2019 | 72 / Special Issue | 93–109 | 16 Figs. | 4 Tabs. | www.geologia-croatica.hr Journal of the Croatian Geological Survey and the Croatian Geological Society Article history: Manuscript received April 23, 2019 Revised manuscript accepted July 02, 2019 Available online December 20, 2019 Keywords: Tethyan-South China Sea, Subduction, Zircon U–Pb age, Geochemistry 1. INTRODUCTION During the Mesozoic Era, there was an ancient Sea situated in the same place as the present-day South China Sea (south of Hainan Island), which experienced northward subduction during the late Mesozoic. Hainan Island lies along the front edge of this ancient subduction zone, and thus was in a special position in the late Mesozoic framework of southeastern China (LI et al., 2000; YANG et al., 1989). Due to the close relationship with oceanic crust, attention was focused on the intense tectonic magmatism that took place during the late Mesozoic (YUN et al., 2004). There are several competing explanations for the tectonic position and formation mechanism of Hainan Island. For example, JIA et al. (2010) & WANG et al. (2012) suggested that the Tunchang intru- sion of Hainan Island is composed of adakitic rocks, and was formed by asthenospheric upwelling resulting from the recession of Pacific subduction. TANG et al. (2014) & WANG et al. (1991) believed that the late Yanshanian magmatism of Hainan Island occurred in a post-arc extensional environment. YUN et al. (2003) considered that the formation of late Mesozoic granites in Hainan Island was closely associated with large-scale litho- spheric extension–thinning, basaltic magma underplating, and enriched mantle-derived basaltic magma related to oceanic crust subduction, which contributed heat and material to the formation and evolution of the granites. From a systematic study of Creta- ceous basic dykes on Hainan Island, GE (2003) proposed that the The characteristics of granites in the Gaofeng and Baocheng areas, Hainan Province, China: Response to subduction of the Tethyan South China Sea Yuan Xiaobo1*, Fang Nianqiao2, Zhang Zhenguo4 and Dong Hailong3 1 Hebei Normal University of Science and Technology, Institute of Marine Science, Qinhuangdao, 066004 China; (*corresponding author: yuanxiaobo2011@163.com) 2 China University of Geosciences (Beiing), School of Ocean Sciences, Beijing, 100083 China 3 Nonferrous geological prospecting bureau of Inner Mongolia, Hohhot, 016043 China 4 Liaoning Technical University, Mining Institute, Fuxin, 123000 China doi: 10.4154/gc.2019.19 Abstract During the early Mesozoic Era there was intense magmatic activity near Hainan Island, South China. As a result, the granites of Hainan Island provide information on, and are suitable mate- rial to potentially improve understanding of the Cretaceous tectonic environment of the northern margin of the South China Sea. The Gaofeng and Baocheng intrusions are composed mainly of medium- to fine-grained biotite adamellite (Baocheng) and granodiorite (Gaofeng). The two in- trusions yielded U–Pb LA-ICP-MS zircon ages of 107.7 ± 6.1 Ma (Gaofeng) and 105.8 ± 2.4 Ma (Baocheng). Regarding the major elements, the Gaofeng and Baocheng intrusions had medium Si and alkali contents and high Ca, Mg, and Al contents, with an aluminum saturation index of 0.95–1.03 and 1.05–1.30. The trace element and rare earth element (REE) characteristics showed that the two intrusions have intense heavy REE/light REE (HREE/LREE) fractionation, LREE enrichment, HREE depletion, and weak negative Eu anomalies. The intrusions were en- riched in high field-strength elements and depleted in large ion lithophile elements. These geo- chemical characteristics indicate that the Hainan Province was in a tectonic subduction environ- ment in the late Yanshanian period. Multiple geochemical characteristics demonstrate that the granites in the Hainan Province were formed by a different mechanism and in a different setting from those in Fujian and Zhejiang. The late Mesozoic granites of Fujian and Zhejiang were formed by the Western Pacific subduction. However, Hainan Island was under an arc environment formed by the northward subduction of the Tethyan-South China Sea during the Cretaceous leading to emplacement of the Gaofeng and Baocheng intrusions. dykes were formed in an intraplate extensional environment, which, together with Cretaceous basic dykes in the coastal region of northern Guangdong and Fujian, indicated that southeastern China experienced an extensional tectonic environment during the Cretaceous period. The current hypotheses for the formation of late Mesozoic igneous rocks in Hainan Island are extensional thinning, post-arc extension, and intraplate anorogenic movement (TANG, 2014; JIA et al., 2010; YUN et al., 2004; LI et al., 2000; YANG et al., 1989). However, a previous study observed that Cre- taceous andesites (QIANG, 2016) in the Hainan Province and detrital zircons from the Lumuwan Formation in the Ledong ba- sin showed signatures of a continental-margin arc (TANG, 2014). We collected samples from the Gaofeng and Baocheng intrusions, and performed U–Pb LA-ICP-MS zircon dating and total-rock geochemical analysis to obtain a clear understanding of the geo- tectonic setting represented by the late Mesozoic rocks on Hainan Island. 2. GEOLOGIC SETTING AND SAMPLING LOCATION This study focused on the Gaofeng and Baocheng intrusions (Table 1), which are represented by granitic rocks collected from the two areas. The Gaofeng intrusion lies at the junction of the southern margin of the Wuzhishan depression belt and the north- ern margin of the South China Sea Platform in the first-order tectonic unit (i.e., the South China Fold System). The Gaofeng complex is a ring-like intrusion emplaced northward within the G eo lo gi a C ro at ic a Geologia Croatica 72 / Special Issue94 Lower Cretaceous Lumuwan Formation. The Baocheng intru- sion occurs in Baoting County in the southeastern Hainan Provi- nce, north of the Jiusuo–Lingshui structural belt, and is also a relatively obvious ring-like complex (Fig. 1). Previous research on the Gaofeng and Baocheng granites is limited, but concluded that the Baocheng rocks are granodiorites and the Gaofeng grani- tes are monzogranites (Fig. 2).The distribution of the two rock masses generally occurs along an east-west axis, without any Figure 1. A simplified geological map of Hainan Island.1: Early Cretaceous Baoting Unit; 2: Early Cretaceous Baoyue Unit; 3: Early Cretaceous Liaociling Unit; 4: Ear- ly Cretaceous granite porphyry; 5: Early Cretaceous Liugong Unit; 6: Early Cretaceous Fushidou Unit; 7: Early Cretaceous Jiamao Unit; 8. Early Cretaceous Shuiding Unit; 9: Middle Triassic Chaopen Unit; 10: Middle Triassic Bushancun Unit; 11: Middle Triassic Jiewei Unit.; 12: Middle Permian Tongshi Unit; 13; Quaternary Basuo formation; 14: Coastal zone; 15: Deep Fault Zone; 16: Normal fault; 17: Sampling point. Table 1. The sample co-ordinates of all samples processed in the study. Area Gaofeng Sample Number YL501 YL601 YL701 YL703 Location 18°19'10.9''N， 109°19'51.7''E 18°21'15,9''N，109°19'36.0''E 18°20'19.6''N，109°19'41.0''E 18°20'19.0''N，109°19'39.2''E Area Baocheng Sample Number SHY101 SHY201 SHY302 SHY401 Location 18°32'00.9''N，109°50'21.2''E 18°31'55.8''N，109°50'17.3''E 18°31'51.3''N，109°50'19.2''E 18°31'41.8''N，109°50'26.8''E G eologia C roatica Xiaobo et al.: The characteristics of granites in the Gaofeng and Baocheng areas, Hainan Province, China ... 95 primary banded structure. The central facies of the rock mass is dominated by monzogranite, which has a fine-medium porphy- roid texture. A small amount of granodiorite and granite can be observed; the marginal facies of the rock mass is dominated by granodiorite and quartz diorite, showing a medium-grained tex- ture. From the centre to the margin, the lithological variation of the rock mass changes from monzogranite to granodiorite , quartz diorite, and the texture alters from fine-medium porphy- roid to medium-grained fabric. There are intrusions in the Bao- cheng rock mass, composed of granite porphyry or granodiorite porphyry, and the contact zone between the rock mass and the surrounding rocks gradually changes to quartz porphyry or fel- site porphyry. The dyke rocks are granite, aplite, lamprophyre and quartz veins. Lithologically, the Cretaceous period mainly consists of sandstone, sandy conglomeratic, and mudstone. Lower Tertiary System formations from bottom to top include the Changliu, Liushagang, and Weizhou formations. Lacustrine deposits make up the majority of these formations. Neogene formations include the Xiayang Formation, Jiaowei Formation, Dengloujiao Forma- tion, and the Wanglougang Formation. the majority of these sedi- ments include neritic facies where the dominant lithology is coarse-grained sandstone and mudstone rich in glauconite, and foraminifera. Quaternary lithologies mainly consists of clay, tuff, pyroclastic rocks, and basalt. Figure 2. A Q-A-P diagram (after MANIAR et al., 1989). Figure 3. Photomicrographs of Gaofeng granite textures: (3a)Gaofeng (YL501) plane polarized light, and (3b)crossed polars (Granitic texture, Quartz shows xeno- morphic granular texture, Plagioclase shows perthitic texture); (3c)Gaofeng (YL501) plane polarized light, and (3d)crossed polars (plagioclase show Carlsbad-albite compound twin). G eo lo gi a C ro at ic a Geologia Croatica 72 / Special Issue96 3. PETROGRAPHY The granodiorite collected from the Gaofeng intrusion in the southern Hainan Province has a fine- to medium-grained granitic texture. In describing the main rock-forming minerals: potash feldspar is of reddish-brown colour and xenomorphic-platy in form, with crosshatched twins and ribbon texture characteristics; plagioclase is euhedral to subhedral-platy, with developed poly- synthetic twins and sericitization; quartz is xenomorphic-granular in form with undulating extinction. Biotite, which appears dark green to yellow, is euhedral to subhedral-flaky, with one perfect cleavage and obvious pleochroism present. Accessory minerals predominantly include zircon and apatite. The main rock-forming minerals are quartz (20-30%), potash feldspar (17-20%), plagio- clase (30-40%), biotite (5-7%), and hornblende (8-10%) (Fig. 3). The samples from the Baocheng intrusion are biotite adamel- lite. The rocks are light-grey in colour, massive with a medium- fine porphyritic-like texture. The main phenocrysts are potash feldspar with some quartz. Of the main rock-forming minerals, plagioclase is euhedral to subhedral-platy, with a ring-like tex- ture. Most plagioclase grains occur as polysynthetic twins, and some are associated with strong sericitization. Potash feldspar is brownish-gray and xenomorphic-platy, with a typical ribbon tex- ture. Quartz is anhedral granular, with undulating extinction. Hornblende is mostly idiomorphic to hypidiomorphic-granular, with moderate relief, two cleavage directions and pleochroism. It is dark green-light yellow in colour, with developed biotite reac- tion borders. Accessory minerals include apatite, zircon, and other opaque minerals. The mineral composition of the Baocheng intrusions is quartz (25–30%), potash feldspar (8–40%), plagio- clase (5–25%), and biotite (5–7%), with hornblende observed lo- cally (approximately 3%) (Fig. 4). 4. ANALYTICAL METHODS The element analysis was completed at the laboratory of the He- bei Institute of Regional Geology & Mineral Survey. Major ele- ments were measured with a Philips PW2404 X Ray Fluores- cence Spectrometer (XRF), using the alkali-fusion cast-bead method. The National Standard Reference Material GBW07103 was used for quality monitoring during the measurement process. The nitric acid + hydrofluoric acid + perchloric acid open-vessel decomposition method was combined with nitric acid + hydro- fluoric acid sealed-vessel decomposition to ensure complete dis- solution of the samples. The equipment used for this assay was an ELEMENT I-type plasma mass spectrometer produced by the German company Finnigan-MAT, as well as the National Stand- ard Reference Materials GBW07106 and GBW07312 for quality monitoring. The method is LA-ICP-MS (Inductively Coupled Plasma Mass Spectrometry). Representative samples YL701 and Figure 4. Photomicrographs of Baocheng granite textures: (4a)Baocheng (SHY401) plane polarized light, and (4b)crossed polars (biotite surround by plagioclase phenocryst); (4c)Baocheng (SHY401) plane polarized light, and (4d)crossed polars (porphyritic-like texture). G eologia C roatica Xiaobo et al.: The characteristics of granites in the Gaofeng and Baocheng areas, Hainan Province, China ... 97 SHY401 were selected for LA-ICP-MS zircon U-Pb dating, and the dating samples corresponded to the samples for main and trace element analysis. The whole rock fresh sample was crushed to 80-120 mesh, then the zircon content was enriched by gravity and magnetic separation methods. Zircon grains were selected under binocular microscope, discharged onto the double-sided tape, placed in the mould and fixed with epoxy resin. After the zircon grains were consolidated, they were polished to expose the surface. Zircon separation was performed at the Lab Center of the Hebei Institute of Regional Geology & Mineral Survey. A laser ablation-inductively coupled plasma mass spectrometry (LA- ICP-MS) device was used for in situ zircon U–Pb dating and trace element measuring at the State Key Laboratory of Continental Dynamics, Northwest University. A 193 nm ArF excimer laser with a spot size of 30 μm was connected to an Elan61(X) DRC- type ICP-MS and used as the carrier gas for the ablation material. The Zircon Standard 91500 was used as the external standard to calibrate the isotopic fractionation during zircon U–Pb isotopic dating. Using the USGS Reference Glass NIST 610 as the exter- nal standard and Si as the internal standard, quantitative calcula- tions were performed to assay the zircon trace-element content. The 91500 + NIST 610 standard zircon was measured once for every six sample spot measurements. Specific details of the labo- ratory processes are provided in YUAN et al. (2003). U–Pb age concordia plots of zircon samples and an age-weighted average calculation were both determined with Isoplot (Ver. 3) (LUD- WIG, 2003). 5. RESULTS 5.1. ZIRCON U–Pb AGES Eight concordant ages were obtained from the Gaofeng intrusion (YL701), and nine from the Baocheng intrusion (SHY401). The analytical results are listed in Table 2. Most zircons from the two intrusions were idiomorphic to hypidiomorphic-columnar, with clean and smooth crystal surfaces. In general the crystals had a length/width ratio of 2:1, but some individual crystals were up to 3:1. Cathodoluminescence images demonstrated that the zircons from both intrusions displayed clear concentric zoning, with Th/U ratios of 0.36–0.93 (Gaofeng) and 0.53–0.90 (Baocheng). As all ratio values were larger than 0.1, these zircons were deter- mined to be magmatic (BELOUSOVA et al., 2002). The Gaofeng intrusion had a weighted average age of (107.7 ± 6.1) Ma, and the Baocheng intrusion an age of (105.8 ± 2.4) Ma, which may rep- resent the formation ages of the two intrusions (Fig. 5-6). 5.2. RESULTS 5.2.1. MAJOR ELEMENTS Table 3. lists the chemical compositions of the representative samples from the Gaofeng and Baocheng intrusions. Granitic rocks from the Gaofeng intrusion had a SiO2 content of 65.90– 72.42%, total alkali content (K2O + Na2O) of 7.29–8.13%, and K2O/Na2O ratios of 1.27–1.6. On the total alkali–SiO2 diagram for intrusive rocks (MIDDLEMOST, 1994; Fig. 7) all samples fell within the granite field, with the exception of sample YL501 that fell outside the granodiorite domain. On the SiO2–K2O diagram, all samples were within the high-K calc-alkaline series domain. On the A/CNK–A/NK diagram, most of the samples were within the metaluminous rock domain (Fig. 8a). The aluminum satura- tion index was 0.95–1.03, and the Rittmann Serial Index(σ) ranged from 2.26 to 2.32. The magma differentiation index (DI) Ta bl e 2. L A -IC P- M S re su lts o f t he z irc on s f ro m th e G ao fe ng a nd B ao ch en g ba th ol ith . A na ly se d Sp ot s Co nc en tr at io ns (μ g/ g) At om ic ra tio s A pp ar en t a ge s（ M a) 23 2 Th 23 8 U 20 6 Pb Th /U 20 7 Pb /20 6 Pb 1σ 20 7 Pb /23 5 U 1σ 20 6 Pb /23 8 U 1σ 20 7 Pb /23 5 U 1σ 20 6 Pb /23 8 U 1σ YL 70 1- 2 50 .9 5 86 .4 5 6. 03 0. 59 0. 05 10 0. 00 84 0. 11 71 0. 01 87 0. 01 66 0. 00 05 11 2. 4 17 .0 10 6. 4 3. 37 YL 70 1- 4 10 72 .1 0 13 93 .7 0 96 .1 2 0. 77 0. 05 58 0. 00 26 0. 12 73 0. 00 48 0. 01 65 0. 00 03 12 1. 7 4. 3 10 5. 7 1. 72 YL 70 1- 6 10 7. 78 15 3. 27 10 .2 4 0. 70 0. 04 56 0. 00 49 0. 10 09 0. 01 04 0. 01 60 0. 00 04 97 .6 9. 6 10 2. 6 2. 32 YL 70 1- 7 11 7. 51 12 9. 00 8. 90 0. 91 0. 05 08 0. 00 57 0. 11 60 0. 01 25 0. 01 66 0. 00 04 11 1. 5 11 .4 10 6. 0 2. 59 YL 70 1- 8 44 6. 00 61 4. 25 39 .4 8 0. 73 0. 04 59 0. 00 29 0. 09 79 0. 00 56 0. 01 55 0. 00 03 94 .9 5. 2 98 .9 1. 79 YL 70 1- 9 17 4. 51 29 8. 16 20 .5 4 0. 59 0. 04 93 0. 00 35 0. 11 27 0. 00 73 0. 01 66 0. 00 03 10 8. 4 6. 6 10 6. 1 2. 01 YL 70 1- 10 19 5. 72 21 1. 17 15 .6 7 0. 93 0. 05 18 0. 00 47 0. 12 78 0. 01 09 0. 01 79 0. 00 04 12 2. 1 9. 8 11 4. 4 2. 53 YL 70 1- 13 18 5. 97 52 0. 50 40 .4 0 0. 36 0. 05 09 0. 00 23 0. 13 17 0. 00 48 0. 01 88 0. 00 03 12 5. 6 4. 3 11 9. 9 1. 91 YL 70 1- 15 27 0. 54 33 3. 97 23 .3 3 0. 81 0. 04 75 0. 00 32 0. 11 09 0. 00 67 0. 01 69 0. 00 03 10 6. 8 6. 2 10 8. 2 2. 00 SH Y4 01 -3 25 7. 50 39 7. 83 27 .5 7 0. 65 0. 04 73 0. 00 25 0. 10 94 0. 00 50 0. 01 68 0. 00 03 10 5. 4 4. 6 10 7. 3 1. 68 SH Y4 01 -4 25 0. 51 39 7. 51 27 .1 4 0. 63 0. 04 63 0. 00 26 0. 10 57 0. 00 52 0. 01 65 0. 00 03 10 2. 0 4. 8 10 5. 7 1. 68 SH Y4 01 -6 24 6. 88 38 0. 59 26 .4 0 0. 65 0. 04 87 0. 00 29 0. 11 27 0. 00 59 0. 01 68 0. 00 03 10 8. 4 5. 4 10 7. 2 1. 80 SH Y4 01 -9 18 8. 96 30 2. 21 19 .8 5 0. 63 0. 05 01 0. 00 36 0. 10 95 0. 00 72 0. 01 59 0. 00 03 10 5. 5 6. 6 10 1. 4 1. 90 SH Y4 01 -1 0 23 0. 68 43 2. 05 30 .5 2 0. 53 0. 04 63 0. 00 26 0. 10 89 0. 00 54 0. 01 70 0. 00 03 10 4. 9 4. 9 10 8. 9 1. 80 SH Y4 01 -1 1 16 7. 08 28 8. 97 19 .8 8 0. 58 0. 04 50 0. 00 27 0. 10 29 0. 00 54 0. 01 66 0. 00 03 99 .4 5. 0 10 6. 1 1. 76 SH Y4 01 -1 5 10 4. 77 14 4. 68 10 .4 2 0. 72 0. 04 63 0. 00 39 0. 11 05 0. 00 87 0. 01 73 0. 00 03 10 6. 4 7. 9 11 0. 6 2. 08 SH Y4 01 -2 1 11 5. 88 18 7. 81 12 .4 0 0. 62 0. 05 32 0. 00 37 0. 11 61 0. 00 74 0. 01 58 0. 00 03 11 1. 6 6. 7 10 1. 2 1. 87 SH Y4 01 -2 2 13 2. 51 14 7. 57 9. 96 0. 90 0. 04 93 0. 00 41 0. 10 99 0. 00 86 0. 01 62 0. 00 03 10 5. 8 7. 9 10 3. 4 2. 01 G eo lo gi a C ro at ic a Geologia Croatica 72 / Special Issue98 value is between 73-86, the solidification index (SI) value is 4-12, and the Harker diagram (Fig. 6) shows that SiO2 is significantly negatively correlated with FeO, MgO, CaO, Al2O3, P2O5 and TiO2 rocks may undergo crystallization differentiation evolution. The Baocheng granites had a SiO2 content range of 69.37– 72.42%, total alkali content (K2O + Na2O) of 6.8–7.54%, and K2O/Na2O ratios of 1.03–1.34. On the total alkali–SiO2 diagram for intrusive rocks (MIDDLEMOST, 1994; Fig. 7), all samples fell within the granite field. All samples were plotted within the high-K calc-alkaline series domain on the SiO2–K2O diagram (Fig. 8a). The A/CNK–A/NK diagram shows that the majority of the samples fell within the weakly peraluminous rock domain (Fig. 8b). The aluminum saturation index was 1.05–1.30%, and the Rittmann Index was σ = 1.75–1.95. 5.2.2. TRACE ELEMENTS Total rare earth element (∑REE) contents were 204.45–236.48 μg/g in the Gaofeng intrusion, and lower (94.35–192.30 μg/g) in the Baocheng intrusion. The (La/Yb)N values of the granitic rocks from the two intrusions were 10.32–15.89 and 17.56–31.13, re- spectively. These values indicate a high degree of heavy REE/ light REE (HREE/LREE) fractionation and LREE enrichment. The Gaofeng intrusion had δEu values of 0.52–0.66 and a mod- erately negative Eu anomaly; the Baocheng granitic rocks had δEu(Eu/Eu*= N N NEu / Sm / Gd ) values of 0.77–0.88, and show a weak negative Eu anomaly. The REE partition pattern shows that the Gaofeng and Baocheng intrusions have basically consis- tent REE partition patterns of right-deviating curves (Fig. 10a). The incompatible-elements spider diagram normalized on a primitive mantle (Fig. 10b) shows that both the Gaofeng and Ba- ocheng intrusions were enriched in large ion lithophile elements (LILE), but depleted in high field-strength elements (HFSE). En- richment of large ion lithophile elements (LILE) such as Rb, Ba, Sr and K, and loss of high field strength elements such as Nb, Ta, P and Ti (Fig. 7b), Rb/Sr value 0.32–0.80, K/Rb value 180–250, is similar to the typical characteristics of granites related to sub- Figure 5. Cathodoluminescent images and spot analysis points of zircon crystals from the Hainan granite (a) Oscillatory zircon from the Gaofeng granite (b) Oscil- latory zircon from the Baocheng granite. Figure 6. Results of in situ zircon 206Pb/238U age dates (a) Gaofeng granite (b) Baocheng granite. G eologia C roatica Xiaobo et al.: The characteristics of granites in the Gaofeng and Baocheng areas, Hainan Province, China ... 99 duction. It also indicates that there may be fractionation crystal- lization of apatite, Ti-rich minerals, rutile and so on during magma evolution. On the mid-oceanic ridge standardized dia- gram, the Gaofeng and Baocheng intrusions were relatively sim- ilar to Chilean granites (PEARCE et al., 1984), which is typical of an active continental-margin environment (Fig. 10c). The Sr content of the Gaofeng rock mass is 191–356 ppm, averaging 277.25 ppm. The Yb content is 2.35–2.93 ppm, (average 2.57 ppm) and the Y content is 23.2–27.9 ppm (average 24.68 ppm); the Sr content of Baocheng rock mass is relatively higher at 327- 431 ppm with an average of 396.75 ppm, and the Yb content is relatively lower at 0.75–1.75 ppm, (average 1.06 ppm). The Y con- tent is relatively lower at 5.6–17.5 ppm, (average 9.5 ppm). Peak Sr/Y value ranges from 8.23–15.15, average 11.3, Sr/Yb value 23.2–27.9, average 24.68; Baocheng Sr/Y value 23.54–76.96, av- erage 50.05, Sr/Yb value 235.43–552.56, average 414.68. The overall characteristics show higher Sr and lower Yb, Y content and higher Sr/Yb, Sr/Y ratios. The characteristics of high SiO2, high Al2O3, Mg# value is 41-44, high Sr, low Y and Yb, high Sr/Y and Sr/Yb, and weak Eu negative abnormity are similar to those of adakites representing the source of the subduction slab (STERN & KILIAN, 1996; WANG et al., 2006; SHEPPARD et al., 2001), which is also consistent with the characteristics of ac- tive continental margins represented by rare earth and trace ele- ments. Figure 7. SiO2 versus K2O+Na2O diagram for intrusive rocks (MIDDLEMOST, 1994; IRVINE & BARAGAR, 1971). Figure 9. Harker diagram of the Gaofeng and Baocehng granites. Figure 8. The classification of the Gaofeng and Baocehng granites: (a) SiO2 versus K2O diagram (after PECCERILLO & TAYLOR, 1976); (b) A/CNK versus A/NK diagram (after MANIAR & PICCOLI, 1989). G eo lo gi a C ro at ic a Geologia Croatica 72 / Special Issue100 6. DISCUSSION 6.1. ROCK TYPE AND GENESIS The I-, S-, M-, and A-type classification scheme (PITCHER, 1983) has been generally accepted as a classification scheme for granites. M-type granites that formed during mantle magma evo- lution are very rare, and represent an oceanic island-arc tectonic environment. Considering the regional tectonic setting of Hainan Island during the Cretaceous, M-type granites are not represented in the granites studied here. Hence, the granites of the southern Hainan Province are mainly represented by I-, S-, and A-types. Fig. 11a shows that most of the samples are undifferentiated I-, S-, and A-types. I- and S-type granites can be discriminated us- ing P2O5 and P2O5–SiO2 diagrams (Fig. 11b). The P2O5 content decreases with increasing SiO2 content, resulting in a negative correlation; this relationship is consistent with the evolution of I- type granites, and is markedly different from S-type granites. The major element characteristics of the granites from this study indicate that these rocks are metaluminous to weakly per- aluminous, with obvious HREE/LREE fractionalization, LREE enrichment, and HREE depletion. The trace element characteri- stics included LILE enrichment and a depletion of Ta, Nb, and Ti and other HFSE, suggesting that the granites had signatures of island-arc granites. In addition, laboratory petrological research implied that partial melting of intermediate-basic rocks in the crust formed metaluminous granitoids with a more basic chemical composition (WOLF et al., 1994; BEARD et al., 1991; JOHANNES et al., 1996; SISSON et al., 2005). The source rocks of these gran- itoids may have been derived from partial melting of island-arc volcanic rocks, or comagma of island-arc volcanic rocks. 6.2. PETROGENESIS AND SOURCE CHARACTERISTICS It is a widely accepted fact in the literature that I-type granite is a product of crust-mantle mixed source magmatism (BERGANTZ, 1989; PETFORD & CRUDEN, 2000; ZHOU & LI, 2000; ANNEN & SPARKS, 2002). The Gaofeng and Baocheng granites are char- acterized by their high Sr, low Yb and Y, high Sr/Yb and (La/Yb) n ranging from 15-31 ppm which is very simi lar to adakites (WANG et al., 2012; JIA et al., 2010). Mantle source characteristic identification charts are shown in Fig. 12a-c. It can be seen in Fig. 12a-c, that the SiO2-Mg# variable diagram, SiO2-MgO variable diagram, and Ba/Th-Nb/Zr variable diagram show that the source area is related to plate subduction. Identification of hornblende, the hydrous mineral in the sample, confirms that the studied rocks originate from subducted plates. There are two possible models for genesis of I-type granites from the mantle (QIU et al., 2008). The first model includes mix- ing between the mantle derived magma and felsic magma from the crust. The second model is where the mantle-derived magma first intrudes into the crust to form the primary crust. Then, this mixed crustal rock which consists of both primary crust and the ancient basement crust is partially melted under the influence of later thermal events. The Nb/La ratios of the Gaofeng and Baocheng granites described here are close to the crust except for the samples which occur in the plate melting zone as presented in Fig.12a-b. The rest of the samples are distributed near the com- ponent lines affected by the AFC indicating that these granites have not originated directly from melting of a mantle-derived subduction plate. This is more consistent with the second model as explained above. These findings also confirm similar reports Figure 10. Normalized diagrams of the Gaofeng and Baocehng granites: (a) REE patterns; (b) incompatible element spidergrams; (c) Ocean Ridge Granite (ORG) granite normalized patterns (Chondrite REE values and primitive mantle-normalized values from SUN & MCDONOUGH (1989); KHOSHNOODI et al. (2017) ; ORG and Chile granite values from PEARCE et al. (1984). Figure 11. Sample classification using diagrams of (a) (Zr+Nb+Ce+Y) vs. (K2O+Na2O)/CaO (WHALEN et al., 1987); (b) P2O5 vs. SiO2 variation (CHAPPELL & WHITE, 1992). G eologia C roatica Xiaobo et al.: The characteristics of granites in the Gaofeng and Baocheng areas, Hainan Province, China ... 101 previously published in the literature (PITCHER et al., 1985; WU et al., 2003b). According to GE et al. (2003) and TANG et al. (2014), basic intrusive rocks with strong arc features in the same area and in the same geological time period (i.e., early and late Cretaceous in the southern of Hainan) have the same geochemical characte- ristics as those of the Gaofeng and Baocheng intrusive rocks. These similar characteristics include high Sr-rich K, high K/Ti- low Ti, low Y and Yb, no negative Eu anomalies, Rb/Sr, Nb/La ratios, enrichment of large ion lithophile elements and high field strength element loss. Basic intrusive rocks originated from the melting of subducted plates (TANG et al., 2014). It can be inferred that the mantle-derived components of the Gaofeng and Baocheng granite magmas may have similar or identical source areas with the basic intrusive rocks. The primary crust and the basic intru- sive rocks mentioned above in the second model may be products of the same source area. Their only difference is the depth of in- trusion. According to TANG et al. (2014), the basic intrusive rocks are derived from the garnet phase. It is speculated here that the primary crust originates from the garnet phase. Magma Differentiation Index (DI) and Solidification Index (SI) values of the Gaofeng and Baocheng granites range from 73 to 86 and from 4 to 12, respectively. In addition, SiO2 is nega- tively correlated with FeO, MgO, CaO, Al2O3, P2O5, and TiO2. It can be concluded here that crystallization differentiation took place during magmatism. The negative anomalies between Nb, Ta, Ti, P, and SiO2 are negatively correlated with Nb/Nb* (Nb*=2Nbn/(Kn+Srn) (Fig. 12d). This indicates that the negative anomalies are mainly caused by crustal AFC (MA et al., 2004). The above characteristics confirm the occurrence of ilmenite, ru- tile, and apatite separation crystallization during magma evolu- tion. The negative anomaly of Ba does not represent the separa- tion and crystallization of potassium feldspar. This is because there is a positive correlation between K2O and SiO2 in the Huck diagram (Fig. 9) and there is only a slight negative anomaly of the Eu element. It is inferred from the insignificant negative Sr anom- aly that there is no or little separation crystallization of plagio- clase. This shows that there is little or no separation of potassium feldspar and plagioclase during magmatic evolution. In summary, the characteristics and evolution process of the source area of the Gaofeng and Baocheng granites are as follows: The partially melted garnet phase affected by the subduction of plates intrudes into the bottom of the crust to form a primary crust with a higher basic composition. The mixed crust formed by the primary crust and the ancient crust partially melts to form a granitic magma. The mixed magma rises and emplaces in the crust with differential crystallization of minerals such as apatite, ilmenite, and rutile. Figure 12. The characteristics of magma source and evolution: (a) Mg#-SiO2 diagram (after STERN & KILIAN,1996); (b) SiO2-MgO diagram (after WANG et al., 2006); (c) Ba/Th-Nb-Zr diagram (ABRATIS, 2001); (d) SiO2-Nb/Nb* diagram (after MA et al., 2004). G eo lo gi a C ro at ic a Geologia Croatica 72 / Special Issue102 Table 3. Major (wt%) and trace element (μg/g) abundances of representative samples from the Gaofeng and Baocheng suites. Gaofeng Baocheng Sample YL501 YL601 YL701 YL703 SHY101 SHY201 SHY302 SHY401 SiO2 65.90 71.45 69.05 69.74 72.42 71.76 72.21 69.37 TiO2 0.71 0.27 0.52 0.45 0.25 0.32 0.28 0.34 Al2O3 15.32 14.32 14.67 14.51 14.63 14.57 14.39 15.80 Fe2O3 1.42 1.42 1.24 0.82 0.87 0.97 1.01 1.14 FeO 2.61 1.00 1.84 1.89 0.69 1.03 0.86 0.98 MnO 0.07 0.06 0.06 0.05 0.03 0.04 0.04 0.03 MgO 1.64 0.54 1.20 1.10 0.58 0.81 0.79 0.89 CaO 3.51 1.71 2.52 2.54 1.58 2.14 1.89 1.70 Na2O 3.21 3.44 3.08 3.01 3.19 3.63 3.45 2.99 K2O 4.08 4.69 4.59 4.83 4.27 3.74 4.09 3.81 P2O5 0.16 0.08 0.11 0.10 0.06 0.09 0.07 0.08 LOI 1.20 0.88 1.00 0.85 1.32 0.76 0.77 2.70 Total 99.84 99.86 99.89 99.89 99.90 99.87 99.85 99.85 ALK 7.29 8.13 7.67 7.84 7.47 7.37 7.54 6.80 A/NKC 0.95 1.03 1.00 0.98 1.15 1.05 1.06 1.30 σ 2.32 2.32 2.26 2.30 1.89 1.89 1.95 1.75 Rb 159.00 153.00 207.00 222.00 173.00 162.00 174.00 137.00 Sr 356.00 191.00 270.00 292.00 327.00 412.00 413.00 431.00 Ba 724.00 719.00 755.00 720.00 705.00 778.00 825.00 858.00 Y 23.50 23.20 27.90 24.10 6.40 17.50 8.50 5.60 Nb 16.30 12.40 18.10 16.50 8.50 11.00 9.60 9.20 Ta 1.35 1.23 1.70 1.83 0.71 1.12 0.90 0.73 Zr 274.00 160.00 256.00 220.00 125.00 152.00 141.00 169.00 Hf 17.00 7.65 14.20 13.00 5.88 8.79 7.37 8.96 Th 18.00 14.00 25.30 25.40 61.00 17.60 12.70 24.20 U 4.10 2.30 5.70 5.10 7.80 6.80 5.30 3.90 La 50.40 57.10 42.20 46.70 24.90 57.30 23.10 33.80 Ce 96.90 103.00 85.30 92.20 40.90 69.70 46.70 57.00 Pr 11.00 11.50 10.40 10.70 4.71 10.40 5.26 6.21 Nd 39.00 39.60 38.40 38.20 15.40 34.10 18.00 19.20 Sm 6.68 6.41 7.09 6.70 2.39 5.66 2.82 2.78 Eu 1.37 1.14 1.22 1.07 0.64 1.35 0.75 0.69 Gd 5.80 5.53 5.92 5.61 1.95 4.84 2.37 2.29 Tb 0.85 0.81 0.93 0.87 0.26 0.71 0.31 0.28 Dy 4.65 4.59 5.36 4.88 1.28 3.62 1.60 1.38 Ho 0.89 0.86 1.01 0.89 0.24 0.64 0.29 0.24 Er 2.42 2.44 2.75 2.37 0.68 1.66 0.83 0.70 Tm 0.41 0.42 0.49 0.42 0.12 0.28 0.14 0.12 Yb 2.35 2.58 2.93 2.41 0.75 1.75 0.95 0.78 Lu 0.34 0.42 0.44 0.35 0.13 0.26 0.16 0.12 ∑REE 222.97 236.48 204.45 213.37 94.35 192.30 103.25 125.46 (La/Yb)N 15.38 15.89 10.32 13.89 23.83 23.46 17.56 31.13 δEu 0.66 0.57 0.56 0.52 0.88 0.77 0.86 0.81 Rb–(Y+Nb), and Rb–(Yb+Ta) trace elements discrimination dia- grams demonstrate that the samples were volcanic-arc granites. Some of the above features correspond to those of a conti- nental margin arc as follows: Early Cretaceous andesite and rhy- olite widely exposed in southern Hainan show typical continental margin arc characteristics (QIANG, 2016; HAN, 2017). The clas- tic compositions, chemical compositions and sedimentary struc- tural characteristics of the Lower Cretaceous Lumuwan Forma- tion and the Upper Cretaceous Baowan Formation all indicate that sedimentation took place in the continental margin arc set- ting. The age of the detrital zircon assemblage especially indi- cates that strong compression and uplift occurred at the turn of early and late Cretaceous in the southern Qiongnan area, and this tectonic activity lasted until the middle of the late Cretaceous 6.3. TECTONIC SETTING The major element characteristics of the Gaofeng and Baocheng intrusions indicate the rocks are high-K calc-alkaline series. The source areas of high-K calc-alkaline series are related to previous subduction (LIEGEOIS et al., 1998). The trace-element spider dia- gram of the Gaofeng and Baocheng intrusions indicates typical negative Nb, Ti, and Ta anomalies, which are similar to the charac- teristics of island-arc granites. Similarly, the mid-oceanic ridge standardized diagram shows that the Gaofeng and Baocheng intru- sions had trace element characteristics similar to those of active continental-margin rocks. On the Rb/30-Hf-Ta×3 diagram (Fig. 14), the Gaofeng and Baocheng intrusions were located within the vol- canic-arc granite domain. Similarly, according to Pearce’s granite tectonic setting discrimination diagram (Fig. 13), the Nb–Y, Ta–Yb, G eologia C roatica Xiaobo et al.: The characteristics of granites in the Gaofeng and Baocheng areas, Hainan Province, China ... 103 Figure 13. Tectonic discrimination diagrams. (a)–(c) after PEARCE et al. (1984); (d) after HARRIS et al. (1986); (ORG – ocean ridge granites; WPG – within plate grani- tes; VAG – volcanic arc granites; Syn-COLG – syn-collision granites). Figure 14. Discriminant diagrams of the tectonic setting (a) R1 vs R2 (after BATCHELOR & BOWDEN, 1985); (b) Rb/30-Hf-Ta×3 (HARRIS et al.,1986,) (ORG – ocean ridge granites; WPG – within plate granites; VAG – volcanic arc granites; Syn-COLG – syn-collision granites). G eo lo gi a C ro at ic a Geologia Croatica 72 / Special Issue104 (TANG, 2014). In addition, YUN (2004) identified the late stage of the Yanshan granites represented by the Tunchang intrusion in Hainan Island as ACG-type granites, which are typical sub- duction granites (XIAO, 2002). Their arc characteristics are widely recognized by almost all scholars who study late Meso- zoic magmatic rocks in Hainan Island, judging by the published literature referenced herein. JIANG & LI (2014) considered that Hainan Island was an Andean continental margin arc tectonic environment before 73Ma in the Late Mesozoic. Moreover, the northward subduction compression tectonics of the ancient Sea provided a necessary high-pressure environ- ment. As a result, the Hainan Province was located in an oceanic- crust subduction tectonic setting in the late Yanshanian period, which would have been an Andean-type continental margin arc environment. This conclusion contradicts the view that magma- tism occurred in an extensional setting (GE et al., 2003; YUN et al., 2003; CHEN et al., 2008). 6.4. IMPLICATIONS FOR REGIONAL GEOLOGY The Cretaceous magmatism of Hainan Island and the Fujian and Zhejiang areas was thought to have been related to western Pa- cific subduction (WANG et al., 2012; JIA et al., 2010; TANG et al., 2014; MAO et al., 2013; LI et al., 2013; WANG et al., 2012). However, the Cretaceous granites on Hainan Island displayed geochemical signatures different to those of the coeval granites from the Fujian and Zhejiang areas (Fig. 15). Specifically, the granites of Hainan Island have the characteristics of high Sr (335), low Yb (1.8), low Y (17.1), and high Sr/Y(20). Although similar granite characteristics have also been reported from the Fujian and Zhejiang Provinces (CHEN, 2014), it is not possible to explain formation of the granites of Fujian and Zhejiang and those of Hainan Island by the same mechanism. Firstly, granites with high Sr are too rare in Fujian and Zhejiang (ZHANG, 2014; JIA et al., 2010). Secondly, some of the granites in Fujian and Zhejiang are actually Guangxi-type granites (ZHANG, 2014) with high Sr and Yb contents (CHEN, 2013, 2014; ZHAO, 2007; ZHANG, 2005), which differ from the high-Sr, low-Yb granites of Hainan Island. Until now, the miarolitic granite widely distributed along the coast of Zhejiang and Fujian has not been found on Hainan Island. In addition, the majority of the granites in the Late Yanshanian in Hainan Island are I-type granites (WANG et al., 1991).But the granites in Fujian and Zhejiang are composed of A-type and I- types, and the proportion of I-type granite is far less than that of the Hainan Island I-type granite in Qiongzhou (JIA et al., 2010; ZHANG, 2014; CHEN, 2013; ZHAO et al., 2007). Source area and diagenetic evolution characteristics of the two diagenetic Figure 15. Geochemical diagrams showing a difference in granite between the Hainan and Zhejiang-Fujian granites in the Cretaceous (a) NK-NKC; (b) Sr-Yb, (after ZHANG, Q., 2014); (c) R1 versus R2, R1=4Si-11(Na+K)-2(Fe+Ti), R2= 6Ca+2Mg+Al, (after BATCHELOR & BOWDEN, 1985); (d) Ta-Rb-Hf, (after HARRIS et al., 1986) data from YUN & XIE (2003); JIA et al. (2010); GE et al. (2003); TANG et al. (2014); CHEN et al. (2013); CHEN et al. (2014); ZHOU & LI (2000); LI et al. (2013); QIU et al. (2008); THUY et al. (2004); NGUYEN et al. (2004); SHELLNUTT et al. (2013). G eologia C roatica Xiaobo et al.: The characteristics of granites in the Gaofeng and Baocheng areas, Hainan Province, China ... 105 models for I-type granite, the granite in Zhejiang and Fujian provi- nces is typical for the first one (QIU et al., 2008, 2012; ZHAO et al., 2012), and the granite of Hainan Island belongs to the second species discussed above. Sr-Nd isotopes also show great differe nces, indicating different magma sources (GE et al., 2003; TANG et al., 2014). This shows that there are fundamental differences in the characteristics of the magma sources and the diagenesis of granites between the two places. The above understanding of the differences between granites from Hainan Island and Fujian-Zhejiang area is in agreement with WANG (1991), who clearly pointed out that the granites in the coastal areas of Fujian and Guangdong are different from the contemporary granites in Hainan Island. Therefore, when discussing the tectonic setting of Yanshanian granite for- mation in Hainan Island, the important influence of oceanic crust subduction is clearly affirmed, though any claim that the ocean crust belongs to the Western Pacific Ocean is not conclusive here. If Fujian, Zhejiang, and Hainan Island have been affected by western Pacific subduction during the Cretaceous, then granites with high Sr/high Yb and low Sr/high Yb, similar to those in the Zhejiang and Fujian area, should also be present in Hainan Island. The low-Sr, high-Yb granites that widely occur in Fujian and Zhe- jiang and the high-Sr, low-Yb granites of Hainan Island represent two different tectonic domains. There are significant differences in the Sr-Nd isotopic composition between the regions which in- dicate that the magmas come from different sources (TANG et al., 2010). It was previously thought that the Cretaceous granites that formed a record of subduction in Fujian and Zhejiang resulted Table 4. Comparison of the geological characteristics of the Hainan and Zhejiang-Fujian granites. Age（Ma） Type ASD TD DD ZST Hainan ZJ-FJ Hainan ZJ-FJ Hainan ZJ-FJ Hainan ZJ-FJ Hainan ZJ-FJ 110-100 I-type I-type 100Ma — SH PH E-W NE-SW 720-770℃ 774-819℃100-90 I-type A-type — — SL 90-70 — A-type — 80-72Ma ASD:The age of associated deposit;TD:Temperature and depth of Rocks generate;DD:Distribution direction of intrusions;SH:Shallow & High temperatures;PH:Plutonic & High temperatures;SL:Shallow & Low temperatures;ZST:Zr saturation temperature;ZJ:Zhejiang; FJ:Fujian.Data from TANG(2010);CHEN(2014);YUN et al.,(2004);ZHOU et al.(1991);LI et al. (2013);GE et al. (2003);ZHAO et al.(2012);KANG et al.(2018). Figure 16. The Cretaceous marginal arc of Hainan Island and its adjacent tectonic setting. G eo lo gi a C ro at ic a Geologia Croatica 72 / Special Issue106 from western Pacific subduction. The influence of the western Pacific subduction was confined to the east of Wuyi Mountain, however, Hainan is located to the far west of Wuyi Mountain, therefore the influence of western Pacific subduction could not have reached Hainan Island. ZHU et al. (2002) & ZHU (2004) believe that the farthest effects of the Pacific plate subduction oc- cur in the Mariana arc, simply because the remaining oceanic crust of late Mesozoic MORB found in the Mariana arc belongs to the Indian Ocean-Tethys type. This also suggests that the sub- duction plates of mantle components during the diagenesis of granites may not originate from the Palaeo-Pacific plate. As a re- sult, the Hainan Island granites were basically not affected by western Pacific subduction. Instead they were influenced by the northward-subducting ancient Sea in the same location as the present-day South China Sea, prior to the opening of the area during the late Mesozoic (TAYLOR & HAYES, 1983; ZHOU, 1992; LI, 1987; YAO et al., 1994; XIA et al., 2000; YAN et al., 2005; MIN et al., 2010; LU et al., 2014). The late Mesozoic granites of Hainan Island have similar geochemical characteristics to granites from the Pearl River Mouth basin and South Vietnam (Fig. 15). Hainan Island and Zhejiang-Fujian area both had similar tectonic settings (i.e., ac- tive continental margin) in the Late Mesozoic. However, there have been differences in the chemical composition of granite, the nature of the source area, magmatic processes involved, and the time series of tectonic evolution. The continental margin arc rep- resented by Hainan Island should be a convergent boundary. It extends westward to reach Yazhuang, Suihe and other places in southern Vietnam, and eastward to the Pearl River Mouth Basin, Fig. 16). According to data from previous studies, the northern shelf of the South China Sea, Hainan Island, and Suihe-Yazhuang, after restoring their geo-historical position, were where the Pearl River Mouth Basin is located. This is backed up by their very similar Cretaceous granite and volcanic rock assemblages, and can be connected to the East-West Andean continental margin arc (MO & SHI, 1987; NGUYEN et al., 2004; THUY et al., 2004; LIANG, 2013; FANG, 2016). According to TAPPONIER’s model (1986), the Indo-China block has slid 650–1200 km southeastward along the Red River Fault since the late Eocene (YANG et al., 1998; LELOUP et al., 1995; WATKINSON et al., 2011; SCHARER et al., 1994). If mode- ling this backwards in time, South Vietnam should be along a line stretching westward from Hainan Island and the Pearl River Mouth basin. The above three sites constitute a latitudinal zone likely representing the active margin of the ancient sea differing from the Pacific system. This ancient sea existed before the expansion of the present- day South China Sea and was roughly equivalent to it, which was close to Hainan Island. Fang (2016) named it as the “Tethys South China Sea” after subducting northward and closing the ancient sea area in the late Mesozoic. Whether the Tethys domain really exists in the study area or not, much more detailed and special investigation is required. According to XIA & HUANG (2000); YAN & ZHOU (2001); ZHU et al. (2004); LIU et al. (2004); YAN (2005), there should be traces of Tethys in the northern waters of the South China Sea. Although the issue of Tethys is not the main point discussed here, we call the northward subduction of oceanic crust (Hainan island facing) in the Late Mesozoic as the “Tethyan South China Sea” for convenience of description. Based on the present findings, the Palaeo-Sea area facing Hainan Island in the late Mesozoic subduction to the north and the palaeo-Pacific area subducted to the West belong to different tectonic settings. The disappeared Palaeo-Sea area is what we refer to here as the “Tethyan South China Sea”. Furthermore, the late Yanshanian Tunchang intrusion of Hainan Island was composed of ACG-type granitoid (YUN & XIE, 2003). Typically, ACG-type granites are granitoids formed in a subduction-zone setting (XIAO et al., 2002). There were dif- ferent rock types, varying ages, and other contrasting elements between the Hainan and Zhejiang-Fujian locations (Table 4). Hainan Island was more readily affected by subduction of the an- cient Sea than by subduction of the western Pacific (Fig. 16). In summary, the “Tethys South China Sea” facing Hainan Island subducted northward, and the subducted slabs entered the garnet peridotite phase and melted at the base of and intruded into the lower part of Hainan Island to form the primary crust. Another part of the melt was intruded into higher positions along deep and large faults to form basic dykes. With the subduction, the mixed crust formed by the primary crust and the ancient base- ment crust were partially melted and further intruded into the granitic rocks. With the further intensification of subduction and compression, the crust and therefore the granite was also uplifted and exposed to the surface and denuded at the same time. With the subduction of the ancient Sea, the denuded granite particles were transported and deposited in the sedimentary strata. The occurrence of zircon is reported in the Late Cretaceous strata of Hainan Island and southeast Qiong basin during the early and late Cretaceous. 7. CONCLUSIONS 1) High-precision U-Pb zircon dating results indicate that the Gaofeng and Baocheng granites in Hainan island crystallized at~107Ma and ~105Ma. 2) The Gaofeng and Baocheng plutons are high-K calc-alka- line I-type granites, resembling magmatic rocks formed in a con- tinental arc setting. 3) The granites of Hainan Island displayed geochemical sig- natures differing from those of coeval granites in the Fujian and Zhejiang areas. Both represented different subduction tectonic domains. The Fujian and Zhejiang areas were affected by western Pacific subduction, Hainan Island was more readily affected by subduction of the Tethyan South China Sea. ACKNOWLEDGEMENT Financial support for this research was provided by the National Natural Science Foundation of China (no. 41572207, no. 41276047, no. 41030853) REFERENCES BARR, S.M. & MACDONALD, A.S. (1981): Geochemistry and geochronology of late Cenozoic basalts of southeast Asia.– Bull. Geol. Soc. Am. 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