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Baisha Fault (Metcalfe, 1996), tectonically equivalent to the South China and Indochina blocks, respectively. In addition, the Permian I-type granitoids and the Early Triassic WNW-trending structural deformation occurred in Hainan as the important carries of the assemblage of the South China with Indochina blocks (Fig. 1b; e.g., Zhang et al., 2011; Chen et al., 2011; Li et al., 2006; Metcalfe, 2002, 1996). Thus, Hainan Island is inclined to be a probable area for revealing the Eastern Paleotethyan tectonic evolution (e.g., He et al., 2016a, b; Zhang et al., 2011; Xu et al., 2008; Li et al., 2002; Ma et al., 1998; Metcalfe, 1996). In Central Hainan, volcanic rocks have been identified in Bangxi-Chenxing zone, which may record signifi-cant meaning to the Late Paleozoic evolution (e.g., He et al., 2017; Chen et al., 2014; Li et al., 2002). To address these ques-tions above, we presented new zircon U–Pb geochronology and whole-rock geochemical, elemental and Sr–Nd isotopic results on representative volcanic rocks at the Chenxing and Bangxi areas in Central Hainan, with the aim to better constrain the age and petrogenesis of the volcanic rocks, and to understand the temporal-spatial relationship with the Jinsha-jiang-Ailaoshan-Song Ma zone along with the tectonic implica-tions of the Paleotethyan evolution in SE Asia. 1 GEOLOGICAL SETTINGS

Hainan Island, separated from China Mainland by the-Qiongzhou Strait, is an important element in tectonicrecon-structions between the Indochina and South China blocks (Guangdong BGMR, 1988). It is characterized by four

EW-trending Wangwu-Wenjian, Changijang-Qionghai, Jian-feng-Diaoluo and Jiusuo-Linshui faults and two NE-trending Gezhen-Lingao and Baisha faults, respectively (Fig. 1b; e.g., Xie et al., 2009; Xia et al., 1990, 1991a, b;Wang et al., 1991, 1992; Guangdong BGMR, 1988). Due to the structural over-printing, there occurred numerous tectonic fragments.

The mainly component consist of the stratigraphical se-quences are Precambrian Baoban and Shilu groups, along with Paleozoic marine and Mesozoic terrestrial packages (e.g., Long et al., 2002; Ma et al., 1998). Mesoproterozoic Baoban Group, mainly preserved in western Hainan, has traditionally consi-dered to be the crystallized basement in Hainan. However, the contact relationship is poorly observed between the Baoban Group and Shilu Group, which only exposed in NW Hainan (e.g., Li et al. 2002; Wang et al., 1991, 1992; Guangdong BGMR, 1988). Available data show that previously-defined Baoban and Shilu groups are the Mesoproterozoic (~1420 Ma) complexes constituted by granitic gneiss, migmatite, metamor-phic volcanics, paragneiss, quartz-mica schist, quartzite and a small amount of amphibolite fragments/pods (e.g., Li et al., 2002; Ma et al., 1998; Wang et al., 1991). Detrital zircons from the Baoban and Shilusupracrustal sedimentary rocks had tec-tonothermal records of the Columbia breakup and Grenvillian orogeny (Li et al., 2002). The Neoproterozoic rocks are poorly identified in Hainan Island. The Lower Paleozoic sequences mainly outcropped in Central Hainan andare dominated by-Cambrian and Ordovician siltstone, sandstone and slate as well

Figure 1. (a) Tectonic outline of Southeast Asia (revised after Wang et al., 2010), (b) geological map of Hainan Island showing sampling locations and (c–d)

simplified geological maps for the Bangxi and Chenxing areas, respectively (revised after Guangdong BGMR, 1988).

as Lower Silurian sandstone (Long et al., 2007; Hu et al., 2001; Tang and Feng et al., 1998; Wang et al., 1991, 1992; Xia et al.,

Carboniferous arc setting in Central Hainan: Geochronologi-cal and geochemical evidences on the andesitic and dacitic rocks 3

1990). The Upper Paleozoic sequences have commonly under-gone the greenschist-facies metamorphism and consist of De-vonian sandstone, Carboniferous slate and volcanics, Lower Permian limestone and Middle Permian sandstone to north of the Jiusuo-Lingshui Fault (Long et al., 2007; Hu et al., 2001; Tang and Feng et al., 1998; Wang et al., 1991, 1992; Xia et al., 1990). The Mesozoic strata in Hainan mainly involve the Upper Triassic siliciclastic rocks and Cretaceous sandstones (Wang et al., 1991). Middle Triassic sandstone is unconformably under-lain by pre-Triassic package and overlain by Jurassic or Lower Cretaceous terrestrial siliciclastics.

The Mesoproterozoic Baoban granitic gneiss (e.g., Gongai and Ledong) and the Permian Wuzhishan and Wanning gneissic granites are the important component of foliated and gneissic granites in Hainan (e.g., Chen et al., 2011; Li et al., 2002; Wang et al., 1991). The granitic rocks with the ~ 60% acreage of Hainan Island composed of monogranites, biotite granites and granodiorites are the remarkable geological signature in Hainan Island, dominated by the Indosinian (e.g., Qiongzhong and Jianfengling) and Yanshanian (e.g., Danxian, Tunchang, Qian-jia and Baochen) with the exception of the Permian gneissic granites (Chen et al., 2013; Wang et al. 1991). In addition, a small amount of mafic rocks has been observed in Hainan Isl-and, mainly including the Mesoproterozoic Baobanmetabasites, Late Paleozoic–Early Mesozoic basaltic, gabbroic and doleritic rocks and Cenozoic basalt. The recently-identified Carbonifer-ous volcanic rocks are characterized by MORB-like metaba-sites, which are interpreted to generate in a back-arc basin (He et al., 2017; Li et al., 2002). Subsequently, the Late Cretaceous to Cenozoic rifting led to the Cenozoic widespread volcanism in Hainan Island and its peripheral areas. In the Bangxi (Changjiang) and Chenxing (Tunchang) areas of Central Hainan, a small amount of andesitic and daciticrocks was identified, which exposed in the Early Paleozoic strata and Permian strata, respectively (Guangdong BGMR, 1988). All Chenxing and Bangxi samples have a similar mineral associa-tion of plagioclase, hornblende and biotite with a porphyrotopic texture. Their phenocrysts include hornblende and biotite, which usually occurs as a euhedral-subhedral columnar crystal in the range of 0.2–0.8 centimeters, whereas the matrix mainly consists of fine-grained plagioclase and volcanic tuffaceous material. Apatite, sphene and zircon are dominating accessory minerals. 2 ANALYTICAL METHODS 2.1 Zircon U–Pb dating

Zircon grains from representative samples were separated using conventional heavy liquid and magnetic techniques in the mineral separation laboratory of the Bureau of Geology and Mineral Resources of Hebei Province. The zircon grains were mounted in epoxy and were documented with cathodolumines-cence (CL) images to reveal their internal structures via a JXA-8100 scanning electron microprobe at the Sun Yat-sen University, Guangzhou. Representative CL images of zircon grains are inserted in Fig. 2. The Neptune Plus MC-ICP-MS coupled with an ArF-193nm laser-ablation system (Resonetic-sResolution M-50-HR) at the Institute of Geochemistry (GIG), the Chinese Academy of Sciences (CAS) was used as Laser

ablation ICP–MS (LA–ICP–MS) zircon U–Pb analyses. The zircon standards 91500 and Plešovice were used to calibrate the U–Th–Pb ratios. In the data table, individual analyses and plots are presented with 2σ errors, and uncertainties in ages are quoted at the 95% confidence level. The detailed analytical procedure follows Xia et al. (2011) and the age calculations and plots and data collection and dealing with questions were made using ICPMSDataCal and ISOPLOT (Liu et al., 1996) and the Isoplot and Squid programs of Ludwig (2003), respectively. The analytical results are shown in Table 1 with 1σ level of uncertainties and 95% confidence level of mean ages for pooled 206Pb/238U results. 2.2 Whole-rock geochemical analyses

The representative samples were collected from the Bang-xi and Chenxing areas in Central Hainan with removed the altered surfaces before crushed to millimeter-scale chips using an agate mill. Chips from all samples were crushed to 200-mesh in an agate mill for major oxide, trace element, and Sr–Nd isotopic analyses. The analytical results are given in Table 2.

Major and trace elements were performed by the X-ray fluorescence (XRF) techniques on the Rigaku RIX 2000 spec-trometer and Perkin-Elmer Sciex ELAN 6000 inductively coupled plasma mass spectrometry (ICP–MS), respectively at the GIG, CAS. The analysis precision generally ranges from 1% to 5%. Detailed sample preparation and analytical procedure followed Li et al. (2002). Analyses of Sr and Nd isotopic ratios were performed on a Neptune Plus multi-collection mass spec-trometry equipped with nine Faraday cup collectors and eight ion counters at the GIG, CAS. The analytical procedures are similar to that reported by Yang et al. (2006). Cation columns and HDEHP coated Kef columns were used to separated Sr, rare earth elements and Nd, respectively. The total procedural blank is in the range of 200–500 pg for Sr and less than 50pg for Nd. The mass normalization for 87Sr/86Sr ratio and 143Nd/144Nd ratios are based on 86Sr/88Sr=0.1194 and 146Nd/144Nd=0.7219, respectively. The reported 86Sr/88Sr were adjusted to (NIST) SRM987 standard 86Sr/88Sr=0.710265±12 (2σ) and 146Nd/144Nd were adjusted to the La Jolla standard 146Nd/144Nd=0.511862±10 (2σ) on this MAT-261 mass spec-trometer during the present study, respectively. The Rb, Sr, Sm and Nd abundances measured by ICP–MS are used to calculate the 87Rb/86Sr and 146Nd/144Nd ratios.

3 RESULTS 3.1 Geochronological results

Andesitic (11HN-01A) and dacitic (11HN-21A) samples were selected for zircon U–Pb dating. The majority of the ana-lyzed zircon grains is euhedral and light brown or colorless with oscillatory zoning (Fig. 2).

Andesitic sample (11HN-01A): This sample was taken from the site (N19°25′30″, E109°57′55″) at the Chenxinga-rea.Two clusters are defined by 21 analytical spots with one-constituted by seven spots yielding a weighted mean 206Pb/238Uage of 353±3 Ma (MSWD=0.5) and other by eight a n a l y s e s

J o u r n a l o f E a r t h S c i e n c e , 2 0 1 7 o n l i n e I S S N 1 6 7 4 - 4 8 7 X Printed in China DOI: 10.1007/s12583-017-0936-0

Li, S. B.,He,H. Y., Qian, X., et al., 2017. Carboniferous arc setting in Central Hainan: Geochronological and geochemical evidences on the andesitic and dacitic rocks. Journal of Earth Science.doi: 10.1007/s12583-017-0936-0. http://en.earth-science.net

Table 1LA–ICP–MS zircon U–Pb dating results for the Chenxing and Bangxi samples (11HN-01A and 11HN-21A) in the Bangxi-Chenxing zone

Spot

Concentration Isotope ratio Calculated apparent age (Ma)

Th U Th/U

207Pb/206Pb 207Pb/235U 206Pb/238U 207Pb/206Pb 207Pb/235U 206Pb/238U

Ratio 1σ Ratio 1σ Ratio 1σ Age 1σ Age 1σ Age 1σ

Andesitic sample (11HN-01A)

11HN-01A-01 242 487 0.50 0.0549 0.0003 0.5228 0.0081 0.0691 0.0009 406 11 427 5 431 6

11HN-01A-02 277 413 0.67 0.0534 0.0003 0.4196 0.0064 0.0570 0.0008 346 1 356 5 357 5

11HN-01A-03 153 498 0.31 0.0743 0.0032 1.6247 0.0610 0.1587 0.0034 1048 89 980 24 950 19

11HN-01A-04 303 463 0.65 0.0746 0.0034 1.6674 0.0647 0.1622 0.0038 1056 94 996 25 969 21

11HN-01A-05 269 427 0.63 0.0552 0.0003 0.5266 0.0075 0.0691 0.0008 420 9 430 5 430 5

11HN-01A-06 257 467 0.55 0.0537 0.0003 0.4196 0.0059 0.0566 0.0007 367 11 356 4 355 4

11HN-01A-07 300 361 0.83 0.0563 0.0004 0.5425 0.0075 0.0699 0.0008 465 15 440 5 436 5

11HN-01A-08 291 451 0.65 0.0549 0.0003 0.5241 0.0078 0.0691 0.0009 409 11 428 5 431 5

11HN-01A-09 192 485 0.40 0.0555 0.0003 0.5304 0.0083 0.0692 0.0010 435 5 432 5 431 6

11HN-01A-10 289 410 0.71 0.1124 0.0041 4.7518 0.1425 0.3067 0.0064 1838 68 1776 25 1725 32

11HN-01A-11 245 534 0.46 0.0536 0.0003 0.4164 0.0065 0.0562 0.0007 354 11 354 5 353 5

11HN-01A-12 288 475 0.61 0.0540 0.0003 0.4155 0.0075 0.0556 0.0008 372 10 353 5 349 5

11HN-01A-13 296 441 0.67 0.0551 0.0003 0.5276 0.0084 0.0693 0.0010 417 11 430 6 432 6

11HN-01A-14 314 392 0.80 0.1112 0.0040 4.3848 0.1286 0.2861 0.0060 1819 67 1709 24 1622 30

11HN-01A-15 491 279 1.76 0.0531 0.0004 0.4079 0.0056 0.0558 0.0005 332 14 347 4 350 3

11HN-01A-16 905 877 1.03 0.1595 0.0064 8.5376 0.2847 0.3883 0.0086 2450 69 2290 30 2115 40

11HN-01A-17 234 423 0.55 0.0698 0.0025 1.4420 0.0426 0.1498 0.0031 923 76 907 18 900 17

11HN-01A-18 430 317 1.36 0.0529 0.0003 0.4118 0.0060 0.0566 0.0007 324 18 350 4 355 4

11HN-01A-19 272 491 0.55 0.0540 0.0003 0.4155 0.0066 0.0558 0.0007 372 10 353 5 350 4

11HN-01A-20 324 396 0.82 0.0552 0.0003 0.5303 0.0064 0.0697 0.0006 420 11 432 4 434 4

11HN-01A-21 412 321 1.28 0.0552 0.0003 0.5247 0.0081 0.0692 0.0009 420 13 428 5 431 6

Dacitic sample (11HN-21A)

11HN-21 A -01 936 1643 0.57 0.0665 0.0031 1.4980 0.0716 0.1580 0.0029 833 97 930 29 946 16

11HN-21 A -02 2424 3687 0.66 0.0485 0.0029 0.4024 0.0241 0.0585 0.0012 124 133 343 17 367 8

11HN-21 A -03 498 909 0.55 0.0554 0.0033 0.5296 0.0327 0.0685 0.0013 428 140 432 22 427 8

11HN-21 A -04 789 1305 0.60 0.0700 0.0029 1.5428 0.0621 0.1576 0.0020 928 85 948 25 944 11

11HN-21 A -05 1040 1743 0.60 0.0540 0.0030 0.4145 0.0235 0.0546 0.0009 369 131 352 17 343 5

11HN-21 A -06 265 1350 0.20 0.0710 0.0025 1.6230 0.0541 0.1637 0.0020 958 73 979 21 977 11

11HN-21 A -07 2753 1875 1.47 0.0556 0.0035 0.5296 0.0302 0.0688 0.0013 435 134 432 20 429 8

11HN-21 A -08 728 956 0.76 0.0598 0.0034 0.5595 0.0337 0.0665 0.0011 594 126 451 22 415 7

11HN-21 A -09 517 1976 0.26 0.0959 0.0015 3.7682 0.0646 0.2793 0.0024 1547 30 1586 14 1588 12

11HN-21 A -10 1324 3098 0.43 0.0495 0.0014 0.4889 0.0125 0.0709 0.0007 169 63 404 9 442 4


11HN-21 A -11 543 981 0.55 0.0521 0.0031 0.4130 0.0250 0.0559 0.0009 287 135 351 18 350 6

11HN-21 A -12 768 1512 0.51 0.0898 0.0028 3.0298 0.1091 0.2394 0.0035 1421 61 1415 28 1384 18

11HN-21 A -13 3972 3924 1.01 0.0533 0.0020 0.5213 0.0200 0.0696 0.0008 343 88 426 13 433 5

11HN-21 A -14 614 1558 0.39 0.1674 0.0056 10.7593 0.3562 0.4592 0.0050 2532 57 2503 31 2436 22

11HN-21 A -15 683 752 0.91 0.0916 0.0036 3.3764 0.1336 0.2633 0.0036 1459 74 1499 31 1507 19

giving a weighted mean206Pb/238U age of 432±4 Ma (MSWD=0.2; Fig. 2a). The remaining eight analyses show older apparent ages ranging from 900 Ma to 2450 Ma, which are interpreted as xenocrysts. Considering the weak oscillatory zoning with low to variable luminescence in the CL image for these grains (inset in Fig. 2a), it is believed that these grains are of the magmatic origin and ~350 Ma can represent its forma-tion age.

Dacitic sample (11HN-21A): This sample was collected

from the site (N19°24′47″, E 109°07′56″) nearby the Bangxi Town. Five spots from 15 grains give the apparent 206Pb/238U ages of 415–442 Ma with a weighted mean age of 433±5 Ma (MSWD=3.2) and seven analyses show the apparentages from 944Ma to 2532 Ma, representing the xenocryst grains. The remaining three analyses yield a coherent group with weighted mean age of 351±7 Ma MSWD=3.3) (Fig. 2b), reflective of the crystallization age of the dacitic sample. Such an age is also consistent with the age of Chenxing andesitic sample.

Figure 2. Concordia diagrams of zircon U–Pb data for the Chenxing sample (11HN-01A) (a) and Bangxi sample (11HN-21A) (b), Central Hainan. Insets show

the representative cathodoluminescence (CL) images for the zircon grains.

3.2 Geochemical characteristics

Whole-rock major oxides, trace elements and Sr–Nd iso-topic data for the representative samples are listed in Table 2. The Chenxing samples have SiO2=51.70–65.41 wt.%, MgO=2.93–4.26 wt.%, TiO2=0.62–0.95 wt.% and K2O/Na2O=1.10–2.78. In comparison with those of typical andesites, the Chenxing samples have similar Al2O3 (14.51–21.07 wt.%), higher K2O (2.46–4.31 wt.%) and lower CaO (2.65–4.47 wt.%) contents. The Bangxi samples show relatively slight variation with SiO2 ranging from 60.69 wt.% to 65.50 wt.%, Al2O3 from 14.85 wt.% to 16.53 wt.%, MgO from 1.84 wt.% to 2.45 wt.% and TiO2 from 0.60 wt.% to 1.11 wt.%. Their K2O/Na2O ratios are in the range of 0.82–2.44. These samples fall in the fields of andesite and dacite in the TAS dia-gram (Fig. 3a), and can be classified as calc-alkalic series rocks in the Zr/TiO2–Nb/Y diagram (Fig. 3b, Winchesterand and Floyd, 1977). In the Harker diagram (Fig. 4), MgO, Al2O3, Fe2O3t, TiO2 and P2O5 show a sharply decreasing but weakly variable for CaO with increasing SiO2. Our samples show sim-ilar chondrite-normalized right-sloping REE patterns (Fig. 5a)with Eu/Eu*=0.61–0.77. Their (La/Yb)N and (Gd/Yb)N ra-tios

range from 6.11 to 8.07 and 1.18 to 1.56, respectively. On the primitive mantle-normalized element spidergram (Fig. 5b), these samples are characterized by enrichment in LILEs (e.g., Rb and Ba) and depletion in HFSEs (e.g., Nb, Ta and Ti) and Sr negative anomalies (Sr/Sr*=0.25–0.75). These samples display high Nb/La (0.29–0.37), Zr/Nb (13.79–17.09), Ce/Pb (1.93–4.99), Th/La (0.29–0.36) ratios, resembling to those of arc volcanic rocks in the Lancangjiang igneous rocks (e.g., Peng et al., 2008).

The Sr–Nd isotopic analysis for seven representative sam-ples were shown in Table 2 and Fig. 6. The Chenxing samples have initial 87Sr/86Sr (i) ratios ranging from 0.70847 to 0.71013 and εNd (t) values from -1.4 to -2.0. The initial 87Sr/86Sr (i) ra-tios for the Bangxi samples range from 0.70719 to 0.70818. Both initial 87Sr/86Sr (i) ratios are most likely reflective of the sea-water alteration. The Bangxi samples have higher εNd (t) values ranging from -3.4 to -4.7 than those of the Bangxi sam-ples (-1.4 to -2.0).


Table 2Majoroxides (wt.%), trace element (ppm) and Sr–Nd isotopic results for the andesitic and dacitic samplesin the CentralHainan

11HN--01A 11HN—01B 11HN--01D 11HN--01E 11HN--01H 11HN--01J 11HN--01L 11HN--01K 10HN13C* 10HN14A* 10HN14B*

SiO2 55.48 65.41 59.78 63.24 60.10 64.16 55.34 59.24 65.12 51.70 55.86

TiO2 0.90 0.72 0.77 0.70 0.77 0.74 0.88 0.82 0.62 0.95 0.88

Al2O3 19.25 14.66 17.20 15.59 17.13 15.33 19.41 17.64 14.51 21.07 18.92

Fe2O3t 8.21 6.05 7.64 6.92 7.55 6.52 8.40 7.40 6.86 9.01 8.70

MgO 3.70 2.93 3.51 3.20 3.50 3.00 3.85 3.38 3.33 4.26 4.12

MnO 0.14 0.16 0.09 0.08 0.09 0.12 0.10 0.11 0.14 0.12 0.12

CaO 3.34 4.01 2.92 2.94 2.65 2.93 3.35 3.09 3.72 3.89 3.09

K2O 3.58 2.46 3.39 2.87 3.61 2.75 3.79 3.21 2.74 4.31 4.18

Na2O 2.83 1.60 2.43 2.27 2.36 2.47 2.71 2.91 0.99 2.22 1.80

P2O5 0.22 0.19 0.20 0.19 0.20 0.20 0.22 0.21 0.19 0.24 0.22

LOI 1.93 1.24 1.58 1.54 1.59 1.31 1.52 1.58 1.35 1.79 1.67

Total 99.59 99.44 99.52 99.54 99.54 99.54 99.56 99.58 99.57 99.57 99.57

mg-number 51 53 52 52 52 52 52 52 53 52 52

Sc 22.8 16.9 19.0 17.0 20.0 18.4 21.5 21.0 15.7 26.7

V 160 110 125 114 124 115 144 145 125 157

Cr 44.8 38.6 37.1 36.1 41.0 65.7 44.5 44.8 39.4 66.6

Co 18.8 12.6 16.3 14.1 15.6 13.5 17.1 16.1 17.7 21.8

Ni 25.7 20.9 24.0 20.9 22.6 34.5 26.3 26.5 22.4 33.3

Rb 121 99.7 113 93.0 117 103 128 108 116 136

Sr 217 203 181 177 176 218 215 197 191 205

Y 33.0 28.1 29.0 24.6 29.3 30.0 35.3 30.7 18.5 29.3

Zr 187 176 150 135 154 185 183 170 113 175

Nb 9.65 8.48 8.24 7.67 8.64 9.06 10.1 9.40 7.67 11.2

Cs 7.70 8.79 7.56 6.36 7.45 9.21 8.61 7.73 10.0 12.2

Ba 502 235 481 374 518 335 536 463 266 535

La 32.2 27.9 27.9 23.7 26.1 29.1 32.9 31.1 22.2 32.0

Ce 62.6 52.7 53.7 47.4 51.3 57.3 64.7 61.4 48.1 63.4

Pr 7.58 6.36 6.71 5.73 6.28 7.04 7.92 7.94 5.45 7.48

Nd 31.2 26.2 27.3 23.9 26.3 28.1 31.6 31.5 20.6 29.3

Sm 6.69 5.64 6.17 5.21 5.53 6.06 6.57 6.88 4.36 6.56

Eu 1.57 1.36 1.34 1.12 1.21 1.34 1.49 1.51 1.12 1.42

Gd 6.45 5.34 5.63 4.76 5.47 5.57 6.13 6.13 3.98 5.55

Tb 1.06 0.89 0.93 0.83 0.91 0.93 1.07 1.04 0.55 0.90

Dy 6.68 5.36 5.94 5.14 5.56 5.83 6.73 6.37 3.20 5.14

Ho 1.24 1.04 1.12 0.98 1.11 1.08 1.26 1.21 0.71 1.18

Er 3.55 3.08 3.26 2.79 3.12 3.22 3.55 3.45 1.95 3.22

Tm 0.54 0.47 0.48 0.41 0.47 0.48 0.52 0.51 0.30 0.49

Yb 3.62 3.02 3.10 2.72 2.99 3.13 3.33 3.41 2.07 3.13

Lu 0.56 0.47 0.50 0.45 0.47 0.50 0.52 0.53 0.32 0.49

Hf 5.26 4.69 4.62 4.21 4.45 4.82 4.92 4.92 2.97 4.83

Ta 0.73 0.59 0.61 0.57 0.64 0.69 0.68 0.59 0.48 0.65

Th 10.3 8.66 8.52 7.72 8.72 8.97 10.0 9.57 6.57 9.52

U 2.82 2.51 2.25 2.14 2.34 2.48 2.68 2.72 1.63 2.52

87Rb/86Sr 1.615 1.921 1.588

147Sm/144Nd 0.130 0.135 0.132

87Sr/86Sr 0.716449 0.717158 0.716375

2σ 15 10 17

143Nd/144Nd 0.512406 0.512387 0.512420

2σ 10 8 6

(87Sr/86Sr)i 0.70847 0.71013 0.70853

εNd -1.6 -2.0 -1.4

J o u r n a l o f E a r t h S c i e n c e , 2 0 1 7 o n l i n e I S S N 1 6 7 4 - 4 8 7 X Printed in China DOI: 10.1007/s12583-017-0936-0

Li, S. B.,He,H. Y., Qian, X., et al., 2017. Carboniferous arc setting in Central Hainan: Geochronological and geochemical evidences on the andesitic and dacitic rocks. Journal of Earth Science.doi: 10.1007/s12583-017-0936-0. http://en.earth-science.net

(to be continued)

10HN-14C* 10HN15A* 10HN15C* 11HN-21A 11HN-21D 11HN-21E 11HN-21F 11HN-21G 11HN-21H 11HN-21J 11HN-21K 11HN-21L

SiO2 64.14 56.78 63.09 63.71 64.99 64.94 64.24 63.83 65.50 64.75 60.69 64.82

TiO2 0.72 0.83 0.69 0.70 0.67 0.60 0.64 0.65 0.64 0.71 1.11 0.69

Al2O3 15.32 18.54 15.55 16.53 15.46 14.85 15.80 16.33 15.07 15.79 16.26 16.12

Fe2O3t 6.58 8.01 7.27 6.10 6.01 5.67 5.80 5.30 6.06 5.55 6.03 5.76

MgO 3.25 3.76 3.51 2.23 2.14 2.08 2.14 2.03 2.16 1.84 2.45 2.03

MnO 0.14 0.14 0.11 0.08 0.09 0.11 0.13 0.09 0.10 0.08 0.15 0.09

CaO 4.47 4.16 3.36 2.98 3.57 3.80 4.44 3.55 3.77 3.66 3.60 3.12

K2O 2.54 3.22 3.02 3.34 2.62 2.76 2.41 3.60 2.52 2.08 3.43 3.12

Na2O 0.91 2.31 1.38 1.37 1.52 1.16 1.41 2.15 1.40 2.54 2.38 1.45

P2O5 0.20 0.21 0.19 0.11 0.10 0.11 0.11 0.11 0.10 0.12 0.13 0.10

LOI 1.28 1.59 1.40 2.39 2.35 3.57 2.43 1.95 2.23 2.54 3.45 2.23

Total 99.56 99.56 99.57 99.54 99.52 99.63 99.55 99.59 99.53 99.65 99.69 99.53

mg-number 54 52 53 46 45 46 46 47 45 43 49 45

Sc 21.1 22.6 27.1 14.3 14.8 14.2 15.0 14.7 13.5 16.8 13.9 16.9

V 123 120 148 118 102 108 116 120 110 125 105 126

Cr 50.0 48.9 59.2 46.0 48.1 42.8 46.1 50.9 47.7 46.3 44.9 58.5

Co 16.1 16.6 20.4 10.9 10.1 11.0 10.9 10.7 10.8 9.83 10.4 13.8

Ni 22.7 24.2 30.4 30.8 28.9 27.5 29.6 29.6 29.3 25.9 27.3 74.9

Rb 99.4 112 117 135 122 141 131 142 125 157 125 127

Sr 170 189 278 239 269 223 290 289 250 313 292 268

Y 26.0 26.2 31.3 24.6 26.4 27.7 30.1 27.2 27.2 26.0 27.6 27.6

Zr 133 131 164 141 139 130 141 145 145 161 146 146

Nb 8.33 8.52 10.5 9.50 9.19 9.43 8.92 9.39 9.27 9.42 8.80 8.94

Cs 9.54 10.3 11.8 9.19 7.97 9.54 7.51 11.1 8.24 17.9 11.2 11.6

Ba 258 310 348 417 325 331 281 575 281 364 477 526

La 25.1 23.2 29.2 28.9 30.3 28.6 29.4 29.0 30.8 28.0 30.1 28.8

Ce 49.3 44.5 56.1 54.5 59.5 55.0 53.4 57.6 58.0 56.2 56.6 52.8

Pr 5.78 5.35 6.41 6.62 7.13 6.83 6.47 6.89 7.20 6.68 6.90 6.21

Nd 22.4 20.6 25.3 26.8 28.0 27.2 25.4 27.4 28.2 27.5 27.7 24.7

Sm 5.36 5.08 5.14 5.42 5.46 5.65 5.50 5.52 5.52 5.21 5.45 5.09

Eu 1.32 1.24 1.53 1.07 1.11 1.05 1.05 1.11 1.10 1.10 1.24 1.13

Gd 4.81 4.73 5.24 5.07 4.98 4.97 4.92 4.91 5.02 4.71 5.18 4.83

Tb 0.83 0.76 0.97 0.84 0.85 0.85 0.82 0.83 0.83 0.82 0.87 0.81

Dy 4.67 4.44 5.60 5.39 5.37 5.47 5.45 5.40 5.21 5.06 5.34 4.90

Ho 1.07 1.19 1.24 1.01 1.02 1.05 1.04 1.05 1.01 0.97 1.01 0.89

Er 2.86 3.03 3.44 2.87 3.02 3.16 3.19 2.99 3.02 2.93 2.92 2.66

Tm 0.44 0.52 0.50 0.43 0.44 0.49 0.52 0.43 0.48 0.46 0.43 0.38

Yb 2.57 2.86 3.41 2.75 2.83 3.33 3.45 2.82 3.17 3.04 2.80 2.56

Lu 0.42 0.50 0.54 0.43 0.42 0.54 0.52 0.42 0.48 0.48 0.43 0.42

Hf 4.17 4.02 4.20 4.33 4.05 4.34 4.00 4.10 4.26 4.58 4.23 4.24

Ta 0.57 0.54 0.72 0.70 0.68 0.72 0.66 0.73 0.73 0.73 0.68 0.66

Th 7.28 6.66 8.75 10.5 10.5 10.3 9.71 10.4 10.20 9.58 9.83 9.63

U 1.91 1.94 2.32 2.83 2.77 2.73 2.58 2.90 2.57 2.45 2.85 2.69

87Rb/86Sr 1.635 1.313 1.448 1.452

147Sm/144Nd 0.122 0.118 0.118 0.115

87Sr/86Sr 0.715693 0.714667 0.714825 0.715108

2σ 14 17 12 12

143Nd/144Nd 0.512227 0.512278 0.512244 0.512279

2σ 9 11 10 5

(87Sr/86Sr)i 0.70761 0.70818 0.70767 0.70719

εNd -4.7 -3.5 -4.2 -3.4

* The data ofthe Chenxing andesitic rocks are from Chen et al. (2013).Fe2O3t represents total Fe-oxides; mg-number=molar Mg×100/(Mg+Fe); LOI. losson

ignition.


Figure 3. (a) TAS (after Le Bas et al., 1986) and Zr/TiO2vsNb/Y (after Winchester and Floyd, 1977) classification diagrams for the andesitic and daciticsam-

ples from the Bangxi-Chenxing zone.

Figure 4. Plots of SiO2vsMgO (a), Fe2O3t (b), Al2O3 (c), CaO (d), TiO2 (e) and P2O5 (f) for the andesitic and dacitic samples from the Bangxi-Chenxing zone.


Figure 5. (a) Chondrite-normalized REE pattern and (b) primitive mantle-normalized trace element spidergram for the andesitic and daciticsamples from the

Bangxi-Chenxing zone. Data of Lancangjiang Early Triassic arc volcanic rocks are from Peng et al. (2008). Also shown the patterns of E-MORB, OIB and

normalized values for chondrite and primitive mantle are from Sun and McDonough (1989).

Figure 6. Plot of initial 87Sr/86Sr (i) vsεNd (t) for the andesitic and dacitic

samples from the Bangxi-Chenxing zone. 4 DISCUSSION 4.1Petrogenesis

The Chenxing and Bangxi samples display slightly high loss of ignition (LOI) contents (1.24–3.57 wt.%). Together with the Sr isotopic deviation from the mantle–evolved array in Fig. 7, these characteristics suggest that these samples may have been undergone some degree of alteration (e.g., Rolland et al., 2002). However, our samples display insignificant correlations between the LOI values and HFSEs or LILEs (e.g., Rb, Sr, Zr and Nb not shown), indicating that they were immobile during the alteration and can be used to discuss the petrogenesis.

The Chenxing and Bangxi samples have relatively high si-lica contents (maximum value is 65.50 wt.%) and low Ni (20.9–74.9 ppm) and Cr (36.2–60.7 ppm) contents, along with the xenocrysts, suggest that the crustal contamination might be significant. However, the crustal contamination could be ex-cluded during the magma ascending as follow: (1) constant Nb/La ratios (0.29–0.37) with increasing SiO2 contents, lower than those of continental crust (~0.7) (Fig. 7a) and (2) the con-stant εNd (t) values of our samples with increasing SiO2 con-tents (Fig. 7b; e.g., Sun & McDonough, 1989; Hoffman and

Ranalli, 1988). Such signatures, along with lower Ce/Pb (1.93–4.99) and Nb/U (3.08–4.70) ratios in comparison with those of average continental crust, indicate that the crustal con-tamination might be insignificant during magma evolution (Taylor and McLennan, 1985). The correlations of Yb with Tb/Yb and La/Yb ratios in Fig. 7c–d indicate that the fractional crystallization and source heterogeneity could be involved dur-ing magma evolution. Hence, the incompatible elements ratios and isotopic compositions are more likely inherited from the magma source.

The mg-numbers for the Chenxing samples range from 51 to 53, Cr contents from 36.2 ppm to 66.6ppm and Ni contents from 20.9 ppm to 34.5 ppm, respectively, suggesting that their magma has been experienced certain degrees of fractional crystallization of clinopyroxene. The Bangxi samples have relatively lower MgO contents (1.84–2.45 wt. %) and higher Ni contents (25.94–74.88 ppm) than those of Chenxing samples, indicate the certain degrees of fractional crystallization. The weak Eu negative anomalies and Sr positive anomalies of all samples argue against strong plagioclase fractionation during the magma process (Fig. 5a–b). The negative correlations be-tween SiO2 and TiO2 and Fe2O3t (Fig. 4b and e) are related to the fractionation crystallization of Ti–Fe oxides. Both of ande-sitic and dacitic samples from the Bangxi and Chenxing areas might be explained as the generation of contiguous fractional crystallization and shared a common magma source according to the similar trends in Harker, SiO2–Nb/La, La–La/Yb and Yb–La/Yb diagrams (Figs. 4 and 7).

Three models have been proposed for the formation of the andesitic samples: (1) hypomigmatization of lower crust; (2) the mixing of basic magma and acid magma; and (3) the partial melting of the mantle wedge, metasomatized by subduc-tion-related melts/fluids (Tatumi et al., 2008; Martin et al., 2007; Dungan and Davidson., 2004; Parman and Grove., 2004). The slightly high mg-number of the Chenxing and Bangxi samples range from 44 to 53, distinct to the product from partial melting of the granulite or eclogitecrust, which commonly has low mg-number (＜40; Rapp et al., 1999, 1991). Together with theenrichment in LILEs and LREEs and relatively low Nb/La


Figure 7. Plots of (a) SiO2vsNb/La, (b) SiO2vsεNd (t), (c) Ybvs Tb/Yb and (d) Ybvs La/Yb for the andesitic and dacitic samples from the Bangxi-Chenxing

zone. ratios (0.29–0.34), the origin of these samples is less likely to be the lower crust of the SCB (data from the amphibolite of the ArcheanKongling Group; Gao et al., 1999; Rudnick and Foun-tain, 1995; Taylor and McLennan, 1985). Besides, in compari-son with variably isotopic and geochemical signatures of mix-ing magma, the homologous εNd (t) values for our samples suggest that the mixing model of basic magma and acid magma is also not likely in the petrogenesis. As mentioned above, our samples from the Bangxi-Chenxing zone have high SiO2 (55.34–65.50 wt.%), Al2O3 (14.26–19.41 wt.%) and low TiO2 (0.82–1.22 wt.%) contents, as well as enrichment in LILEs and LREEs and depletion in Nb, Ta and Ti. These signatures to-gether with the high Sc (13.5–22.8 ppm) and V (102–160 ppm) contents and Nb/La, Nb/U, Nd/Pb, Ce/Pb ratios and negative εNd (t) values, suggest that our samples were probably inherited an enriched mantle source modified by the fluids/melts from subducted slab or sediments (e.g., Turner et al., 1997; Stolz et al., 1990).

The Th/Yb ratios for all samples range from 2.23 to 3.82 and Ba contents from 235 ppm to 257 ppm. In Fig. 8a, they plot in the Kitakami andesite range, which has been interpreted to form in the subductedmetasomatism source. These samples have high Th/Zr and Ba/Y ratios along with the low Nb/Zr and Nb/Y ratios in Fig. 8b–c, suggesting a fluid-related enrichment in the source and negligible melt-related enrichment. In addi-tion, the involvement of subducted sedimentary component into the mantle source can be recognized by the relatively low εNd (t) values of –1.39 to –4.71, high Al2O3 contents (14.26–19.41

wt.%) and relatively high Th/Yb ratios (43.62–52.97) and low-er Ba/La (2.75–3.82) ratios relative to N-MORB (e.g., Plank and Langmuir, 1998; Stolz et al., 1990; Sun and McDonough, 1989). The synthesis of these data indicates that the volcanic rocks in the Bangxi-Chenxing zone might have originated from an enriched lithospheric mantle modified by slab-derived fluids mixed with the recycled sediments. 4.2 Tectonic setting

The Early Paleozoic tectonic setting in Hainan has been poorly constrained in last decades with the controversies main-ly around the igneous rocks along the Bangxi-Chenxing zone in Central Hainan. Various tectonic assumptions have been pro-posed for these igneous rocks. Xia et al. (1991) proposed that the Late Paleozoic tectonic setting of Hainan was intraconti-nental rift setting on the basis of the Carboniferous bimodal volcanic rocks, whereas Zhang et al. (1997) considered that the volcanic rocks along the Bangxi-Chenxing zone formed in a Mesoproterozoic continental rift based on the Sm–Ndisochron age of 1165 Ma from the mafic sequence. As mentioned above, our samples display low TiO2 (0.82–1.22 wt.%), Cr (36.2–66.6 ppm), Ni (21.0–74.9 ppm) and high Al2O3 (14.26–19.41 wt.%) contents and enrichment in LILEs and depletion in HFSEs, indicating an arc affinity (Pearce et al. 1994). The high Ba/Y, Th/Zr and Nb/U ratios also indicate the potential input of the subducted component in the source. In Fig. 9a–c, these samples plot in the field of continental arcs (Tian et al., 2008; Shinjo et al., 1999; Pearce, 1983). In addition, Early Carboniferous


Figure 8. Plots of (a) Ba vsNb/Y, (b) Th/ZrvsNb/Zr and (b) Nb/Y vs Ba/Y

(after Hofmann and Jochum, 1996; Wang et al., 2004) for the andesitic and

dacitic samples from the Bangxi-Chenxing zone. (~330 Ma) MORB-like metabasites have also been identified along the Bangxi-Chenxing zone, which formed in a back-arc basin setting (He et al., 2017). These geochemical features synthetically suggest a continental arc setting for the generation of these volcanic rocks. Therefore, the arc volcanic rocks along with the MORB-like metabasites exhibit an arc-back-arc sys-tem in the Bangxi-Chenxing zone (Fig. 10), resembling those in

Figure 9. (a) Plots of (a) Sc/Ni vs La/Yb, (b) Nb/YbvsTh/Yb and (c)

YbvsTh/Ta for the andesitic and daciticsamples from the Bangxi-Chenxing

zone. the Mariana, East Scotia and Lau back-arc basins (Taylor and Martinez, 2003).

A key issue remains to whether or not the Carboniferous back-arc basin in Central Hainan geodynamically links the Paleopacific or Paleotethyan domain. Li and Li (2007) and Li et al. (2006) suggested that the westward flat-slab subduction of the Pacific Plate beneath the South China Block since the


Permian on the basis of Wuzhishan I-type granites (267–262 Ma). However, the westward subduction of the Pacific plate may not initiate until the Middle Jurassic (e.g., Zhou and Li, 2000) due to the Carboniferous–Permian sedimentary se-quences around the coastal provinces, which are characterized by carbonate platform and shallow-marine/lacustrine coal-bearing sandstone, shale and synchronous foreland basin (e.g., Shu et al., 2008; Wang et al., 2007, 2005 and references therein). By contrast, recent studies have shown that abundant Late Paleozoic to Mesozoic igneous rocks developed along the Jinshajiang-Ailaoshan-Song Ma zone. Jian et al. (2009a, b; 1998) and Wang et al. (2000) obtained zircon U–Pb ages of 383-334 Ma from the Jinshajiang-Ailaoshan suture zone. Simi-lar ages (387–313 Ma) also have been reported in the Song Ma suture zone (e.g., Zhang et al., 2014; Vượng et al., 2013). These data indicate that the Bangxi-Chenxing zone has similar mag-matic activity with the Jinshajiang-Ailaoshan-Song Ma zone (e.g., He et al., 2017a, 2016a, 2016b; Chen at al., 2013; Xu et

al., 2007; Li et al., 2006, 2002). In addition, the Devonian fish fossils and Late Permian PangeanDicynodon in the Indochina Block are same with those in the South China Block (e.g., Thanh et al., 2007; Janvier et al., 1994), additionally arguing for continental linkage rather than ocean. To the south of Bang-xi-Chenxing zone, abundant Permian–Triassic granitoids have been reported and suggested to form in the magmatic activities of Bangxi-Chenxing BAB with ages of 272–233 Ma (e.g., Chen et al., 2011, 2006; Zhang et al., 2011; Li et al., 2006). These data are similar to the Permian–Triassic igneous rocks in the Truong Son zone in the Central Vietnam (e.g., Maluskiaa et al., 2005; Lai et al., 2014) and Jinshajiang-Ailaoshan zone in SW China (e.g., Liu et al., 2015; Zi et al., 2012), indicating the closely relationship of tectonic magmatism in response to the Paleotethyan Ocean. As a result, our data along the Bang-xi-Chenaxing zone support a continental BAB linkage with the Jinshajiang-Ailaoshan-Song Ma zone between the Indochina and South China blocks.

Figure 10.Schematic cartoon showing the Early Carboniferous subduction pattern of the Bangxi-Chenxing zone. 5 CONCLUSIONS

Based on our new zircon U–Pb geochronological and whole-rock elemental and Sr–Nd isotopic data, the following scenario can be outlined.

(1) These volcanic rocks exposed within the Bang-xi-Chenxing zone in Central Hainan were generated at ~350 Ma, indicative of the Early Carboniferous origin.

(2) These volcanic rocks originated from an enriched mantle source modified by slab-related fluids and sediments in a conti-nental-arc setting.

(3) The Bangxi-Chenxing zone can westerly link with the Jinshajiang-Ailaoshan-Song Ma zone.

ACKNOWLEDGMENTS

We would like to thank Dr. Y-Z Zhang, F-F Zhang, X-Y Chen, A-M Zhang and H-C Liu for their help during fieldwork, geochronological and geochemical analyses. Financial supports are gratefully acknowledged from National Science Foundation of China (No. 41190073), National Basic Research Program of Chi-na (Nos. 2016YFC0600303 and 2014CB440901), andthe Project

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