COVER The G-quadruplex is a special secondary structure formed by G-rich DNA sequences that is stabilized by Hoogsteen hydrogen bonding among four guanine bases arranged in a square planar configuration. G-quadruplexes have attracted growing interest in recent years as studies imply that these DNA motifs are associated with various cancers. As a motif present under physiological conditions, flanking sequences are recognized as important parts of G-quadruplexes. However, the impact of flanking sequences on (G-quadruplex)-ligand binding remains unresolved. To address this issue, we have studied the effect of flanking sequences on ligand binding to G-quadruplexes. The results showed that flanking sequences play critical roles in the interaction between c-myc G-quadruplexes and their ligands. It was found that the c-myc G-quadruplex with two flanking tails presents the strongest binding affinity to the two studied ligands, followed by the c-myc G-quadruplex with only one tail and finally that without any flanking tails. Molecular simulation studies indicated that the flanking sequence folded into a binding cavity by forming a fold-back structure above the terminal G-quartet. Such a structure may provide a suitable site for the docking of ligands. This structure may stabilize the (c-myc G-quadruplex)-ligand complex effectively and increase the binding affinity dramatically (see the article by GAI Wei et al. on page 731).

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Volume 58 Number 7 March 2013

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CONTENTS CONTENTS

Volume 58 Number 7 March 2013

Progress of Projects Supported by NSFC

REVIEW

Geology 701 The Lantian biota: A new window onto the origin and early evolution of multicellular organisms YUAN XunLai, CHEN Zhe, XIAO ShuHai, WAN Bin, GUAN ChengGuo, WANG Wei, ZHOU ChuanMing & HUA Hong

INVITED ARTICLE Materials Science 708 Facile synthesis of Ca-α-SiAlON:Eu2+ phosphor by the microwave sintering method and its photoluminescence properties LIU LiHong, ZHOU XiaoBing, XIE Rong-Jun & HUANG Qing

ARTICLES Applied Physics 713 Dielectric anomalies in CaCu3Ti4O12 at high temperatures ZHANG MeiNi, XU KeBiao, WANG GuoJing & WANG ChunChang

Organic Chemistry 717 Tandem addition-cyclization reaction catalyzed by ytterbium chloride: An efficient one-step synthesis of 2-amino-4H-3,1-

benzothiazine HUANG Jie, YU Yong, HUA Lu, YAO ZhiGang, XU Fan & SHEN Qi

Environmental Chemistry 724 Characterization and assessment of volatile organic compounds (VOCs) emissions from typical industries WANG HaiLin, NIE Lie, LI Jing, WANG YuFei, WANG Gang, WANG JunHui & HAO ZhengPing

Chemical Biology 731 Roles of flanking sequences in the binding between unimolecular parallel-stranded G-quadruplexes and ligands GAI Wei, YANG QianFan, XIANG JunFeng, SUN HongXia, SHANG Qian, LI Qian, JIANG Wei, GUAN AiJiao, ZHANG Hong, TANG YaLin & XU GuangZhi

Preventive Medicine & Hygienics 741 Influence of extreme weather and meteorological anomalies on outbreaks of influenza A (H1N1) XIAO Hong, TIAN HuaiYu, LIN XiaoLing, GAO LiDong, DAI XiangYu, ZHANG XiXing, CHEN BiYun, ZHAO Jian & XU JingZhe

Ecology 750 Impacts of changed litter inputs on soil CO2 efflux in three forest types in central south China YAN WenDe, CHEN XiaoYong, TIAN DaLun, PENG YuanYing, WANG GuangJun & ZHENG Wei

758 Soil fungi of three native tree species inhibit biomass production and shift biomass allocation of invasive Mikania micrantha Kunth

GAO Lei, ZAN QiJie, LI MingGuang, GUO Qiang, HU Liang, JIANG Lu, ZHOU Sheng & LIU HaiJun 766 Molecular cloning of partial 14-3-3 genes in the marine sponge Hymeniacidon perleve and its role in differentiating

infectious and non-infectious bacteria FU WanTao, ZHANG JuLin, ZHENG ChangBo, LIU Jing, AN ZhongFu, LIU HongWen & ZHANG Wei

Geochemistry 777 Zircon U/Pb dating and Hf-O isotopes of the Zhouan ultramafic intrusion in the northern margin of the Yangtze Block, SW

China: Constraints on the nature of mantle source and timing of the supercontinent Rodinia breakup WANG MengXi, WANG ChristinaYan & ZHAO JunHong

Geology 788 Late Paleozoic magmatism in South China: Oceanic subduction or intracontinental orogeny? YU JinHai, LIU Qian, HU XiuMian, WANG Qin & O’REILLY Suzanne Y

796 High-resolution stalagmite δ13C record of soil processes from southwestern China during the early MIS 3 LIU DianBing, WANG YongJin, CHENG Hai & EDWARDS R L

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803 Calibration of the U3K7′ index of long-chain alkenones with the in-situ water temperature in Lake Qinghai in the Tibetan

Plateau WANG Zheng & LIU WeiGuo

Atmospheric Science809 Sensitivity experiments of impacts of large-scale urbanization in East China on East Asian winter monsoon CHEN HaiShan & ZHANG Ye

Materials Science816 Effect of rare earth elements on the structures and mechanical properties of magnesium alloys LÜ Zhong, ZHOU Jian, SUN ZhiMei & CHEN RongShi

821 Room temperature H2S micro-sensors with anti-humidity properties fabricated from NiO-In2O3 composite nanofibers YUE XueJun, HONG TianSheng, YANG Zhou & HUANG ShuangPing

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Article

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Geology March 2013 Vol.58 No.7: 788795

doi: 10.1007/s11434-012-5376-8

Late Paleozoic magmatism in South China: Oceanic subduction or intracontinental orogeny?

YU JinHai1,2*, LIU Qian1, HU XiuMian1, WANG Qin1 & O’REILLY Suzanne Y2

1 State Key Laboratory for Mineral Deposits Research, School of Earth Sciences and Engineering, Nanjing University, Nanjing 210093, China; 2 GEMOC ARC National Key Centre, Department of Earth and Planetary Sciences, Macquarie University, Sydney, N.S.W. 2109, Australia

Received March 9, 2012; accepted May 31, 2012; published online November 14, 2012

A gneissic granite with an U-Pb age of 313±4 Ma was found in northeastern Fujian Province, South China. It is an S-type granite characterized by high K2O, Al2O3 and low SiO2, Na2O contents with high A/CNK ratio of 1.22 for the whole rock. Zircons with stubby morphology from the gneissic granite yield 206Pb/238U ages ranging from 326 to 301 Ma with a weighted average age of 313±4 Ma, and negative Hf(t) values from 8.35 to 1.74 with Hf model ages (TC

DM) of 1.43 to 1.84 Ga. This S-type granite probably originated from late Paleoproterozoic crust in intracontinental orogeny. Integrated with previous results on paleogeo-graphic reconstruction of South China, the nature of Paleozoic basins, Early Permian volcanism and U-Pb-Hf isotope of detrital zircons from the late Paleozoic to early Mesozoic sedimentary rocks, we suggest the occurrence of a late Paleozoic orogeny in the eastern Cathaysia Block, South China. This orogenic cycle includes Late Carboniferous (340–310 Ma) orogeny (compression) episode and Early Permian (287–270 Ma) post-orogenic or intraplate extension episode. Therefore, the late Paleozoic magmatism in the southeastern South China probably occurred during the intraplate orogeny rather than the arc-related process.

S-type granite, zircon U-Pb age, zircon Hf isotope, late Paleozoic orogeny, South China

Citation: Yu J H, Liu Q, Hu X M, et al. Late Paleozoic magmatism in South China: Oceanic subduction or intracontinental orogeny? Chin Sci Bull, 2013, 58: 788795, doi: 10.1007/s11434-012-5376-8

The South China Block (SCB) is comprised of the Yangtze Block to the northwest and the Cathaysia Block to the southeast. The Yangtze Block is characterized by Me-so-Neoarchean crystalline basement in the Kongling terrain and widespread Neoproterozoic magmatic rocks in the pe-riphery of the block [1–8]. In the Cathaysia Block, the old basement rocks include Paleoproterozoic granites and late Neoarchean metamorphic rocks of the Badu Group [9–12], with minor Neoproterozoic magmatic rocks in the Wuy-ishan area [13–15]. Notably, the Cathaysia Block experi-enced three episodes of intense Phanerozoic granitic mag-matism: early Paleozoic (Caledonian), early Mesozoic (In-dosinian) and late Mesozoic (Yanshanian) [16]. Although the late Paleozoic (Hercynian) magmatism was reported previously [17–19], little attention was paid due to lack of accurate dating results. In the past few years, some Permian

granitic and alkaline magmatism (287–262 Ma) and meta-morphism have been identified in Hainan Island and Luoding area of Guangdong Province [20–23]. Li et al. [20]

interpreted that ~265 Ma granitic magmatism in Hainan Island was induced by the subduction of the Paleo-Pacific ocean plate beneath the SCB. By contrast, Xie et al. [21] argued that ~272 Ma shoshonitic intrusive rocks in Hainan Island were generated in the early stage of a post-collisional event. They related it to the amalgamation of the SCB with the Indochina-South China Sea plate during the conver-gence of the late Paleozoic Pangea supercontinent. Recently, 340–280 Ma detrital zircons were found in late Paleozoic sedimentary rocks in the SCB [24,25], stimulating interest in the late Paleozoic tectonics and magmatism. However, the sedimentary provenances of detrital zircons and the na-ture of their host magma are very difficult to decipher. Therefore, the geological significance of these zircons re-mains controversial.

Yu J H, et al. Chin Sci Bull March (2013) Vol.58 No.7 789

This study determines a Late Carboniferous granitoid in the Wufenglou village, Zhouning County of Fujian Province, which throws light on the characteristics of the late Paleo-zoic magmatism in the SCB and its relationship with the late Paleozoic Pangea supercontinent.

1 Geological background and sample description

The coastal region of the SCB can be divided into three parts by the NE-striking Zhenghe-Dabu and Changle- Nan’ao faults (Figure 1(a)). The Caledonian fold belt is lo-cated to the west of the Zhenghe-Dabu fault, containing Precambrian basement rocks, early Paleozoic sedimentary rocks and Caledonian granites, whereas late Mesozoic gran-ites, volcanic and sedimentary rocks are dominant to the east of the fault. The Changle-Nan’ao fault along the coast-line of Fujian Province separates the Pingtan-Dongshan metamorphic belt in the east from the inland Mesozoic ig-neous belt [26]. However, some high-grade metamorphic rocks and Paleozoic sedimentary rocks are sparsely exposed as inliers to the east of the Zhenghe-Dabu fault. It is worthy to note that these inliers are confined to the west of the Fu’an-Nanjing fault (Figure 1(a)). Although the Fu’an- Nanjing fault have not been clearly recognized due to the extensive covering of Mesozoic volcanic rocks, geophysical data show sharp gradients of bouguer gravity and aeromag-

netic anomalies along the Fu’an-Nanjing fault [27]. Thus, the Fu’an-Nanjing fault is probably an important tectonic boundary constraining the distribution of old basement.

A fresh granitic gneiss sample was collected near the Wufenglou village, Zhouning County of Fujian Province, to the east of the Zhenghe-Dabu fault (Figure 1). In the 1:250000 geological map of Fuzhou region1), these meta-morphic rocks sporadically outcropping in the study area are classified as the late Neoproterozoic Longbeixi For-mation. The outcrop covers approximately 2.3 km2 around the Wufenglou village, hosted by Early Cretaceous Makeng granite. The Makeng granite intrudes into Late Jurassic to Early Cretaceous volcanic rocks (the Nanyuan Formation) and is overlaid by Early Cretaceous volcanic rocks of the Zhaixia Formation. Many exposed gneisses have suffered intense weathering.

Sample FN10-5-2 is a biotite-rich granitic gneiss with porphyroclastic texture (Figure 2), suggesting that it under-went brittle-ductile deformation. Quartz grains show static recrystallization, and the elongated contours of their fine- grained aggregates indicate ductile-shear deformation. Bio-tite grains are also fine-grained, and K-feldspar and minor plagioclase grains show brittle cracking (Figure 2(b)). Major element contents were analyzed using an ARL 9800XP+ X-ray fluorescence spectrometer (XRF) at the Centre of Modern Analysis, Nanjing University. Sample FN10-5-2 contains SiO2 content of 65.49%, TiO2 of 0.59%, Al2O3 of 16.20%, total Fe2O3 of 4.17%, MnO of 0.06%,

Figure 1 (a) Geological frame of Fujian Province, eastern South China. (b) Simplified geological map of the study area (modified from 1:250000 geologi-cal map of Fuzhou region1)). ① the Changle-Nan’ao fault; ② the Zhenghe-Dabu fault; ③ the Fu’an-Nanjing fault. The outcrops of Precambrian strata

are mainly after refs. [26]; 1, late Cretaceous intrusive rocks; 2, early Cretaceous basaltic rocks; 3, early Cretaceous granites; 4, Cretaceous subvolcanics; 5, Cretaceous sediments; 6, late Jurassic granites; 7, Jurassic subvolcanics; 8, Jurassic sediments; 9, Permian intrusive rocks; 10, Silurian intrusive rocks; 11, Carboniferous metamorphic rocks.

1) Institute of Geology Survey of Fujian Province. 1:250000 Geological Map of Fuzhou Region. 2006.

790 Yu J H, et al. Chin Sci Bull March (2013) Vol.58 No.7

Figure 2 Field outcrop (a) and photomicrograph (b) of the Wufenglou gneissic granite (FN10-5-2). Bt, Biotike; kf, K-feldspar; pl, plagioclase; Qz, quartz.

MgO of 1.74%, CaO of 2.07%, Na2O of 1.83%, K2O of 6.06% and P2O5 of 0.12%. Clearly, it shows an affinity with typical S-type granites characterized by high contents of K2O and Al2O3, and low SiO2 and Na2O contents with low Na2O/K2O ratio of 0.30 and high A/CNK value of 1.22.

2 U-Pb ages and Hf-isotope compositions of zircons

Zircon grains from the sample FN10-5-2 are prismatic to stubby prismatic, colorless to light grey, and transparent with no inclusions. They have prism faces of {110} = {100}, and pyramid faces of {101} = {211} or {101} < {211}. Most zircons display oscillatory zoning in CL images (Fig-ure 3(a),(c)–(e)) with minor planar zoned structures (Figure 3(b)), indicating their magmatic origin. All grains do not show obvious overgrowth rims and a few have irregular inherited cores (Figure 3(d)). Th/U ratios of these zircons range from 0.13 to 0.81 with a mean of 0.34, also suggest-ing a magmatic genesis.

CL imaging, LA-ICPMS U-Pb dating and MC-ICPMS Hf-isotope analyses of zircons were carried out at GEMOC National Key Centre, Macquarie University, Australia. De-

tailed analyses procedures and corrections are referred to papers [12,28,29]. Nineteen analyzed zircons have similar ages (Table 1). Seventeen zircons with ages ranging from 326 to 301 Ma yield a weighted average 206Pb/238U age of 313±4 Ma (MSWD = 1.5) (Figure 4), which represents the intrusive age of this gneissic granite. One grain with the youngest age of 285 Ma has abnormally low Th and U con-tents and large analytical error, whereas the older age of 334 Ma from another grain is probably due to the minor mixing of its inherited core during laser ablation.

MC-ICPMS analyses show that thirteen zircons have rel-atively homogeneous Hf-isotope compositions with 176Hf/ 177Hf ratios of 0.282354 to 0.282534, negative Hf(t) values of 8.35 to 1.74 (a mean of 6.0) and two-stage Hf model ages (TC

DM) from 1.43 Ga to 1.84 Ga (an average of 1.70 Ga) (Table 2). The results suggest that the host magma of these zircons probably derived from the late Paleoproterozoic crust [12,14].

3 Discussion and conclusions

Due to late metamorphism and deformation, the petrogra-phy of this granitic gneiss cannot be used directly to infer

Figure 3 CL images of zircons from the Wufenglou gneissic granite. Small circles are dating dots; big circles are Hf-isotope analysis dots; scale bars are 50 μm.

Yu J H, et al. Chin Sci Bull March (2013) Vol.58 No.7 791

Table 1 U-Pb ages of zircons in the Wufenglou meta-granite, Fujian Province

Grain No.

Isotopic ratios Age(Ma) Th

(ppm) U

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

1 0.05314 0.00119 0.36493 0.01272 0.04981 0.00110 335 52 316 9 313 7 80 404 0.20 2 0.05248 0.00107 0.34960 0.01110 0.04831 0.00101 306 48 304 8 304 6 311 404 0.77

2B 0.05225 0.00111 0.34916 0.01140 0.04847 0.00101 296 50 304 9 305 6 52 408 0.13 3B 0.05239 0.00160 0.34483 0.01587 0.04774 0.00119 302 71 301 12 301 7 81 407 0.20 4 0.05285 0.00137 0.35593 0.01392 0.04884 0.00109 322 60 309 10 307 7 87 541 0.16

5C 0.05264 0.00196 0.35505 0.01883 0.04897 0.00115 313 87 309 14 308 7 85 361 0.24 6 0.05279 0.00110 0.34910 0.01090 0.04796 0.00093 320 48 304 8 302 6 126 424 0.30 7 0.05272 0.00108 0.36500 0.01134 0.05021 0.00100 317 48 316 8 316 6 260 347 0.75 8 0.05583 0.00118 0.38857 0.01271 0.05049 0.00108 446 48 333 9 318 7 147 352 0.42 9 0.05274 0.00089 0.36519 0.00968 0.05022 0.00097 318 39 316 7 316 6 103 520 0.20 10 0.05406 0.00096 0.38153 0.01037 0.05119 0.00097 374 41 328 8 322 6 223 777 0.29 11 0.05296 0.00118 0.37504 0.01294 0.05136 0.00113 327 52 323 10 323 7 81 481 0.17 12 0.05273 0.00107 0.36568 0.01142 0.05031 0.00102 317 47 316 8 316 6 95 676 0.14 14 0.05272 0.00104 0.35938 0.01101 0.04945 0.00101 317 46 312 8 311 6 312 384 0.81 20 0.05312 0.00108 0.37496 0.01168 0.05120 0.00103 334 47 323 9 322 6 108 457 0.24 23 0.05264 0.00116 0.35598 0.01204 0.04906 0.00105 313 51 309 9 309 6 188 454 0.41 27 0.05296 0.00134 0.37875 0.01471 0.05187 0.00122 327 59 326 11 326 7 316 814 0.39 22 0.05329 0.00116 0.39109 0.01304 0.05324 0.00111 341 50 335 10 334 7 75 395 0.19 3 0.05236 0.00668 0.32644 0.06038 0.04522 0.00257 301 289 287 46 285 16 5 28 0.18

Table 2 Hf-isotope compositions of zircons in the Wufenglou gneissic granite

Grain No.

176Hf/177Hf 1σ 176Lu/177Hf 1σ 176Yb/177Hf Age

Hf i Hf(t) T(DM) T C

(DM) (Ma) (Ga) (Ga)

2B 0.282408 0.000010 0.00174 0.00002 0.05967 305 0.282398 6.53 1.22 1.73 3 0.282397 0.000011 0.00134 0.00001 0.05033 285 0.282390 7.26 1.22 1.76

3B 0.282367 0.000012 0.00193 0.00005 0.07383 301 0.282356 8.11 1.28 1.82 4 0.282354 0.000023 0.00153 0.00002 0.06641 307 0.282345 8.35 1.29 1.84 6 0.282425 0.000010 0.00161 0.00002 0.06059 302 0.282416 5.97 1.19 1.69 7 0.282534 0.000011 0.00121 0.00002 0.04627 316 0.282527 1.74 1.02 1.43 9 0.282409 0.000012 0.00151 0.00002 0.06572 316 0.282400 6.22 1.21 1.72 11 0.282431 0.000011 0.00164 0.00003 0.07008 323 0.282421 5.32 1.18 1.67 14 0.282526 0.000016 0.00166 0.00002 0.07786 311 0.282516 2.21 1.05 1.46 20 0.282423 0.000007 0.00141 0.00002 0.05684 322 0.282415 5.58 1.19 1.68 22 0.282363 0.000016 0.00144 0.00002 0.05930 334 0.282354 7.44 1.27 1.81 23 0.282382 0.000007 0.00150 0.00004 0.05682 309 0.282373 7.32 1.25 1.78 27 0.282403 0.000010 0.00173 0.00003 0.06664 326 0.282392 6.27 1.23 1.73

Figure 4 U-Pb concordia diagram of zircons from the Wufenglou gneissic granite.

the protolith type, while the whole-rock composition can provide important constraint on the nature of the protolith. Generally, regional metamorphism is a closed system and makes negligible changes to major element compositions. Strong mylonitization, in some cases, may increase SiO2

content and decrease contents of other oxides. In this study, the Wufenglou gneiss shows low SiO2 content of 65.49% (relative to average value of granites) and weak ductile de-formation, suggesting that its chemical compositions were not significantly changed. Consequently, its whole-rock composition can reflect its original components. High K2O, Al2O3 contents (A/CNK = 1.22) indicate that the protolith of the Wufenglou gneiss presumably is S-type granite or sedi-mentary rocks (e.g. arkosic sandstone). However, euhedral morphology and same ages of zircons indicate that the pro-tolith of this sample probably is S-type granite. Thus, the zircon U-Pb age of 313±4 Ma represents the formation age of the Wufenglou gneissic granite. It is the first report about

792 Yu J H, et al. Chin Sci Bull March (2013) Vol.58 No.7

the Late Carboniferous granitic magmatism in South China with accurate isotope chronology. Negative Hf(t) values of zircons with Hf model age of ~1.7 Ga suggest that the orig-inal magma of the S-type granite probably derived from a crust which is mainly composed of late Paleoproterozoic component. In fact, Hu et al. [24] and Li et al. [25] have reported the possible occurrence of 340–280 Ma magma-tism in South China according to U-Pb ages of detrital zir-cons in sedimentary rocks. However, the nature and the location of host magma producing those detrital zircons have not been well constrained.

Hu et al. [24] found numerous late Paleozoic detrital zir-cons from Permian and Jurassic sedimentary rocks in the Fuding inlier, 90 km northeast of the Wufenglou village. The detrital zircons from their Permian sedimentary rocks exhibit an U-Pb age peak of 320–290 Ma, with minor mid-late Paleoproterozoic (1.9–1.7 Ga) and late Archean to early Paleoproterozoic (2.55–2.35 Ga) ages. The detrital zircons in the Jurassic sedimentary rocks were mainly formed at 1.85–1.75 Ga and 345–330 Ma (Figure 5). Hu et al. [24] proposed that the detrital zircons probably originat-ed from the northeastern Cathaysia Block and recorded the late Paleozoic magmatism in the continental rifting setting. However, the lack of direct geochemical and isotope evi-dence of protolith hampers them to exclude an alternative scenario that the late Paleozoic magmatism occurred in the continental arc environment related to the oceanic subduc-tion. Recently, Li et al. [25] determined late Paleozoic (~280 Ma) and early Paleozoic (~370 Ma) detrital zircons from Permian sedimentary rocks in Shaoguan, Leiyang, Ji’an and Yongding areas in the SCB (Figure 5). They at-tributed the ~280 Ma magmatism as an Early Permian ac-tive continental margin in southeastern China due to sub-duction of the Paleo-Pacific plate. However, it is well estab-lished that both oceanic arc and continental arc are charac-terized by the relative depletion of high field strength ele-ments (HFSE) [30]. Consequently, element Zr is undersatu-rated in primary arc-type melts and thus zircon is not able to crystallize from them [30]. Thus, detrital zircons with the U-Pb age of late Paleozoic would not come from the pri-mary arc magmas, but derive from secondary arc-derived magmas due to remelting of arc-type rocks in which Zr be-comes saturated to crystallize zircon [31].

Late Paleozoic detrital zircons from the Fuding Permian sedimentary rocks in Fujian Province have negative Hf(t) values (19.9 to 3.1, Figure 6), suggesting that these zir-cons probably came from S-type granitic rocks. It is con-sistent with the discovery of the Wufenglou gneissic S-type granite. S-type granites are generally considered to be gen-erated in the intraplate orogeny and continental collisional orogeny [32–39]. Hence, the identification of Late Carbon-iferous S-type granite, coupled with the absence of coeval basaltic and andesitic magmatism in the SCB, can primarily exclude that the late Paleozoic magmatism took place in the subduction-related arc setting.

Figure 5 Age comparison of the late Paleozoic zircons in the SCB.

In fact, the early Paleozoic (Caledonian) and the early Mesozoic (Indosinian) magmatism are also characterized by predominant S-type granites with little volcanism, sharing typical tectonic characteristics of intraplate orogeny and continental collisional orogeny [40–44]. Early Permian (~280 Ma) detrital zircons reported by Li et al. [25] have younger ages, and positive Hf(t) values (Figure 6), distin-guishable from the magmatic zircons of the Wufenglou granite and the Fuding detrital zircons [24]. Therefore, Ear-ly Permian magmatism probably involves the input of juve-nile materials, which is different from Late Carboniferous magmatism.

Volcanic rock interbeds in Permian sedimentary rocks were found in many places of the SCB [45–49]. Permian basaltic volcanic rocks, including pillow basalts and spilite,

Yu J H, et al. Chin Sci Bull March (2013) Vol.58 No.7 793

Figure 6 Hf-isotope compositions of zircons from the Wufenglou gneissic granite. Other data source: Fuding from [24]; Ji’an, Leiyang and Yongding from [25].

were found in the western Cathaysia Block [50]. In addition, alkaline rocks with ages of 287–272 Ma were discovered in Hainan Island [21], coincident with detrital zircons reported by Li et al. [25]. These rocks were mainly generated in the extensional tectonic setting. Furthermore, Permian sedi-mentary basins in the SCB are intracontinental fault basins or rifting basins [51–53]. Paleogeographic reconstruction shows that the coastal region of Zhejiang-Fujian Province was an “old land” during Late Devonian to Late Carbonif-erous, and the entire SCB was covered by seawater in Early Permian [54–56]. Because Early Permian is regarded as global icehouse period [57–59], extensive marine sedimen-tation in the SCB during this period should result from the regional subsidence of a continental margin by tectonics rather than by the increase of the global sea level. All above evidence demonstrates that the SCB was subjected to an extensional tectonic setting during the Early Permian. In the extension environment, the upwelling mantle flow would induce the partial melting of the lower crust to generate volcanism [45–49] as well as the eruption of lithospheric mantle-derived basaltic magma [50]. Hence, Early Permian magmatism in the SCB is characterized by volcanism in the extensional setting, and partial melting of the juvenile crust would produce the Zr-saturated magma [30,31], consistent with positive Hf(t) values of most ~280 Ma zircons [25]. Therefore, we propose that the eastern SCB experienced a late Paleozoic orogenic cycle from Late Carboniferous (340–310 Ma) orogenic (compression) episode to Early Permian (287–270 Ma) post-orogenic or intraplate exten-sion episode. Therefore, late Paleozoic igneous rocks were induced under intraplate orogeny rather than arc-related tectonic setting.

This late Paleozoic orogeny mainly occurred in the east-ern South China. The reason that it was not recognized be-

fore can be due to voluminous late Mesozoic volcanic rocks in the eastern SCB. Another possible reason is that the oro-genic belt has been severely eroded. Paleogeographic re-construction shows the eastern South China has experienced a tectonic uplifting since the late Early Permian, which may cause the extensive erosion of the orogen and westward Paleo-waterflow [25,55,56] and provide massive clastic materials to the inland basins (e.g. Shaoguan, Leiyang, Ji’an and Yongding areas). The Wufenglou gneissic granite with a U-Pb age of ~313 Ma is the direct evidence for the exist-ence of the late Paleozoic orogen in the eastern South China.

The late Paleozoic orogeny in the eastern SCB is coinci-dent with the significant Hercynian magmatism in Europe and assembly-breakup orogeny of the late Paleozoic Pangea supercontinent. The distribution and nature of the late Paleozoic orogen in the eastern SCB and its relationship with the Pangea supercontinent need further study.

Most analytical work was carried out at GEMOC, Earth and Planetary Sciences, Macquarie University, using instruments funded by DEST Sys-temic Infrastructure Grants, ARC LIEF, NCRIS, Industry partners and Macquarie University. We thank Su Bin, Cui Xiang and Xu Hai for their help in field work, and Dr. Norman Pearson and E.A. Belousova for assis-tance in lab at GEMOC National Key Centre, Macquarie University, Aus-tralia. This work was supported by the National Basic Research Program of China (2012CB416701), the National Natural Science Foundation of China (40972127) and the State Key Laboratory for Mineral Deposits Research (Nanjing University) (ZZKT-201106). This is contribution 827 from the Australia Research Council National Key Centre for Geochemical Evolution and Metallogeny of Continents (www.geomoc.mq.edu.au).

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