Block, China. Precambrian Research 174 (3 4), 347 363. fi Shi, Y.S., Liu, S.H., 1980. Discovery of flysch construction at Nanxi, Fuding: implications Yu, J.H., O'Reilly, S.Y., Wang, L.J., Grif n, W.L., Zhou, M.F., Zhang, M., Shu, L.S., 2010. to the Paleozoic basement and tectonics. Journal of Nanjing University (Natural Components and episodic growth of Precambrian crust in the Cathaysia Block, – Science) 4, 121–127 (in Chinese). South China: evidence from U Pb ages and Hf isotopes of zircons in Neoprotero- – Shu, L.S., 2006. Pre-Devonian tectonic evolution of South China: from Cathaysian block zoic sediments. Precambrian Research 181, 97 114. fi to Caledonian period folded orogenic belt. Geological Journal of China Universities Yu, J.H., O'Reilly, S.Y., Zhou, M.F., Grif n, W.L., Wang, L.J., 2011. U-Pb geochronology and 12 (4), 418–431 (in Chinese). Hf-Nd isotopic geochemistry of the Badu Complex. Southeastern China: implica- Soederlund, U., Patchett, P.J., Vervoort, J.D., Isachsen, C.E., 2004. The 176Lu decay con- tions for the Precambrian crustal evolution and paleogeography of the Cathaysia stant determined by Lu–Hf and U–Pb isotope systematics of Precambrian mafic in- Block. Precambrian Research. doi:10.1016/j.precamres.2011.07.014. – trusions. Earth and Planetary Science Letters 219 (3–4), 311–324. Yui, T.F., Okamoto, K., Usuki, T., Lan, C.Y., Chu, H.T., Liou, J.G., 2009. Late Triassic Late Ting, W.K., 1929. The orogenic movement in China. Bulletin of the Geological Society of Cretaceous accretion/subduction in the Taiwan region along the eastern margin — China 8 (1), 151–170. of South China evidence from zircon SHRIMP dating. International Geology Re- – Van Achterbergh, E., Ryan, C.G., Jackson, S.E., Griffin, W.L., 2001. Data reduction soft- view 51 (4), 304 328. ware for LA–ICP–MS. Appendix: Laser Ablation–ICP–Mass Spectrometry in the Zeng, Y.F., Zhang, J.Q., Liu, W.J., Zhou, H.L., Chen, H.D., 1993. Devonian lithofacies paleo- Earth Sciences: Principles and Applications. : Mineralog. Assoc., 29. Canada Short geography and mineralization in South China. Geological Publishing House, Bei- Course Series, Ottawa, Ontario, Canada, pp. 239–243. jing. (123pp. in Chinese). Wan, Y.S., Liu, D.Y., Xu, M.H., Zhang, J., Song, B., Shi, Y., Du, L., 2007. SHRIMP U–Pb zir- Zhao, G.C., Cawood, P.A., 1999. Tectonothermal evolution of the Mayuan assemblage in con geochronology and geochemistry of metavolcanic and metasedimentary rocks the Cathaysia Block: implications for Neoproterozoic collision-related assembly of – in Northwestern Fujian, Cathaysia Block, China: tectonic implications and the need the South China craton. American Journal of Science 299 (4), 309 339. to redefine lithostratigraphic units. Gondwana Research 12, 166–183. Zhao, X., Allen, M.B., Whitham, A.G., Price, S.P., 1996. Rift-related Devonian sedimenta- Wang, H.Z. (Ed.), 1986. Paleogeographic maps of China. Geological Publishing House, tion and basin development in South China. Journal of Southeast Asian Earth Sci- – – Beijing (110pp. in Chinese). ences 14 (1 2), 37 52. Wang, Y., Jin, Y., 2000. Permian palaeogeographic evolution of the Jiangnan basin, Zhejiang Petroleum Exploration Department, 1991. Geological reports of the sedimen- South China. Palaeogeography, Palaeoclimatology, Palaeoecology 160 (1–2), tary rocks underlying the Mesozoic volcanic successions, southeast Zhejiang. Zhe- 35–44. jiang Petroleum Exploration Department research report (in Chinese). Wang, D.Z., Liu, C.S., 1986. Distribution and genesis of the Hercynian–Indosinian gran- Zhejiang Regional Geological Survey Team, 1975. Pingyang sheet of the 1: 200 000 geo- itoids along the southeast coast of China. Acta Petrologica Sinica 2 (4), 1–13 (in logical map and reports. (in Chinese). Chinese). Zhou, X.M. (Ed.), 2007. Genesis of the late Mesozoic granites at Nanling: implications to Wang, D.Z., Zhou, X.M., 2002. Genesis of the Late Mesozoic Igneous Rocks of Granitic lithosphere dynamic evolution. Science Publishing House, Beijing (691pp. in Composition in Southeast China and Their Implications to Crustal Evolution. Sci- Chinese). ence Publishing House, Beijing. (295pp. in Chinese). Zhou, X.M., Li, W.X., 2000. Origin of Late Mesozoic igneous rocks in Southeastern China: fi Wang, D.Z., Zhao, G.T., Qiu, J.S., 1995. The tectonic constraint on the late Mesozoic A- implications for lithosphere subduction and underplating of ma c magmas. Tecto- – – type granitoids in eastern China. Geological Journal of Chinese Universities 1 (2), nophysics 326 (3 4), 269 287. 13–21 (in Chinese). Zhou, X., Sun, T., Shen, W., Shu, L., Niu, Y., 2006. Petrogenesis of Mesozoic granitoids Wang, X.L., Zhou, J.C., Griffin, W.L., Wang, R.C., Qiu, J.S., O'Reilly, S.Y., Xu, X.S., Liu, X.M., and volcanic rocks in South China: a response to tectonic evolution. Episodes 29 – Zhang, G.L., 2007. Detrital zircon geochronology of Precambrian basement se- (001), 26 33. quences in the Jiangnan orogen: dating the assembly of the Yangtze and Cathaysia Zhu, D.S., Hu, Y.H., Guan, S.G., 1994. A discovery of animal fossils in the Hexi Group Blocks. Precambrian Research 159 (1–2), 117–131. low-grade metamorphic rocks at Zhixitou of Qingtian county, Zhejiang. Geology – Wang, L.J., Yu, J.H., O'Reilly, S.Y., Griffin, W.L., Sun, T., Wei, Z.Y., Shu, L.S., Jiang, S.Y., of Zhejiang 10 (2), 9 12 (in Chinese). 2008. Grenvillian orogeny in the Southern Cathaysia Block: constraints from U– Zhu, D.C., Mo, X.X., Zhao, Z.D., Niu, Y., Wang, L.Q., Chu, Q.H., Pan, G.T., Xu, J.F., Zhou, C.Y., Pb ages and Lu–Hf isotopes in zircon from metamorphic basement. Chinese Sci- 2010. Presence of Permian extension- and arc-type magmatism in southern Tibet: – ence Bulletin 53 (14), 1680–1692. paleogeographic implications. Geological Society of America Bulletin 122 (7 8), – Wang, L.J., Griffin, W.L., Yu, J.H., O'Reilly, S.Y., 2010a. Precambrian crustal evolution of 979 993. the Yangtze Block tracked by detrital zircons from Neoproterozoic sedimentary rocks. Precambrian Research 177, 131–144.