Journal of Earth Science, Vol. 29, No. 5, p. 1181–1202, October 2018 ISSN 1674-487X Printed in China https://doi.org/10.1007/s12583-018-0877-2

Petrogenesis and Tectonic Implications of Peralkaline A-Type Granites and Syenites from the Suizhou-Zaoyang Region, Central China

Hafizullah Abba Ahmed 1, 2, Changqian Ma *1, Lianxun Wang1, Ladislav A. Palinkaš3, Musa Bala Girei1, 4, Yuxiang Zhu1, Mukhtar Habib5 1. State Key Laboratory of Geological Processes and Mineral Resources, School of Earth Sciences, China University of Geosciences, Wuhan 430074, China 2. Department of Geology, Modibbo Adama University of Technology, Yola P.M.B. 2076, Nigeria 3. Institute of Mineralogy and Petrology, Faculty of Sciences, University of Zagreb, Zagreb HR-10000, Croatia 4. Department of Geology, Faculty of Earth and Environmental Sciences, Bayero University, Kano, Nigeria 5. Department of Mineral and Petroleum Resources Engineering, Kaduna Polytechnic, Kaduna, Nigeria Hafizullah Abba Ahmed: https://orcid.org/0000-0002-6679-4427; Changqian Ma: https://orcid.org/0000-0002-1778-0547

ABSTRACT: In this study, we present systematic petrological, geochemical, LA-ICP-MS zircon U-Pb ages and Nd isotopic data for the A-type granites and syenites from Suizhou-Zaoyang region. The results show that the peralkaline A-type granites and syenites were episodically emplaced in Suizhou-Zaoyang region between 450±3 and 441±7 Ma which corresponds to Late Ordovician and Early Silurian periods, respec- tively. Petrologically, the syenite-peralkaline granite association comprises of nepheline normative-syenite and alkaline granite in Guanzishan and quartz normative syenite and alkaline granite in Huangyangshan. The syenite-granite associations are ferroan to alkali in composition. They depict characteristics of typical OIB (oceanic island basalts) derived A-type granites in multi-elements primitive normalized diagram and Yb/Ta vs. Y/Nb as well as Ce/Nb vs. Y/Nb binary plots. Significant depletion in Ba, Sr, P, Ti and Eu indi-

cates fractionation of feldspars, biotite, amphiboles and Ti-rich augite. The values of ɛNd(t) in Guanzishan nepheline syenite and alkaline granite are +1.81 and +2.26, respectively and the calculated two-stage model age for these rocks are 1 040 and 1 003 Ma, respectively. On the other hand, the Huangyangshan alkaline

granite has ɛNd(t) values ranging from +2.61 to +3.46 and a relatively younger two-stage Nd model age val- ues ranging from 906 to 975 Ma, respectively. Based on these data, we inferred that the Guanzishan nepheline syenites and granites were formed from fractional crystallization of OIB-like basic magmas de- rived from upwelling of metasomatized lithospheric mantle. The Huangyangshan quartz syenite and gran- ite on the other hand, were formed from similar magmas through fractional crystallization with low input from the ancient crustal rocks. Typically, the rocks exhibit A1-type granite affinity and classified as within plate granites associated with the Ordovician crustal extension and the Silurian rifting. KEY WORDS: Huangyangshan, Guanzishan, OIB derived A-type granites, nepheline syenite, alkaline granite, South Qinling, Suizhou-Zaoyang region.

0 INTRODUCTION granitoids compose of iron-rich mafic silicate mineral such as Several contrasting petrogenetic processes in an extension hedenbergite, ferrohastingsite and annite as well as sodic pyrox- setting (within plate or post-collisional setting) give rise to a geo- ene (e.g., aegirine) and sodic amphiboles (e.g., arfvedsonite and/ chemically and minerallogically distinct group of granitoids gen- or riebeckite). Chemically, these diverse groups of rock are gen- erally dubbed as A-type (Grebennikov, 2014; Vilalva and Vlach, erally characterized by remarkable enrichment in high field 2014; Peng et al., 2012; Nardi and de Fatima Bitencourt, 2009; strength elements (HFSE) (e.g., Nb, Ta, and Zr), F, REE (Wang DallʼAgnol and de Oliveira, 2007; Katzir et al., 2007; Litvinovsky et al., 2018; Eby, 1992). Additionally, they have high alkali con- et al., 2002; King et al., 1997; Eby, 1992). Minerallogically, these tent, high FeOT/MgO and Al/Ga, but low CaO content compared to other granitoids (Whalen et al., 1987). Typically, they cover *Corresponding author: [email protected] wide spectrum in composition ranging from strictly alkaline/ © China University of Geosciences and Springer-Verlag GmbH peralkaline, metaluminous and occasionally, peraluminous Germany, Part of Springer Nature 2018 (Bonin, 2007; Martin, 2006). These petrologically distinct grani- toids (also referred to as A-type) are widespread both in space Manuscript received May 12, 2018. and time (e.g., Litvinovsky et al., 2002; Whalen et al., 1987). Manuscript accepted August 19, 2018. Largely due to their association with significant Nb, Ta, Sn, U

Ahmed, H. A., Ma, C. Q., Wang, L. X., et al., 2018. Petrogenesis and Tectonic Implications of Peralkaline A-Type Granites and Syenites from the Suizhou-Zaoyang Region, Central China. Journal of Earth Science, 29(5): 1181–1202. https://doi.org/10.1007/s12583-018-0877- 2. http://en.earth-science.net 1182 Hafizullah Abba Ahmed, Changqian Ma, Lianxun Wang, Ladislav A. Palinkaš, Musa Bala Girei, and et al. and REE mineralization, A-type granites continue to attract at- (Dong and Santosh, 2016; Dong et al., 2011; Zhang et al., 2001). tention from several researchers globally (e.g., Jiang et al., 2018; The Tongbai-Hongʼan-Dabie orogenic belt in the South Qinling is Li et al., 2018, 2014; Dostal and Shellnut, 2015; Shellnutt et al., further divided into six tectonic units of different rock assem- 2009). However, in spite of significant advances recorded re- blages, separated by sutures and major fault systems such as cently in applying experimental petrology, trace element and Xiaotian-Mozitan suture, Xixian suture, Tanlu fault, Tongbai- isotopic systematics in constraining the petrogenesis and geody- Mozitan fault, Xiangfan-Guangji fault, Dawu fault and Shangma namic setting of igneous rocks, the genesis of A-type granitoids fault. These six tectonic units include the Beihuaiyang tectonic still remain highly controversial (e.g., Litvinovsky et al., 2015). region, which comprised predominantly of Meso–Neoproterozoic The major controversy lies in the determination of the most suit- Luzhengguan orthogneisses and Paleozoic metaclastic rocks with able magma source for these granitoids (Bonin, 2007; Martin, greenschist facies metamorphic characteristics. The South Dabie 2006; Eby, 1992). Several petrogenetic models involving crustal, unit which is divided by Xiaotian-Mozitan suture has its compo- mantle or the direct mixing of these two distinct end members nents ranging from high-pressure (HP) amphibolites, eclogites sources have been proposed for genesis of A-type granites (Lit- and schist facies to ultra-high-pressure (UHP) eclogite facies (Zhu vinovsky et al., 2015, 2011; Dostal et al., 2014; Jahn et al., 2009; et al., 2017) rocks. Other tectonic units include Nanwan, South Martin, 2006; Wu et al., 2002; King et al., 1997; Patiño Douce, Hongʼan, North Tongbai and South Tongbai units (Fig. 1a). A 1997; Turner et al., 1992). These A-type granites are more com- major feature in South Tongbai tectonic unit is the Meso– positionally diverse than those were initially recognized by Neoproterozoic Wudang uplift, which includes low-grade meta- Loiselle and Wones (1979), who introduced the term “A-type” to morphosed sedimentary-volcanic rocks of the Wudangshan and denote granitoids that are mildly “alkaline” and “anorogenic”; Yaolinghe groups (Wang et al., 2016). In South Qinling, many the term “anhydrous” was later introduced by Bowden (1985), to giant granitic and dioritic intrusions of Neoproterozoic Age, such highlight their low oxygen fugacity and water content. Impor- as the Fenghuangshan and Douling plutons (Dong and Santosh, tantly, the significantly high content of both large-ion lithophile 2016) are overlain by the thick Sinian–Cambrian sedimentary elements (LILE) and HFSE in these rocks suggests that they are sequences, Cambrian–Ordovician carbonate rocks, Silurian shale, derived either from enriched OIB (oceanic island basalts)-like Devonian–Carboniferous clastic sediments intercalated with lime- mantle source or from continental crust (Eby, 1992). However, stone and limited Permian–Triassic sandstone (Zhang et al., 2001). isotopic composition of two enriched OIB mantle reservoirs: South Qinling orogenic belt has experienced widespread EMI and EMII typically overlap with those of continental crust Early Paleozoic magmatism extending to the east from North (Zindler and Hart, 1986). Hence, some OIB mantle derived A- Dabashan Mountains to Suizhou-Zaoyang regions. Mafic and type granitoids could be misinterpreted as crustally derived (e.g., intermediate outcrops constitute the dominant rock units in these Litvinovsky et al., 2015). In this regard, more composite data and areas including limited occurrences of carbonitite and syenitic geological input are therefore required in constraining the origin complexes (Wang et al., 2017; Cao L et al., 2015; Cao Q et al., of A-type granites (Wang et al., 2018; Litvinovsky et al., 2015; 2015; Xu et al., 2008; Zhang et al., 2007; Dong et al., 1998; Yu, Dostal et al., 2014; Jahn et al., 2009; Shellnutt et al., 2009). 1992; Li, 1991). The Guanzishan and Huangyangshan alkaline In this contribution, we present major and trace elements, granitoids occur in the southern margin of Tongbai Orogen out- mineral chemistry, Sr-Nd isotope as well as zircon U/Pb data of cropping within the South Tongbai tectonic zone and they form some alkaline granites and syenites from Suizhou-Zaoyang part of the intermediate to felsic rocks found in this region. region within the Tongbai-Hongʼan-Dabie orogenic belt in Central China. The Huangyangshan and Guanzishan alkaline 1.2 Sample Description granitoids are arguably the least known in South Qinling oro- The sampling locations are shown in Figs. 1b and 1c. The genic belt. Our aim is to constrain the petrogenesis of the grani- Huangyangshan pluton is covered in the southern part by Creta- toids and infer their tectonic implication within the framework ceous meta-sedimentary rocks, comprising matrix supported con- of geodynamic evolution of the Tongbai-Hongʼan-Dabie oro- glomeration of different rocks (sandstone, limestone, marble, etc.). genic belt in Central China. Huangyangshan pluton consists mainly of quartz syenites and very little occurrence of alkaline granite (Fig. 1b), whereas in 1 GEOLOGICAL SETTING AND SAMPLE DESCRIP- Guanzishan area, nepheline syenite, quartz syenite and minor TION occurrence of alkali granites occur (Fig. 1c). The plutons from 1.1 Geological Setting both areas are composed of fine-medium-coarse grained and por- The Tongbai-Hongʼan-Dabie Orogen which is part of the E- phyritic textures (Fig. 2). They range in color from dark to grayish W trending Qinling orogenic belt is outcropped between the brown containing amphiboles, quartz and K-feldspars under vis- North China Block (NCB) and Yangtze Craton (Dong and San- ual observation in hand specimen. The rocks in Huangyangshan tosh, 2016), linking Kunlun-Qilian Orogen to the west and Dabie- are composed of K-feldspar (~45%), amphiboles (~25%), biotite Sulu Orogen towards the east (Fig. 1a). Shangdan suture has sub- (~20%) and plagioclase (~10%). The feldspars have undergone divided the Qinling Orogon into south and north (Fig. 1a), with incipient alteration (Figs. 2a–2d). They range from subhedral to North Qinling believed to be part of the NCB, while the South euhedral and include orthoclase feldspars and sanidine. Qinling as part of the Yangtze Craton before the Mianlue Ocean A small massive stock of Guanzishan nepheline syenites opened up in the Devonian (Wang et al., 2017; Zhang et al., 2001). outcropped in Yulong Village. The rocks are medium-coarse During the Early Mesozoic, the NCB and the South China Block grained nepheline-bearing syenites, with grayish-dark green (SCB) merged after the closing of the Mianlue Ocean Basin color and massive structure. They compose of feldspars ~50%,

Petrogenesis and Tectonic Implications of Peralkaline A-Type Granites and Syenites 1183

Figure 1. Simplified geological map showing the study area in Qinling orogenic belt (a) (modified after Zhu et al., 2017). NCB. North China Block; SCB. South China Block. Simplified geological map of Huangyangshan area (b), and the Guanzishan area (c).

1184 Hafizullah Abba Ahmed, Changqian Ma, Lianxun Wang, Ladislav A. Palinkaš, Musa Bala Girei, and et al.

Figure 2. Photographs showing the specimen of alkaline granite from Huangyangshan (a)–(b), quartz syenite from Huangyangshan (c)–(d), nepheline syenite from Guanzishan (e)–(f). Qz. Quartz; Bt. biotite; Kfs. K-feldspar; Amp. amphibole; Pl. plagioclase; Ne. nepheline. biotite ~20%, amphibole ~20% and nepheline ~10% (Figs. 2e Guanzishan plutons were determined at the State Key Laboratory and 2f). Rocks in this area are altered and characterized by of Geological Processes and Mineral Resources, China University subhedral texture. A total number of eight samples have been of Geosciences, Wuhan, with a JEOL JXA-8100 electron probe used in this study. Six samples are from Huangyangshan Mas- micro analyzer equipped with four wavelength-dispersive spec- sif, while two samples are from Guanzishan. The distribution trometers (WDS). Initially, the samples were coated with a thin of samples from Huangyangshan and Guanzishan are shown as conductive carbon film prior to analysis. The precautions sug- red stars in Figs. 1b and 1c, respectively. gested by Zhang and Yang (2016) were used to minimize the difference of carbon film thickness between samples and obtained 2 ANALYTICAL METHODS a ca. 20 nm uniform coating. During the analysis, an accelerating 2.1 Mineral Chemistry voltage of 15 kV, a beam current of 20 nA and a 10 µm spot size The composition of amphiboles from Huangyangshan and were used to analyze the minerals. The ZAF procedure was em-

Petrogenesis and Tectonic Implications of Peralkaline A-Type Granites and Syenites 1185 ployed in order to correct for the atomic number, absorption and separated using cation columns, followed by separation of Nd fluorescence effects. Amphibole stoichiometry and nomenclature from the REE fraction using HDEHP columns. All isotopic data were determined based on recommendation by Hawthorne et al. were analyzed by MC-ICP-MS. The 87Sr/86Sr value of the (2012) using an Excel spreadsheet programmed for amphibole NBS987 standard and 143Nd/144Nd value of the JNdi-1 standard classification (Version 1.9, Locock, 2012) (Table 1). were 0.710 288±0.000 028 (2σ) and 0.512 109±0.000 012 (2σ), respectively; all measured 143Nd/144Nd and 86Sr/88Sr values were 2.2 Whole-Rock Major and Trace Elements Analyses fractionated and corrected to 146Nd/144Nd=0.721 9. Eight samples from Huangyangshan and Guanzishan alka- line granitoids were first crushed using steel crusher and subse- 3 RESULTS quently pulverized to <200 mesh size using an agate mill. 3.1 Amphibole Composition Analysis of major element compositions was carried out at the The composition of amphiboles from the Guanzishan and ALS Laboratory, Guangzhou, using X-ray fluorescence (XRF) Huangyangshan alkaline granitoids are presented in Table 1, Fig. techniques. Analytical precision for major element varies from 3. Owing to alteration in Guanzishan samples, only very few 2% to 5%. Trace elements were analyzed using Agilent 7700e fresh points were analyzed. The amphibole-group minerals have ICP-MS at the Wuhan Sample Solution Analytical Technology a double silicate chain structure and a generic chemical formula

Co. Ltd., Wuhan, China following the procedures outlined by of AB2CVI5TVI8O22(OH) (Leake et al., 1997). According to Liu et al. (1996). International standard materials (e.g., AGV-2, Leake et al. (1997) classification, calcic amphiboles generally BHVO-2, RGM-2 and RGM-2) were measured to monitor data have Ca+Na>1 (apfu) in the B-site with Na being less than 0.5 quality during analysis, which show a correlative standard de- (apfu) while sodic-calcic amphiboles typically have Ca+Na>1 viation of ±5%–10% for most of the trace elements. apfu in the B-site with Na ranging between 0.5 and 1.5 (apfu). High contents of Na in the B-site (>1.5 apfu) and alkalis in the 2.3 Zircon U-Pb Dating A-site (>0.5 apfu) are indicative of sodic amphiboles. The am- Zircons from Huangyangshan (quartz syenite) and Guanzis- phiboles in the study area are subdivided into riebeckite, potassic han (nepheline syenite) were separated using conventional den- arfvedsonite, ferro-eckermannite, ferro-ferri-winchite, ferro- sity and magnetic separation techniques and handpicked under a katophorite and ferro-ferri-katophorite (Locock, 2012, Table 1). binocular microscope. The grains were subsequently mounted in Majority of the amphiboles are sodic and only few of them fall epoxy resin, polished to half their thickness and they were later within the range of sodic-calcic affinity (Fig. 4). photographed in transmitted and reflected light. The morphology and internal structures of zircons were examined using cathodo- 3.2 Whole Rock Major and Trace Elements Composition luminescence (CL) imaging prior to U-Pb isotopic analysis. Zir- Major and trace elements data are presented in Table 2. Sil- con CL images were obtained at the Wuhan Sample Solution ica (SiO2) content in the rocks ranges from 59.35 wt.% to 72.20 Analytical Technology Co. Ltd., Wuhan, China, using an ana- wt.%. The granitoids are typically alkaline as shown on T T lytical scanning electron microscope (JSM-IT100) connected to a (Al2O3+CaO)/(FeO +Na2O+K2O) vs. 100(MgO+FeO +TiO2)/ GATAN MINICL system. Zircon U-Pb dating was conducted by SiO2 discrimination diagram (Fig. 5a) and peralkaline in compo- the LA-ICP-MS method at the same laboratory, using an Agilent sition (Fig. 5b). The alkaline suites range in composition from 7500a ICP-MS equipped with a 193 nm ComPex102-ArF laser- quartz syenites to alkaline granites sensu-stricto; though one ablation system (Coherent Inc, USA). Helium was used as the sample from Guanzishan area plots within the field of nepheline carrier gas, and a spot size of 32 µm with a repetition rate of 6 Hz syenite as shown on the discrimination diagram proposed by De was applied to all analyses with a 10 J/cm2 energy density. Zir- la Roche et al. (1980) (Fig. 5c). Similarly, on the 10 000×Al/Ga con 91500 was used as an external calibration standard for age vs. Y and Na2O+K2O discrimination diagram proposed by calculation, while NIST SRM 610 and Plesovice were also used Whalen et al. (1987), all the granitoids plot within the field of A- for quality control. All analyzed 207Pb/206Pb and 206Pb/238U ratios type granite (Figs. 6a and 6b). The potassium content in the were calculated using ICPMSDataCal (Liu et al., 2010). The age granitoids is high (K2O=3.65 wt.%–6.78 wt.%) and in Na2O+ calculations and concordia plots were made using ISOPLOT K2O-CaO vs. SiO2 diagram (Fig. 6c), they plot within the field of (Ludwig, 2003). alkaline granites. According to the classification scheme pro- posed by Frost et al. (2001), the granites are ferroan and alkalic 2.4 Whole Rock Sr-Nd Isotopes in composition (Fig. 6d) similar to the granites in Gardar Prov- Whole rock Sr and Nd isotopic compositions of quartz ince, South Greenland (Frost et al., 2001). syenite, alkaline granite and nepheline syenite from Huangyang- In the primitive mantle multi-element normalized diagram, shan and Guanzishan were determined using a micromass iso- the granitoids are characterized by enrichment of both LILE such probe multi-collector-inductively coupled plasma-mass spec- as Rb, Th, La, Ce, and Nd and HFSE such as Nb, Ta and Zr (Figs. trometer (MC-ICP-MS) at the Qingdao Speed Analysis and Test- 7a and 7b) which is typical of rocks derived from OIB-like ing Company Limited, Shandong, China. Analytical procedures sources (Eby, 1992). Additionally, in the Yb/Ta vs. Y/Nb and for Sr and Nd isotopes are described in detail by Li et al. (2004) Ce/Nb vs. Y/Nb binary plots, the syenite and peralkaline granites and Wei et al. (2002). Chemical separation of Sr and Nd is similar from both Guanzishan and Huangyangshan plot within OIB field to the methods described by Li and McCulloch (1998). Sample (Figs. 7c and 7d). Similarly, some coeval mafic rocks (e.g., powder (∼50–100 mg) were digested with distilled HF-HNO3 in Ziyang-Zhenba gabbro and diabase) and some rock units with screw-top PFA beakers at 120 °C for 15 d. Sr and REEs were then similar chemical composition such as Mogou and Sandaogou

1186 Table 1 Representative microprobe analysis of amphiboles from alkaline granitoids of Guanzishan and Huangyangshan (classification of amphiboles is based on Locock, 2012)

Sample 3-5A2-1 3-5-A2-2 3-5A-1 3-5-A1-2 1-2A-1 1-2A-2 3-3-A1-2 3-3-A2-3 3-3A-4 2-A1-1 2-1A-2 2-1A2-1 2-1A2-2 3-6-A1 3-6-1-A-2 Rock type HY QS HY QS HY QS HY QS HY QS HY QS HY QS HY QS HY QS HY QS HY QS HY QS HY QS HY AG HY AG

SiO2 51.685 50.269 51.763 51.899 49.393 49.419 51.271 50.823 50.341 50.694 50.351 49.405 49.71 51.644 51.307

Al2O3 0.617 0.928 0.692 1.211 1.529 1.712 1.708 0.413 0.665 0.534 0.618 0.675 0.732 0.422 0.387

TiO2 1.396 1.083 0.676 0.059 1.82 1.582 0.134 0.255 0.558 1.881 1.964 1.787 2.056 0.481 0.359 FeO 33.328 32.595 34.037 34.237 29.5 29.175 34.693 35.662 33.62 30.706 31.346 29.927 30.816 32.409 34.3

MnO 0.858 1.013 0.657 0.593 0.93 1.264 0.73 0.808 0.976 1.298 1.24 1.315 1.528 1.347 1.221 Hafizullah Abba Ahmed,Changqian Ma MgO 1.11 1.018 1.178 0.849 3.537 3.843 0.512 0.344 1.117 1.863 1.793 1.947 1.999 2.058 1.191 CaO 1.004 1.305 0.698 0.029 4.764 5.475 0.892 1.136 2.062 1.3 0.816 2.881 2.615 1.281 0.817

Na2O 6.714 6.588 6.943 7.12 4.17 4.111 6.538 6.602 5.707 6.626 6.544 6.452 6.228 6.408 6.499

K2O 1.057 1.683 0.93 0.246 0.891 0.904 0.438 0.406 1.367 1.533 1.396 1.352 1.353 1.265 0.609

Cr2O3 - 0.026 - 0.021 0.06 0.026 0.133 0.01 0.057 0.002 0.028 0.011 0.113 0.003 0.098 NiO 0.013 0.01 - 0.003 0.001 - 0.027 0.051 - 0.043 0.004 - - 0.017 - Total 97.782 96.518 97.574 96.267 96.595 97.511 97.076 96.51 96.47 96.48 96.1 95.752 97.15 97.335 96.788 Formulas based on 24 oxygen atoms Si 8.19 7.98 8.02 8.05 7.80 7.75 7.94 8.00 7.96 8.00 7.93 7.99 7.92 8.01 7.98 AlIV 0.00 0.02 0.00 0.00 0.20 0.25 0.06 0.00 0.04 0.00 0.07 0.01 0.08 0.00 0.02 T-site 8.19 8.00 8.02 8.05 8.00 8.00 8.00 8.00 8.00 8.00 8.00 8.00 8.00 8.01 8.00

Ti 0.17 0.13 0.08 0.01 0.22 0.19 0.02 0.03 0.07 0.22 0.23 0.22 0.25 0.06 0.04 , Lianxun Wang, Ladislav A.Palinka AlVI 0.12 0.16 0.13 0.22 0.09 0.06 0.26 0.08 0.09 0.10 0.05 0.12 0.06 0.08 0.05 Cr 0.00 0.00 0.00 0.00 0.01 0.00 0.02 0.00 0.01 0.00 0.00 0.00 0.01 0.00 0.01 Mn3+ 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 Fe3+ 0.00 0.78 1.17 1.46 0.28 0.25 1.41 1.38 1.09 0.67 1.00 0.07 0.19 1.19 1.53 Ni 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.01 0.00 0.01 0.00 0.00 0.00 0.00 0.00 Mn2+ 0.04 0.14 0.09 0.08 0.00 0.02 0.10 0.11 0.13 0.17 0.17 0.14 0.10 0.18 0.16 Fe2+ 4.42 3.55 3.25 2.98 3.58 3.57 3.09 3.32 3.36 3.39 3.13 3.98 3.91 3.01 2.94 Mg 0.26 0.24 0.27 0.20 0.83 0.90 0.12 0.08 0.26 0.44 0.42 0.47 0.47 0.48 0.28 C-site 5.00 5.00 4.98 4.95 5.00 5.00 5.00 5.00 5.00 5.00 5.00 5.00 5.00 4.99 5.00 Mn2+ 0.08 0.00 0.00 0.00 0.12 0.14 0.00 0.00 0.00 0.00 0.00 0.04 0.11 0.00 0.00

Ca 0.17 0.22 0.12 0.00 0.81 0.92 0.15 0.19 0.35 0.22 0.14 0.50 0.45 0.21 0.14 š, Musa BalaGirei, and etal. Na 1.75 1.78 1.88 2.00 1.03 0.94 1.85 1.81 1.65 1.78 1.86 1.46 1.44 1.79 1.86 B-site 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 Na 0.31 0.25 0.20 0.15 0.25 0.31 0.11 0.21 0.10 0.25 0.14 0.56 0.48 0.14 0.10 K 0.21 0.34 0.18 0.05 0.18 0.18 0.09 0.08 0.28 0.31 0.28 0.28 0.28 0.25 0.12 A-site 0.53 0.59 0.39 0.20 0.42 0.50 0.20 0.29 0.38 0.56 0.42 0.84 0.76 0.39 0.22 Classifi- Fe-Eck Po-Arf Rbk Rbk Fe-Fe- Fe-Fe- Rbk Rbk Rbk Po-Arf Rbk Fe-Kap Fe-Fe-Kap Rbk Rbk cation Win Win

Petrogenesis and TectonicImpl

Table 1 Continued

Sample 5-3A1-2 03-05B1 03-05B2 03-05B-2 01-01B1 01-01B2 03-03B1 03-03B2 03-03B3 03-03B4 02-1B1 02-1B2 0306-AB1 0306-AB2 0306-B2 05-3B1 Rock type HY QS HY QS HY QS HY QS HY QS HY QS HY QS HY QS HY QS HY QS HY QS HY QS HY AG HY AG HY AG GZ

SiO2 50.17 50.669 52.499 54.426 49.327 49.55 51.117 51.666 51.509 50.857 50.943 49.521 51.334 49.213 51.346 50.449

Al2O3 1.329 0.675 0.257 1.277 2.252 1.854 0.821 1.423 0.346 0.758 0.699 0.794 1.01 0.251 0.439 1.427

TiO2 1.866 1.404 0.214 0.06 1.291 1.497 0.152 0.093 0.06 0.598 1.127 1.926 0.274 1.754 0.282 1.803 FeO 26.916 33.141 35.772 34.092 29.881 28.939 34.623 33.206 36.187 33.685 31.439 29.928 34.354 33.174 33.753 27.76 MnO 0.934 0.926 0.556 0.54 1.172 1.255 0.796 0.835 0.818 0.865 1.088 1.553 1.214 1.733 1.107 0.926 MgO 4.662 0.817 0.735 0.804 3.821 4.023 1.281 1.589 0.222 1.211 1.971 2.046 0.647 1.246 1.508 4.122 ications of Peralkaline A-Type Granites and Syenites CaO 5.716 2.32 0.03 0.023 5.224 5.926 0.844 1.171 0.757 1.906 0.776 2.726 1.159 0.686 0.343 5.445

Na2O 3.732 6.098 7.146 7.183 4.293 4.067 6.589 6.516 6.575 5.928 6.847 6.393 6.562 6.396 6.83 3.622

K2O 1.195 1.396 0.091 0.19 0.953 0.994 0.551 0.318 0.252 1.142 1.203 1.425 0.289 0.791 0.483 1.176

Cr2O3 0.008 0.068 0.002 0.02 - 0.022 0.008 0.049 0.014 0.056 0.079 0.02 0.038 1.199 0.065 0.045 NiO - - - - 0.018 - 0.002 - 0.031 0.014 0.009 - - 0.009 0.014 - Total 96.528 97.514 97.302 98.615 98.232 98.127 96.784 96.866 96.771 97.02 96.181 96.332 96.881 96.452 96.17 96.775 Formulas based on 24 oxygen atoms Si 7.85 8.00 8.08 8.15 7.68 7.73 7.93 7.97 8.04 7.97 7.99 7.96 7.99 7.91 7.99 7.87 AlIV 0.15 0.00 0.00 0.00 0.32 0.27 0.07 0.03 0.00 0.03 0.01 0.04 0.01 0.05 0.01 0.13 T-site 8.00 8.00 8.08 8.15 8.00 8.00 8.00 8.00 8.04 8.00 8.00 8.00 8.00 8.00 8.00 8.00 Ti 0.22 0.17 0.02 0.01 0.15 0.18 0.02 0.01 0.01 0.07 0.13 0.23 0.03 0.17 0.03 0.21 AlVI 0.10 0.13 0.05 0.23 0.10 0.07 0.09 0.23 0.06 0.11 0.12 0.11 0.18 0.00 0.07 0.13 Cr 0.00 0.01 0.00 0.00 0.00 0.00 0.00 0.01 0.00 0.01 0.01 0.00 0.00 0.15 0.01 0.01 Mn3+ 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 Fe3+ 0.20 0.59 1.58 1.50 0.32 0.21 1.57 1.38 1.55 1.11 1.02 0.11 1.33 0.54 1.60 0.33 Ni 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00

Mn2+ 0.07 0.12 0.07 0.07 0.00 0.05 0.10 0.11 0.11 0.11 0.14 0.15 0.16 0.00 0.15 0.07 Fe2+ 3.32 3.79 3.03 2.77 3.54 3.57 2.92 2.90 3.18 3.31 3.11 3.91 3.14 3.84 2.80 3.29 Mg 1.09 0.19 0.17 0.18 0.89 0.94 0.30 0.37 0.05 0.28 0.46 0.49 0.15 0.30 0.35 0.96 C-site 5.00 5.00 4.92 4.75 5.00 5.00 5.00 5.00 4.96 5.00 5.00 5.00 5.00 5.00 5.00 5.00 Mn2+ 0.06 0.00 0.00 0.00 0.15 0.12 0.00 0.00 0.00 0.00 0.00 0.07 0.00 0.24 0.00 0.05 Ca 0.96 0.39 0.00 0.00 0.87 0.99 0.14 0.19 0.13 0.32 0.13 0.47 0.19 0.12 0.06 0.91 Na 0.98 1.61 2.00 2.00 0.94 0.89 1.86 1.81 1.87 1.68 1.87 1.47 1.81 1.57 1.94 1.04 B-site 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 2.00 Na 0.15 0.26 0.14 0.09 0.35 0.34 0.12 0.14 0.12 0.12 0.21 0.53 0.17 0.43 0.12 0.05 K 0.24 0.28 0.02 0.04 0.19 0.20 0.11 0.06 0.05 0.23 0.24 0.29 0.06 0.16 0.10 0.23 A-site 0.39 0.54 0.16 0.13 0.54 0.54 0.23 0.20 0.17 0.35 0.45 0.82 0.23 0.59 0.21 0.29 Classifi- Fe-Fe- Po-Arf Rbk Rbk Fe-Fe- Fe-Fe- Rbk Rbk Rbk Rbk Rbk Fe-Fe- Rbk Arf Rbk Fe-Fe- cation Win Kap Kap Kap Win 1187 Fe-Fe-Win. Ferro-ferri-winchite; Eck. eckermannite; Rbk. riebeckite; Arf. arfvedsonite; Po. potassic; Kap. katophorite. HY. Huangyangshan; GZ. Guanzishan; QS. quartz syenite; AG. alkaline granite. 1188 Hafizullah Abba Ahmed, Changqian Ma, Lianxun Wang, Ladislav A. Palinkaš, Musa Bala Girei, and et al.

Table 2 Major (wt.%) and trace elements (ppm) compositions of the rocks from Huangyangshan and Guanzishan

Pluton Huangyangshan pluton Guanzishan pluton

Rock type QS QS QS QS AG QS NS AG

Sample 16SZ01-01 16SZ02-01 16SZ03-03 16SZ03-05 16SZ03-06 16SZ04-01 16SZ05-03 16SZ06-01

SiO2 70.26 69.91 67.07 69.21 70.14 69.76 71.36 59.35

TiO2 0.63 0.42 1.15 0.23 0.51 0.46 0.39 0.42

Al2O3 11.64 12.74 10.98 13.48 11.78 12.4 12.91 18.76

Fe2O3 7.32 5.09 10.09 5.22 6.82 5.52 3.69 6.03

FeO 6.59 4.58 9.08 4.7 6.14 4.97 3.32 5.43

MnO 0.11 0.13 0.32 0.1 0.23 0.15 0.08 0.16

MgO 0.22 0.11 0.15 0.09 0.13 0.03 0.5 0.38

CaO 0.78 0.33 0.55 0.12 0.35 0.31 1.08 0.45

Na2O 4.68 5.69 5.27 5.66 5 5.54 4.62 6.28

K2O 3.65 4.84 3.96 5.3 4.55 4.97 4.92 6.78

P2O5 0.04 0.02 0.03 0.01 0.01 0.01 0.04 0.11

LOI 0.31 0.5 0.45 0.58 0.37 0.39 0.43 0.74

Total 106.23 104.36 109.1 104.7 106.03 104.51 103.34 104.89

Li 1.13 17.64 10.04 19.66 19.53 14.3 1.97 78.82

Be 5.82 3.67 3.5 3.48 3.59 3.91 3.99 6.05

Sc 1.47 1.22 1.87 1.25 1.47 0.83 1.68 2.44

V 11.79 1.04 1.37 1.07 1.19 0.7 10.9 0.57

Cr 0.5 0.35 0.66 0.62 0.43 0.28 2.2 0.41

Co 2.11 0.32 0.84 0.78 0.58 0.18 3.22 2.6

Ni 1.19 0.88 0.94 1.21 1.23 0.85 2.37 0.8

Cu 3.24 4.3 4.31 3.6 3.25 3.37 14.46 5.42

Zn 56.61 121.92 161.58 115.98 133.63 117.99 66.86 114.3

Ga 41.55 41.17 36.4 42.47 38.9 42.72 31.87 38.01

Rb 39.38 112.34 58.83 127.98 82.03 123.44 56.41 379.85

Sr 27.89 3.91 10.91 2.6 8.82 7.27 43.68 55.69

Y 86.18 39.11 30.32 22.23 25.59 44.32 45.31 68.21

Zr 844.83 417.04 368.53 274.99 297.31 503.55 408.89 2 652.95

Nb 113.97 71.41 64.28 46.83 55 81.62 90.06 426.36

Sn 5.11 3.66 5.43 3.37 2.77 5.37 4.06 14.42

Cs 0.21 0.37 0.48 0.29 0.35 0.49 0.34 8.2

Ba 178.25 29.63 244.63 70.77 163.35 114.38 441.67 235.9

Hf 19.95 10.65 9.78 7.13 7.35 12.86 10.28 57.63

Ta 8.17 4.74 3.93 2.88 3.45 5.49 5.37 22.23

Tl 0.06 0.15 0.12 0.24 0.2 0.26 0.13 0.35

Pb 5.43 7.55 3.51 6.95 6.38 8.34 2.32 28.01

Th 19.37 8.87 5.74 4.79 5.6 9.36 11.11 60.92 U 4.1 1.62 1.21 1.02 1.08 1.64 2.33 14.3

La 101.08 50.19 47.94 37.68 28 60.95 50.28 192.02

Ce 204.3 101.53 97.88 71.95 68.38 113.49 105 276.34

Petrogenesis and Tectonic Implications of Peralkaline A-Type Granites and Syenites 1189

Table 2 Continued

Pluton Huangyangshan pluton Guanzishan pluton Rock type QS QS QS QS AG QS NS AG Sample 16SZ01-01 16SZ02-01 16SZ03-03 16SZ03-05 16SZ03-06 16SZ04-01 16SZ05-03 16SZ06-01 Pr 22.71 12 12.01 8.89 6.85 14.16 12.27 37.99 Nd 89.63 46.55 46.73 33.45 27.05 53.85 47.02 126.39 Sm 18.63 9.21 9.09 6.21 5.6 11.42 9.77 21.98 Eu 1.96 1.12 1.18 0.72 0.79 1.78 1.2 0.87 Gd 16.45 7.68 6.86 4.67 4.65 9.26 8 16.39 Tb 2.82 1.35 1.12 0.79 0.8 1.55 1.37 2.7 Dy 16.27 7.68 6.35 4.21 4.82 8.57 8.06 14.06 Ho 3.19 1.53 1.23 0.84 0.93 1.64 1.63 2.7 Er 9.06 4.22 3.45 2.45 2.77 4.54 4.65 7.04 Tm 1.34 0.62 0.63 0.43 0.44 0.66 0.74 1.15 Yb 8.62 4.09 4.59 3.03 3.13 4.25 4.65 7.71 Lu 1.3 0.61 0.74 0.53 0.58 0.66 0.69 1.32 Eu/Eu* 0.34 0.41 0.46 0.41 0.48 0.53 0.42 0.14 Mg# 6.55 4.79 3.35 3.86 4.25 1.25 24 12.81

(La/Yb)N 7.81 8.19 6.97 8.3 5.97 9.55 7.21 16.6 ∑REE 497.37 248.37 239.8 175.83 154.8 286.78 255.33 708.67

QS. quartz syenite; AG. alkaline granite; NS. nepheline syenite; LOI. loss on ignition; Mg#=Mg2+/(Mg2++Fe2+)×100. syenite from South-Central China also plot within or near a field 87Rb/86Sr ratio is rather high in all the rocks analyzed. The Guan- typical of OIB derived rocks (Figs. 7c and 7d). Negative Ba and zishan nepheline syenites and alkaline granites have 87Rb/86Sr Sr in Guanzishan and Huangyangshan syenites and granites (Fig. values of 3.74 and 19.77, respectively, while the Huangyangshan 7a) suggest feldspar fractionation. Furthermore, the syenites and alkaline granites have 87Rb/86Sr values ranging from 48.28 to the granites also show enrichment in LREE but depletion in 140.84, respectively. Such high 87Rb/86Sr ratios in the rocks often

HREE with high (La/Yb)N values (5.97 to 16.6) and a pro- create some uncertainties in calculating ISr values (e.g., Feng et al., nounced negative Eu anomaly (Fig. 7b). 2014; Jahn et al., 2009, 2004, 2000; Wu et al., 2002). Hence, discussion regarding source constrains of the granitoids is cen- 3.3 Zircon U-Pb Ages tered mainly on whole rock Nd isotope as well as major and trace The results of LA-ICP-MS U-Pb dating are presented in elements compositions. The 143Nd/144Nd in Guanzishan nepheline Table 3. Thirty zircon grains were analysed from Guanzishan syenite and alkaline granite are 0.512 544 and 0.512 521, respec- nepheline syenite (16SZ06-01) and another twenty-three zircon tively, while in Huangyangshan pluton the 143Nd/144Nd ranges grains from Huangyangshan quartz syenite (16SZ03-05). The from 0.512 544 to 0.512 66, respectively. The values of ɛNd(t) in zircons are generally pale yellow and transparent and are sub- Guanzishan nepheline syenite and alkaline granite are +1.81 and hedral to euhedral in shapes. However, some few zircons are +2.26, respectively and the calculated two-stage model age for colorless and prismatic in shape. The zircons range in sizes from these rocks are 1 040 and 1 003 Ma, respectively (Table 4). This

125 to 290 µm (Figs. 8a and 8b). They generally exhibit oscilla- ɛNd(t) is close to the values recorded from Wudang mafic dikes in tory zoning in CL images and have Th/U ratios ranging from 0.3 South Qinling (Table 4). On the other hand, the Huangyangshan to 0.9 typical of magmatic zircon (Belousova et al., 2002). Sam- alkaline granite has ɛNd(t) values ranging from +2.61 to +3.46 and ple 16SZ06-01 is nepheline syenite from Guanzishan and a total a relatively younger two-stage Nd model age values ranging from number of thirty zircon spots were analyzed from this sample. 906 to 975 Ma, respectively. They plot on a concordia diagram with a weighted mean 206Pb/238U age of 450±3 Ma (MSWD=2.5) (Figs. 8c and 8d). 4 DISCUSSION Sample 16SZ03-05 is a medium to coarse-grained quartz syenite 4.1 Genetic Affinity and Temporal Relationship from Huangyangshan. Results of analyses of eight zircon spots The mineralogical composition of the syenite-granites as- with low degree of discordance (less than 10%) from this sam- sociation from Suizhou-Zaoyang region, comprising of alkaline ple yielded 206Pb/238U ages varying from 430±6 to 456±9 Ma, amphiboles such as riebeckite, coupled with their significant and plot on a concordia diagram, with a weighted mean age of enrichment in high field strength elements such as Nb, Zr, Y, as 441±7 Ma (MSWD=1.5) (Figs. 8e and 8f). well as their high REE content (except Eu), when compared to S-type and I-type granitoids suggest that the granitoids are 3.4 Whole Rock Sr and Nd Isotopes typically syenite and A-type (e.g., Eby, 1992). Similarly, the Whole rock Sr and Nd data are presented in Table 4. The nepheline syenite associated with Suizhou-Zaoyang region

1190

Table 3 LA-ICP-MS zircon U-Pb data for the rocks from Guanzishan (16SZ06-03)

Spot No. Th (ppm)U(ppm) Th/U 207Pb/206Pb 1σ 207Pb/235U1σ 206Pb/238U 1σ 207Pb/206Pb (Ma) 1σ 207Pb/235U (Ma) 1σ 206Pb/238U (Ma) 1σ 1 182 232 0.8 0.056 6 0.002 0 0.563 2 0.017 8 0.072 3 0.000 9 476 78 454 12 450 5 2 308 298 1 0.055 0 0.001 8 0.550 3 0.017 1 0.072 1 0.000 8 413 72 445 11 449 5

3 359 337 1.1 0.055 2 0.001 9 0.549 1 0.016 7 0.072 0 0.000 7 417 78 444 11 448 4 Hafizullah Abba Ahmed,Changqian Ma 4 151 184 0.8 0.055 9 0.002 5 0.556 1 0.021 3 0.071 5 0.000 8 450 98 449 14 445 5 5 65.1 109 0.6 0.055 8 0.002 9 0.557 1 0.026 0 0.072 1 0.001 0 443 121 450 17 449 6 6 107 153 0.7 0.054 6 0.002 0 0.534 0 0.017 8 0.070 4 0.000 8 394 83 434 12 438 5 7 73.1 117 0.6 0.056 7 0.002 6 0.568 1 0.023 8 0.072 7 0.000 8 480 100 457 15 453 5 8 92.8 123 0.8 0.056 5 0.003 6 0.569 2 0.044 9 0.071 8 0.001 0 472 143 457 29 447 6 9 86.4 140 0.6 0.056 2 0.002 0 0.559 3 0.019 3 0.072 1 0.000 8 457 106 451 13 449 5 10 100 137 0.7 0.055 8 0.002 4 0.548 2 0.022 2 0.071 8 0.000 9 443 127 444 15 447 5 11 352 344 1 0.055 0 0.001 7 0.526 8 0.015 9 0.069 6 0.000 7 413 69 430 11 434 4 12 159 187 0.8 0.056 6 0.001 9 0.561 7 0.019 7 0.072 2 0.000 9 476 78 453 13 450 5 13 148 198 0.8 0.055 4 0.001 7 0.529 8 0.015 5 0.069 8 0.000 8 428 64 432 10 435 5 14 174 220 0.8 0.055 6 0.0019 0.549 6 0.018 2 0.072 2 0.000 8 435 71 445 12 449 5 , Lianxun Wang, Ladislav A.Palinka 15 299 291 1 0.055 8 0.001 8 0.560 9 0.017 7 0.073 2 0.000 8 456 74 452 12 456 5 16 186 242 0.8 0.055 5 0.001 8 0.546 0 0.017 0 0.071 6 0.000 9 435 69 442 11 446 5 17 243 254 1 0.056 1 0.001 7 0.556 0 0.014 9 0.072 4 0.000 8 457 65 449 10 451 5 18 116 160 0.7 0.056 3 0.002 1 0.555 5 0.019 7 0.072 4 0.000 9 465 79 449 13 450 5 19 98.1 136 0.7 0.057 2 0.001 8 0.591 8 0.018 3 0.075 4 0.000 8 498 70 472 12 469 5 20 169 219 0.8 0.055 7 0.001 7 0.549 9 0.015 9 0.072 0 0.000 8 443 67 445 10 448 5 21 84.5 129 0.7 0.054 9 0.002 2 0.541 3 0.022 3 0.071 3 0.000 8 406 92 439 15 444 5 22 476 423 1.1 0.056 5 0.001 5 0.564 1 0.013 7 0.072 6 0.000 6 472 57 454 9 452 3 23 421 365 1.2 0.055 3 0.001 4 0.549 7 0.013 5 0.072 1 0.000 6 433 56 445 9 449 3 24 145 177 0.8 0.057 5 0.001 7 0.574 5 0.017 6 0.072 6 0.000 9 509 67 461 11 452 5

25 223 253 0.9 0.055 5 0.001 6 0.557 1 0.016 6 0.072 8 0.000 7 432 65 450 11 453 4 š, Musa BalaGirei, and etal. 26 267 291 0.9 0.061 3 0.002 4 0.605 6 0.023 6 0.072 0 0.001 2 650 82 481 15 448 7 27 231 248 0.9 0.055 2 0.002 3 0.544 5 0.022 1 0.071 4 0.000 9 420 93 441 15 445 5 28 220 137 1.6 0.061 6 0.002 9 0.600 4 0.031 2 0.071 6 0.001 8 657 107 478 20 446 11 29 238 277 0.9 0.058 9 0.002 3 0.546 4 0.021 1 0.067 4 0.001 2 565 90 443 14 420 7 30 292 1 293 0.2 0.055 7 0.001 4 0.550 6 0.014 9 0.071 6 0.001 2 443 56 445 10 446 7

Petrogenesis and TectonicImpl

Table 3 Continued, LA-ICP-MS zircon U-Pb data for the rocks from Huangyangshan (16SZ05-03)

Spot No. Th (ppm) U (ppm) Th/U 207Pb/206Pb 1σ 207Pb/235U 1σ 206Pb/238U 1σ 207Pb/206Pb (Ma) 1σ 207Pb/235U (Ma) 1σ 206Pb/238U (Ma) 1σ 2 106 1 114 0.1 0.061 5 0.001 4 0.592 1 0.015 6 0.069 4 0.000 9 657 48 472 10 432 6 4 267 291 0.92 0.061 3 0.002 4 0.605 6 0.023 6 0.072 0 0.001 2 650 82 481 15 448 7 16 292 1 293 0.23 0.055 7 0.001 4 0.550 6 0.014 9 0.071 6 0.001 2 443 56 445 10 446 7 ications of Peralkaline A-Type Granites and Syenites 9 59.6 182 0.33 0.059 4 0.002 7 0.564 2 0.026 2 0.068 9 0.001 0 583 98 454 17 430 6 10 231 248 0.93 0.055 2 0.002 3 0.544 5 0.022 1 0.071 4 0.000 9 420 93 441 15 445 5 11 220 137 1.61 0.061 6 0.002 9 0.600 4 0.031 2 0.071 6 0.001 8 657 107 478 20 446 11 17 83.3 205 0.41 0.057 1 0.003 5 0.582 1 0.043 2 0.073 3 0.001 5 498 137 466 28 456 9 20 43.3 256 0.17 0.058 2 0.002 1 0.565 0 0.021 1 0.070 7 0.001 3 539 82 455 14 440 8

Table 4 Sr-Nd isotopic composition for Huangyangshan, Guanzishan and Wudang

147 144 143 144 Sample No. Rock type Pluton name Age (Ma) Rb Sr ISr Sm Nd Sm/ Nd Nd/ Nd εNd(t) T2DM (Ma) Reference (ppm) (ppm)

16SZ02-01 Quartz syenite Huangyangshan 441 112.34 3.91 0.727 3 9.21 46.5 0.112 2 0.512 55 +3.14 931 This study 16SZ03-05 Quartz syenite Huangyangshan 441 127.98 2.6 0.715 6 6.21 33.4 0.119 7 0.512 54 +2.61 975 This study 16SZ04-01 Quartz syenite Huangyangshan 441 123.44 7.27 0.713 5 11.4 53.9 0.112 2 0.512 57 +3.46 906 This study 16SZ05-03 Alkaline granite Guanzishan 450 56.411 43.7 0.719 8 9.77 47 0.125 6 0.512 54 +2.26 1 003 This study

16SZ06-01 Nepheline syenite Guanzishan 450 379.85 55.7 0.797 7 22 126 0.105 2 0.512 52 +1.81 1 040 This study WD12-01 Gabbro Wudang 460 4.05 300 0.706 6 5.72 23 0.150 5 0.512 60 +1.47 - Nie et al. (2016) WD12-02 Gabbro Wudang 460 4.52 301 0.706 4 5.7 22.73 0.151 6 0.512 60 +1.52 - Nie et al. (2016) WD12-04 Gabbro Wudang 460 3.28 229.7 0.707 0 7.24 28.85 0.151 7 0.512 60 +1.87 - Nie et al. (2016) WD12-07 Gabbro Wudang 460 7.51 317.3 0.707 6 7.55 30.35 0.150 3 0.512 60 +2.32 - Nie et al. (2016) WD12-11 Gabbro Wudang 460 11.1 322.3 0.704 3 6.28 26 0.144 8 0.512 60 +1.47 - Nie et al. (2016) WD12-15 Gabbro Wudang 460 1.55 535.1 0.705 3 6.32 26.32 0.145 2 0.512 60 +2.34 - Nie et al. (2016)

1191 1192 Hafizullah Abba Ahmed, Changqian Ma, Lianxun Wang, Ladislav A. Palinkaš, Musa Bala Girei, and et al.

Figure 3. BSE images for samples from Guanzishan amphiboles (a) and Huangyangshan quartz syenite (b), Huangyangshan alkaline granites (c)–(d), Guanzis- han alkaline granite (e), Guanzishan nepheline syenite (f). Fe-Fe-Win. Ferro-ferri-winchite; Rbk. riebeckite; Arf. arfvedsonite.

A-type suites is also characterized by high content of Zr, Y and association were emplaced between 450±3 and 441±7 Ma, re- REE (except Eu). According to Whalen et al. (1987) it is gener- spectively, which correspond to Late Ordovician to Early Silu- ally very difficult to distinguish A-type granite from highly frac- rian Period (Fig. 8). The LA-ICP-MS zircon U-Pb age of Huang- tionated I-type granitoids owing to the fact that the mineralogical yangshan determined in this study is quite similar to the and chemical composition of these two distinct granitoids could SHRIMP zircon age (439±6 Ma) determined by Ma et al. (2005). overlap. However, the characteristically high content of Ga/Al This age is however, significantly higher than the Rb/Sr isochron T T ratio, high Na2O+K2O and FeO (FeO +MgO) (Figs. 6a–6d) age of 215 Ma reported by Qiu (1993). further suggest that the granitoids under investigation are A-type (e.g., Wu et al., 2002) and nepheline syenites. Additionally, the 4.2 Magma Source granitoids are depleted in P2O5, Sr, Ba and Ti when compared to Peralkaline A-type granites and syenites generally form at typical S-type granitoids, which are always peraluminous. The anomalously higher temperature than other granitoids, which Guanzishan and Huangyangshan nepheline syenites and granites imply that mantle derived magmas generally play significant

Petrogenesis and Tectonic Implications of Peralkaline A-Type Granites and Syenites 1193 role in their genesis (e.g., Wu et al., 2002; King et al., 1997; Litvinovsky et al. (2000) has revealed that syenitic magmas can- Turner et al., 1992). In this respect, fractional crystallization of not form through melting of sialic crustal material even at pres- mantle derived magmas has been considered as important sures as high as 15 to 25 kbar. According to Litvinovsky et al. mechanisms for the genesis of peralkaline A-type granites and (2015), peralkaline granites and syenites characterized by high syenites (Litvinovsky et al., 2015; Shellnutt et al., 2009; Bonin, K2O and Na2O are generally derived from K-rich basaltic or 2007; Shellnutt and Zhou, 2007; King et al., 1997; Turner et al., andesitic magmas with negligible crustal input. 1992). However, peralkaline A-type granitoids are generally Elements Nb, Ta and Ti have useful application in differ- characterized by anomalous enrichment of HFSE as well as entiating crustal derived rocks from rocks that formed from REE, which is the hallmark of rock derived from enriched/ metasomatised mantle (Shellnutt et al., 2011; Bonin, 2007; 2.2 Huangyangshan Upton et al., 2003; Eby, 1992, 1990; Sutcliffe et al., 1990). (a) 2.0 Guanzishan Nonetheless, models involving partial melting of sialic crustal materials and/or fusion of crustal materials modified by en- 1.8 Calc-alkaline & strongly peraluminous richment of LILE and volatiles at higher pressure have also been 2 2 proposed for the origin of peralkaline A-type granitoids (Martin, 1.6 2006; Lubala et al., 1994). For instance, Collins et al. (1982) 1.4 argued that A-type granite could be derived through partial melt- ing of chemically depleted (restitic) lower crustal sources. How- 1.2 Alkaline

ever, A-type granites derived through the above process are gen- 23

erally peraluminous rather than peralkaline in composition (e.g., (Al O +CaO)/(FeOt+Na O+K O) 1.0

Martin, 2006). Alternatively, Martin (2006) proposed a model SiO2 >68 wt.% involving melting of “fenitized” lower crustal source for the 0.8 0 24681012 formation of A-type granite. But experiment carried out by 100(MgO+FeOt+TiO22 )/SiO 7 2 (b) (a) 6 Huangyangshan quartz syenite Huangyangshan alkaline granite Alkali Guanzishanalkaline granite 5

4 Metaluminous Peraluminous

A/NK Na-Ca 3

BNa 2 Fe-Mg-Mn 1 Peralkaline Calcic 0 0.6 0.8 1.0 1.2 1.4 A/CNK 0 023 000 BCa+BNa 1.0 (c) (b) 2 500 Ultrmafic rock 0.9 Melteigite 2 000 Ijolite 0.8 f Theralite Gabbro-norite Low O2 Alkali gabbro 1 500 Gabbro Essexite Gabbro- Syeno- 0.7 gabbro diorite Syeno- Monzo- gabbro f diorite Diorite 2+ 2+ 2+ Intermediate O2

R2=6Ca+2Mg+Al

1 000 diorite

nite Monzo-

Fe /(Fe +Mg ) 0.6 Monzo- Quartz Tonalite Nepheline syenite monzonite Granodiorite 0.5 High f 500 Syenite Quartz Granite O2 syenite Alkali granite 0.4 0 0.0 0.1 0.2 0.3 0.4 0.5 0.6 0.7 0.8 0.9 1.0 -1 000 0 1 000 2 000 3 000 IV Al (apfu) R1=4Si–11(Na+K)–2(Fe+Ti)

Figure 4. (a) Chemical composition of analysed amphiboles plotted on BNa Figure 5. (a) (Al2O3+CaO)/(FeO+Na2O+K2O) vs. 100(MgO+FeO+TiO2/SiO2 vs. BCa+BNa diagram after Hawthorne (1981); (b) Fe2+/(Fe2++Mg2+) vs. for the studied samples (Sylvester, 1989). (b) A/CNK vs. A/NK diagram (after AlIV discrimination diagram of Anderson and Smith (1995) based on am- Shand, 1943). (c) R1-R2 discrimination diagram for studied alkaline granitoids phibole chemistry of the studied alkaline granitoids. (De la Roche et al., 1980).

1194 Hafizullah Abba Ahmed, Changqian Ma, Lianxun Wang, Ladislav A. Palinkaš, Musa Bala Girei, and et al.

(a) (b) 100 100

A 10 A

Y (ppm)

22 10 I & S

(Na O+K O)/CaO I & S Huangyangshan Guanzishan 1 1 1 310201 31020 10 000×Ga/Al 10 000×Ga/Al 16 1.0 (c) (d) 12 Alkalic 0.9

8 0.8 Ferroan

4 A-type granites 0.7 Magnesian

22 0 Alkali-calcic TT 0.6

Na O+K O-CaO Calc-alkalic FeO /(FeO +MgO) -4 0.5 Calcic -8 0.4 50 55 60 65 70 75 80 50 55 60 65 70 75 80 SiO2 SiO2

Figure 6. (a) 10 000×Ga/Al vs. (Na2O+K2O)/CaO diagram (after Whalen et al., 1987), (b) 10 000×Ga/Al vs. Y diagram (after Whalen et al., 1987), (c) T T (Na2O+K2O-CaO) vs. SiO2 (wt.%), (d) FeO /(FeO +MgO) vs. SiO2 (wt.%) (Frost et al., 2001).

1 000 1 000 (a) (b)

100 100

10

Rock/chondrite 10 Huangyangshan Gaotan

Sample/primitive mantle 1 Guanzishan E-MORB Ziyang-Zhenba N-MORB Alkaline granitoids OIB from South Qinling 0.1 1 Rb Th Nb K Ce Pr P Zr Sm Ti Tb La Pr Sm Gd Dy Er Yb Ba U Ta La Pb Sr Nd Hf Eu Gd Dy Ce Nd Eu Tb Ho Tm Lu 100 100 Huangyangshan (c) Guanzishan (d) Guanzishan Huangyangshan Ziyang diabase Mogou Sandaogou Sandaogou Mogou Gaotan diabase 10 10 Ziyang mafic rocks IAB IAB

Yb/Ta

Ce/Nb

1 OIB 1 OIB

0.1 0.1 0.1 1 10 0.1 1 10 Y/Nb Y/Nb

Figure 7. (a) Primitive-mantle normalized trace element spider diagrams (after Sun and McDonough, 1989) and (b) chondrite-normalized REE patterns (after Sun and McDonough, 1989) of the studied alkaline granitoids from Guanzisahn, Huangyangshan and some published data; (c) Yb/Ta vs. Y/Nb (after Eby, 1992, 1990); (d) Ce/Nb vs. Y/Nb (after Eby, 1992, 1990). Published data including Ziyang-Zhenba and Gaotan mafic rocks are from Wang et al. (2017); Cao L et al. (2015); Zhang (2010); Zhang et al. (2010); and Ma et al. (2005).

Petrogenesis and Tectonic Implications of Peralkaline A-Type Granites and Syenites 1195

Figure 8. Representative CL images of zircon grains from Guanzishan (a) and Huangyangshan (b); LA-ICP-MS zircon U-Pb concordia for Guanzishan (c) and Huangyangshan (d); mean weighted average for Guanzishan (e) and Huangyangshan (f). mantle magmas as well as in tracing contamination of mantle Y/Nb and Y/Ta ratio <2 are typical of A-type suites that are derived rocks via crustal assimilation (e.g., Wang et al., 2017; commonly considered as derivatives of enriched OIB mantle Niu and OʼHara, 2009). This stem from the fact that rocks that sources (Bonin, 2007; Eby, 1992, 1990). Similarly, ratios of formed from melting of crustal material generally showed sig- some LILE and HFSE such as Th/Ta, Th/Nb, Rb/Nb, Ba/Nb nificant depletion in Nb, Ta, and Ti when compared to rocks generally reflect the source materials from which igneous rock that formed from mantle derived magmas (e.g., Niu and were derived (e.g., Shellnutt et al., 2009). This is because these OʼHara, 2009; Rudnick and Gao, 2003; Taylor and McLennan, trace elements remain largely immobile throughout the course 1985; Taylor, 1977). This suggests a genetic link between the of magmatic differentiation (Wang et al., 2017; Shellnutt et al., formation of continental crust and subduction related (island 2009; Shellnutt and Zhou, 2007). Binary plots of these trace arc) magmatism (Taylor and McLennan, 1985; Taylor, 1977). element ratios revealed that the peralkaline granites of both The absence of negative Nb and Ta anomalies in peralkaline Guanzishan and Huangyangshan plutons were largely derived granites and syenites from both Guanzishan and Huangyang- from an enriched mantle sources (Figs. 9a–9e). Typically, man- shan is therefore inconsistent with rocks derived from melting tle derived rocks generally have lower Th/Ta ratio≈2 compared of crustal sources. Negative Ti anomalies in these rocks point to upper crust (Th/Ta≈6.9) or lower crust (Th/Ta≈7.9) (Shell- to magmatic evolution involving the fractionation of horn- nutt et al., 2009; Rudnick and Gao, 2003). The average Th/Ta blende and Fe-Ti oxide. The geochemical characteristics of the values obtained from the samples of peralkaline granitods are syenites and granites such as their high K2O and Na2O and low approximately 2 (Fig. 9c), which further suggests that the per-

1196 Hafizullah Abba Ahmed, Changqian Ma, Lianxun Wang, Ladislav A. Palinkaš, Musa Bala Girei, and et al. alkaline granitoids were most likely derived from the mantle. Importantly, the peralkaline nature of the rocks coupled with

Furthermore, the peralkaline Guanzishan pluton yielded the ɛNd(t) their OIB-like geochemical characteristic (Figs. 7 and 9) are also values ranging from +1.81 to +2.26 (Table 4). These slightly compatible with rocks that were derived from enriched mantle positive ɛNd(t) values suggest an origin from enriched mantle sources (Shellnutt et al., 2009; Bonin, 2007; King et al., 1997; source (e.g., Feng et al., 2014; Jahn et al., 2009; Winter, 2001). Eby, 1992). Additionally, the high K2O content in the granitoids

600 10

(a) Arc volcanics (b) Guanzishan Huangyangshan 100 8 Mogou Sandaogou Gaotan diabase UC Ziyang mafic rocks Dupal 6 10 OIB E-MORB OIB PM CC average

Ba/Nb

Rb/Nb 4 OIB LC MORB Guanzishan 1 Huangyangshan Mogou N-MORB 2 Sandaogou Gaotan Diabase Ziyang mafic rocks 0.1 0 0.1 1 10 20 0 123 4 56 La/Nb La/Nb 8 0.6 (c) LC (d) LC Guanzishan UC Huangyangshan 0.5 Mogou Guanzishan Sandaogou 6 Huangyangshan UC Gaotan diabase Mogou 0.4 Ziyang mafic rocks Sandaogou OIB Gaotan diabase N-MORB 4 Ziyang mafic rocks 0.3

Th/Ta E-MORB OIB

Th/Nb E-MORB N-MORB 0.2 2 0.1

0 0.0 0 102030405060708090100 0 102030405060 Ba/Nb Ba/La 7 60 (e) (f) Guanzishan Guanzishan 6 Huangyangshan 50 Huangyangshan Mogou Mogou 5 Sandaogou Sandaogou Gaotan Diabase 40 Gaotan Diabase 4 Ziyang mafic rocks E-MORB 30 Ziyang mafic rocks

La/Nb N-MORB 3 (La/Yb)N OIB OIB LC 20 OIB E-MORB 2 UC 10 1 N-MORB E-MORB N-MORB 0 0 0 5 10 15 20 25 30 35 0 50 100 150 200 250 Zr/Nb Y (ppm)

Figure 9. Trace element ratio comparison of the Guanzishan and Huangyangshan nepheline syenites and A-type granitoids with other alkaline granitoids and mafic rocks in the region, showing fields of upper crust, lower crust, OIB, N-MORB and E-MORB. UC. Upper crust; LC. lower crust (Shellnutt et al., 2009; Wedepohl, 1995); N-MORB. normal mid-ocean ridge basalt; E-MORB. enriched mid-ocean ridge basalt; OIB. ocean-island basalt (data from Sun and McDonough, 1989).

Petrogenesis and Tectonic Implications of Peralkaline A-Type Granites and Syenites 1197

(a) tive or silica oversaturated quartz-normative evolved magmas. Huangyangshan Amphibole group minerals play an important role in en- Guanzishan suring transition from SiO2 undersaturated to SiO2 saturated Wudang mafic dikes melt (Martin, 2007). Amphiboles in the syenites and peralka- line granites investigated show variation from sodic-calcic to sodic in composition (Fig. 4a). The absence of SiO poor calcic -25 -20 -15 -10 -5 0 +5 2 ε t Nd() amphiboles implies that they were removed from depth to form 100 a cumulate (Papoutsa and Pe-Piper, 2014; Martin, 2007; Giret (b) et al., 1980). The presence of nepheline normative syenite in Guanzishan pluton suggests that this rock probably formed EM1 from fractional crystallization of mafic magmas. Similarly, the HIMU EM2 variation in amphibole composition from riebeckite to arfved- sonite in Huangyangshan quartz syenite and granite which is Nb/U marked by decreasing CaO, MgO and Mg# contents and in-

creasing SiO2 (Table 2), is typical of magma evolution through 10 Continental crust fractional crystallization (Pe-Piper, 2007; Giret et al., 1980). Plot of Fe2+/(Fe2++Mg2+) vs. Al show that the rocks were formed under the condition of low oxygen fugacity (Fig. 4b), -30 -25 -20 -15 -10 -5 0 +5 +10 ε t which is typical of amphiboles found in A-type granites (Pa- Nd() +12 poutsa and Pe-Piper, 2014). +8 (c) Wang et al. (2017) established a genetic link between mafic, Depleted mantle +4 ultramafic and nepheline synenite in Guanzhishan via a liquid CHUR 0 line of decent involving fractional crystallization and/or assimila- tion fractional crystallization (AFC) of OIB mantle derived

t -4

()

Nd magmas. By contrast, we obtained an average U/Pb age of 450 ε -8 Huangyangshan Ma from Guanzishan nepheline syenite which is slightly older -12 Guanzishan than the age of mafic rocks (Gaotan diabase 440 Ma and Ban- -16 Wudang jiuguan gabbro 439 Ma) as reported by Wang et al. (2017) and a -20 little younger than the Wudang mafic dikes 460 Ma (Nie et al., -24 2016). Apart from that, the Guanzhishan nepheline syenites are 200 300 400 500 600 700 800 900 1 000 geochemically more enriched in K O than the Gaotan diabase Age (Ma) 2 (Fig. 7a). This further negates the hypothesis involving the deri- Figure 10. (a) Comparison of εNd(t) values between Huangyangshan and vation of geochemically more evolved nepheline syenite magmas Guanzishan after Zhang et al. (2018); (b) Nb/U plot against εNd(t) from from fractional crystallization of the original mafic magma from Hofmann (1997); (c) εNd(t) vs. age diagram for Huangyangshan and Guan- which the Gaotan diabase was formed. This is because fractional zishan after Condie (2007). Isotopic data for mafic intrusions from Wudang crystallization that resulted in strong Ba depletion (Fig. 7a) in- mafic dikes near the study area (Nie et al., 2016) are shown for comparison. volving either K-feldspar or biotite fractionation is expected to

have resulted in K2O depletions in Guanzhishan nepheline is consistent with rocks derived from EM mantle sources (Jack- syenites relative to Gaotan diabase. On the contrary, K2O is even son and Daskupta, 2008). In the plots of ɛNd(t), Nb/U vs. ɛNd(t) more enriched in nepheline syenites and granites than in Gaotan and ɛNd(t) vs. age (Ma), peralkaline granitoids from Guanzishan diabase. More so, the possibility of crustal assimilation that could and Huangyangshan both plot in the field of EM2 mantle de- lead to increase in K2O in Guanzhishan nepheline syenites and rived rocks (Figs. 10a, 10b and 10c). peralkaline granitoids from Huangyangshan pluton has also been

ruled out based on both trace element and ɛNd(t) data. The mean 4.3 Petrogenesis U/Pb age obtained from Huangyangshan (441 Ma) is consistent Fractional crystallization of alkaline transitional or theolitic with the 440 to 439 Ma peak of alkaline magmatism in Gaotan basalt with minimal or no crustal assimilation have been pro- diabase and Banjiuguan gabbro, respectively (Wang et al., 2017). posed as the main petrogenetic processes that give rise to peral- We therefore infer that the Guanzhishan nepheline syenites and kaline alkali-calcic to alkali granite and syenite (Frost and Frost, granites were formed from fractional crystallization of OIB-like 2011; Eby, 1992, 1990; Loiselle and Wones, 1979). The positive basic magmas derived from upwelling of metasomatized litho- ɛNd(t) values in nepheline syenites and alkaline granites from spheric mantle during the Late Ordovician extension. The em- Guanzishan and Huangyangshan plutons indicate that they placement of such granitoids was probably controlled by some probably formed from fractional crystallization of basic magmas. deep seated fault and/or shear zones. The Huangyangshan quartz In this respect, significant depletion in Ba, Sr, P, Ti and Eu indi- syenite and granite on the other hand probably formed from up- cate fractionation of feldspars, biotite, apatite, amphiboles and welling and subsequent assimilation fractional crystallization of Ti-rich augite. According to Barker (1987), fractionation of oli- enriched aesthenospheric mantle derived magmas. The formation vine, Ti-rich augite and plagioclase from an alkaline basic of these granitoids therefore marked the main period of rifting in magma can give rise to silica-undersaturated nepheline norma- the Early Silurian, which facilitated significant mantle upwelling

1198 Hafizullah Abba Ahmed, Changqian Ma, Lianxun Wang, Ladislav A. Palinkaš, Musa Bala Girei, and et al.

(e.g., Ma et al., 2005). This period also marked the peak of mag- (Eby, 1992). Additionally, the ferroan and alkalic features of matism in South Qinling (Wang et al., 2017). the granitoids (Figs. 6c and 6d) are also typical of granitoids of the A1 group (e.g., Dall’Agnoll et al., 2012), which are notably 4.4 Tectonic Implication different from A2 granite that are generally alkali-calcic. Simi- A-type granitoids are generally emplaced in extensional larly, coeval mafic rocks and some younger perakaline suites environment: post-collisional or anorogenic (Bonin, 2007; Wu with similar chemical composition from Mogou and San- et al., 2002; Eby, 1992, 1990; Whalen et al., 1987). In a broad daogou also plot within the field typical of OIB derived rock. sense, Eby (1992, 1990) subdivided A-type granite into two We therefore infer that peralkaline granitiods from Suizhou- major groups: namely, A1 and A2 based on their peculiar trace Zaoyang region and some plutons with comparable composi- element compositions especially their Nb/Y ratio and Nb-Y-Ce tion such as Mogou and Sandaogou were mainly derived from contents. According to the authors, the A1 subgroups are prod- OIB magmas with low contribution from ancient crustal ucts of fractional crystallization of basaltic magmas derived sources. These rocks are linked directly with the coeval mafic from OIB related sources and are generally emplaced in anoro- rocks in the area (e.g., Wang et al., 2017). Previous studies genic setting such as continental rift or intraplate settings (e.g., (e.g., Wang et al., 2017; Ma et al., 2006, 2005, 2004) have Eby, 1992). The A2 groups on the other hand are associated revealed that the Dabie orogenic belt has experienced complex with post-collisional or post-orogenic settings and are generally tectonic history especially during the Late Ordovician to Late derived from subcontinental lithosphere or lower crust. Without Cretaceous periods. During the Early Paleozoic, while the sub- exception, the peralkaline syenites and alkaline granites from duction of the ancient ocean was taking place towards the south Suizhou-Zaoyang region plot within the A1 field (Figs. 11a and (Fig. 12), concurrently, the northern margin of Yangtze Craton 11b). Typically, all the granitoids from Suizhou-Zaoyang re- began to break (Xu et al., 2008; Ma et al., 2005), resulting into gion plot within the same field in Pearce et al. (1984) tectonic back arc extension in the southern fringe of Qinling-Dabie (Ma et discrimination diagram (Figs. 11c and 11d) which implies that al., 2006). The products of magmatisms that resulted from the they are within plate anorogenic granites associated with subduction of this ancient Qinling Plate in the north and the sub- crustal extension and/or rifting. Importantly, the granitoids sequent back arc extension/rifting from the south (Fig. 12) are have Y/Nb and Y/Ta ratio <2 (Fig. 7c) which further suggest considered as typical example of “paired magmatic belts” (Ma et that they were mainly derived from O1B related mantle sources al., 2006). This short period of extension and subsequent rifting

Nb Nb

(a) (b)

A1 A1

A2 A2

Y Y 3×Ga Ce

1 000 (c) 1 000 (d) WPG Syn-COLG WPG 100 100

VAG+

Nb (ppm)

Rb (ppm) syn-COLG VAG ORG 10 ORG 10

Huangyangshan Guanzishan 1 1 1 10 100 1 000 1 10 100 1 000 Y (ppm) Y+Nb (ppm)

Figure 11. (a) The ternary plots Nb-Y-3×Ga of A-type granite for the studied alkaline granitoid samples (after Eby, 1992); (b) ternary plots Nb-Y-Ce (Eby, 1992); (c) Rb vs. Y diagram (after Pearce et al., 1984); (d) Nb vs. Y+Nb diagram (after Pearce et al., 1984).

Petrogenesis and Tectonic Implications of Peralkaline A-Type Granites and Syenites 1199

Figure 12. Sketched model showing the tectonic setting of the Guanzishan nepheline syenites and Huangyangshan A-type granites within the Suizhou-Zaoyang region (modified after Ma et al., 2006). prompted the emplacement of A-type granites (Wang et al., 2017; peralkaline syenites and alkaline granites from Suizhou- Ma et al., 2005). Extension during the Late Ordovician triggered Zaoyang region exhibit A1-type granite affinity with all the the upwelling of small volume of metasomatized lithospheric granitoids from the studied region plotting in within plate gran- OIB-like melt (e.g., Wang et al., 2017). The Guanzishan ite in the tectonic discrimination diagram, which imply that nepheline syenite and A-type granite formed from the evolved they are within plate anorogenic granites associated with the fraction of these melts (Fig. 12). The emplacement of these rocks Ordovician crustal extension and Silurian rifting. was probably controlled by some deep-seated fault/shear zones. Extension and subsequent rifting continued into Early Silurian ACKNOWLEDGMENTS Period (Ma et al., 2006, 2004). This period facilitated the upwell- Professor Changqian Ma has received long-term guidance ing of metasomatized asthenosphere-derived OIB sources and and mentorship from Prof. Zhendong You, which is highly appre- the emplacement of mafic rocks such as the Gaotan diabase (Fig. ciated. We also acknowledge the support from the National Natu- 7). The Huangyangshan peralkaline quartz syenites and alkaline ral Science Foundation of China (No. 41502046), partial financial granites probably formed from the same mafic magma through support by the China Geological Survey (No. DD20160030), and assimilation fractional crystallization (Fig. 12). the Fundamental Research Funds for the Central Universities, China University of Geosciences, Wuhan (No. CUGCJ1711) are 5 CONCLUSION also acknowledged. We also thank Prof. Bernard Bonin and two Peralkaline A-type granitoids and nepheline syenites were anonymous reviewers whose painstaking reviews have signifi- episodically emplaced in Suizhou-Zaoyang region between cantly improved this work. The final publication is available at 441±7 and 450±3 Ma, which corresponds to Early Silurian and Springer via https://doi.org/10.1007/s12583-018-0877-2. Late Ordovician periods, respectively. All the A-type suites and nepheline syenites showed affinity for within plate setting REFERENCES CITED hence, they are anorogenic senso-stricto. The emplacement of Anderson, J. L., Smith, D. R., 1995. The Effects of Temperature and fO2 on the granitoids marked important periods of extensions and/or the Al-in-Hornblende Barometer. American Mineralogist, 80(5/6): rifting from Late Ordovician to Early Silurian periods. Geo- 549–559. https://doi.org/10.2138/am-1995-5-614 chemical and isotopic evidences suggest that these peralkaline Barker, D. S., 1987. Tertiary Magmatism in Trans-Pecos Texas. In: Fitton, J. syenites and granites originated from fractional crystallization G., Upton, B. G. J., eds., Alkaline Igneous Rocks. Geological Society and/or assimilation fractional crystallization of enriched OIB- Special Publication, 30: 415–431 like mantle sources. We therefore conclude that the peralkaline Belousova, E. A., Griffin, W., OʼReilly, S. Y., et al., 2002. Igneous Zircon: syenites and granites in Suizhou-Zaoyang region and by exten- Trace Element Composition as an Indicator of Source Rock Type. sion those within the Qinling orogenic belt and NCC, with Contributions to Mineralogy and Petrology, 143(5): 602–622. parallel geochemical characteristics e.g., the Sandaogou and https://doi.org/10.1007/s00410-002-0364-7 Mogou syenites were largely derived from OIB magmas which Bonin, B., 2007. A-Type Granites and Related Rocks: Evolution of a Con- originated from enriched aesthenospheric and lithospheric man- cept, Problems and Prospects. Lithos, 97(1/2): 1–29. tle with minor contribution from older continental crust mate- https://doi.org/10.1016/j.lithos.2006.12.007 rial. These A-type suites and nepheline syenites are co-genetic Bowden, P., 1985. The Geochemistry and Mineralization of Alkaline Ring with coeval mafic rocks in the area. Episodic extension and/or Complexes in Africa (a Review). Journal of African Earth Sciences, rifting triggered significant asthenospheric mantle upwelling 3(1/2): 17–39. https://doi.org/10.1016/0899-5362(85)90020-x and subsequent mixing with lithospheric mantle sources. The Cao, L., Zhang, Q. X., Hu, S. J., et al., 2015. LAICP-MS Zircon U-Pb Age

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