Geochemistry and geochronology of ore-bearing and barren intrusions in the Luanchuan ore fields of East Qinling metallogenic belt, China: Diverse tectonic evolution and implications for mineral exploration

Accepted Manuscript Geochemistry and geochronology of ore-bearing and barren intrusions in the Luanchuan ore fields of East Qinling metallogenic belt, China: Diverse tectonic evolution and implications for mineral exploration Fei Xue, Gongwen Wang, M. Santosh, Fan Yang, Zhiwei Shen, Liang Kong, Nana Guo, Xuhuang Zhang PII: DOI: Reference:

S1367-9120(17)30205-5 http://dx.doi.org/10.1016/j.jseaes.2017.04.027 JAES 3063

To appear in:

Journal of Asian Earth Sciences

Received Date: Revised Date: Accepted Date:

16 February 2017 23 April 2017 25 April 2017

Please cite this article as: Xue, F., Wang, G., Santosh, M., Yang, F., Shen, Z., Kong, L., Guo, N., Zhang, X., Geochemistry and geochronology of ore-bearing and barren intrusions in the Luanchuan ore fields of East Qinling metallogenic belt, China: Diverse tectonic evolution and implications for mineral exploration, Journal of Asian Earth Sciences (2017), doi: http://dx.doi.org/10.1016/j.jseaes.2017.04.027

This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain.

Geochemistry and geochronology of ore-bearing and barren intrusions in the Luanchuan ore fields of East Qinling metallogenic belt, China: diverse tectonic evolution and implications for mineral exploration

Fei Xuea, Gongwen Wanga *, M. Santosha, d, Fan Yanga, Zhiwei Shena, Liang Kongc, Nana Guob, Xuhuang Zhangb

a

School of Earth Sciences and Resources, China University of Geosciences

Beijing, 29 Xueyuan Road, Beijing 100083, China b

Luanchuan Bureau of Geology and Resources, Luoyang 417500, China

c

Hunan Institute of Geological Survey, Changsha 410116, China

d

Department of Earth Sciences, University of Adelaide, SA 5005, Australia

First author, E-mail address: [email protected]; *Corresponding author e-mail address: [email protected]

Abstract The Luanchuan ore fields form part of the East Qinling metallogenic belt in central China. In this study, we compare two ore-bearing intrusions, the

Shibaogou granitic pluton (SBG) and the Zhongyuku granitic pluton (ZYK), with the ore-barren Laojunshan intrusion (LJS) from the Luanchuan ore field. Geochemically, all the three intrusions are characterized by high-Si, high-K, and alkalis, together with moderate-ASI, exhibiting I-type granite features. The rocks, especially the ore-related plutons also show enrichment in LREEs. Mineral chemistry of biotite from the intrusions exhibits similar features of high Si and Mg, and low Al and Fe. Zircon grains from the ZYK intrusion yielded a U-Pb age of 149.6±2.4 Ma. The zircon grains show εHf (t) values and two stage model ages (TDM2) in the range of-16.8 to -19.7 and 1998 to 2156 Ma respectively. The biotite composition and Hf isotopic data indicate that the magma was derived by re-melting of deep crustal material with minor input of mantle

components.

We

evaluate

the

results

to

understand

the

physico-chemical conditions, petrogenesis, and tectonic setting, and their implications for mineral exploration. The ore-bearing plutons show wide ranges of temperature and oxygen fugacity, favoring Mo-W mineralization. In addition, estimates on pressure and depth of emplacement suggest that lower solidification pressure in a decompressional setting contributed to the evolution of magmatic hydrothermal deposits. Our data suggest that the ZYK has the highest potential for Mo-W mineralization. The ore-bearing plutons of ZYK and SBG were formed in a transitional tectonic setting from compression to extension, with the large-scale metallogeny triggered by slab melts at ca.145 Ma. However, the ore-barren LJS batholith formed in an extension-related geodynamic setting at ∼115 Ma. Our study shows that different tectonic settings and consequent physico-chemical conditions dictated the ore potential of the intrusions in the Luanchuan ore district.

Keywords: Mineral chemistry; Geochemistry; Zircon U–Pb geochronology and Hf isotopes; Tectonic model; Mineral exploration

1. Introduction The Luanchuan ore district forms part of the East Qinling metallogenic belt that hosts world-class Mo mineralization distributed along the southern margin of the North China Craton. This ore field is among the largest Mo-W-Pb-Zn-Ag polymetallic ore deposits in China (Mao et al., 2011; Li et al., 2012b; Han et al., 2013; Li et al., 2013; Bao et al., 2014; Gao et al., 2015; Li et al., 2015). Previous studies in this region evaluated the types of deposits, metal source and theirs genesis and classified the ores as skarn and porphyry-skarn (Qi et al., 2009; Duan et al., 2011; Xiang et al., 2012; Yang et al., 2013; Zhang, 2014; Cao et al., 2014; Yang et al., 2016). The Luanchuan ore district can be mainly divided into two ore fields, one within the northern Nannihu ore field, and the other in the southern Yuku ore field, together constituting the Luanchuan polymetallic system (Zhang, 2014; Tang et al., 2014; Cao et al., 2015). Some researchers have also attempted 3D geological models to assess the mineral potential based on data from multidisciplinary studies (Wang et al., 2011; Wang et al., 2012; Wang et al., 2015; Li et al., 2016). The Luanchuan ore deposits are considered to be related to deep-sourced granitic plutons which were emplaced at hypabyssal settings during the Late Jurassic- Early Cretaceous, including Nannihu, Shangfanggou, Shibaogou, Yuku and Huangbeiling intrusions. Several studies have addressed the geochemical, geochronological and isotopic features of the of the granitoids, and their relationship with ore mineralization (Bao et al., 2009; Li et al., 2012a; Xu et al., 2013; Bao et al., 2014; Zhang, 2014; Tang et al., 2014; Cao et al., 2015; Li et al., 2015; Zhang et al., 2015). The Luanchuan polymetallic system is mainly associated with the Late Jurassic- Early Cretaceous granitic plutons. A systematic distribution of porphyry-skarn Mo-W deposits, skarn-hydrothermal Zn deposits and hydrothermal-vein Pb-Zn-Ag deposits outwards from the contact zone with granitic plutons has been identified (Cao et al., 2015; Li et al.,

2015). The Laojunshan batholith located to the south of these deposits is ore-barren (Meng, 2010). Although previous studies have reported the general geochemical features of the Laojunshan batholith and some other ore-bearing plutons (Li et al., 2012a), detailed mineral chemical and isotopic data are still lacking. The compositional features, degree of fractional crystallization, and oxidation state are important indicators for mineral exploration of magmatic-hydrothermal deposits associated with granitoids (Blevin, 1992, 1995, 2004; Zhu et al., 2012; Zhu, 2014). The structure and chemical composition of mafic silicate minerals in magmatic suites have been used to derive the physical-chemical conditions of host magma (Borodina et al., 1999). Biotite is one of the most common mafic minerals occurring in granitoids, and previous studies have shown that the chemical composition of biotite can effectively trace the degree of magma differentiation, physico-chemical conditions, and tectonic setting (Jacobs and Parry, 1979; Speer, 1984; Lalonde and Bernard, 1993; Borodina et al., 1999; Aydin et al., 2003; Henry, 2005; Uchida et al., 2007; Kumar and Pathak, 2010). The chemistry of biotite is also a good indicator for mineral exploration (Dong et al., 2011; Tao et al., 2015; Xu et al., 2015; Tao et al., 2015). In this study, petrology, mineral chemistry, zircon U-Pb geochronology and isotope geochemistry are employed to understand the relationship between the ore-barren LJS batholith and ore-related Zhongyuku and Shibaogou granitic plutons, as well as to identify the salient indicators for mineral exploration. We analyse the physico-chemical conditions (including redox state,

temperature

and

pressure),

compositional

features,

evolution,

petrogenesis and tectonic setting to evaluate the metallogenic potential in Luanchuan ore district.

2. Geological setting The Central China orogenic belt which is located between the North China Craton and the Yangtze Craton comprises West Kunlun, Qilian, West Qinling, East Qinling, Dabie and Sulu (Pirajno, 2013; Bao et al., 2014; Yang et al., 2013; Yang et al., 2016; Dong and Santosh, 2016) (Fig. 1a). The Qinling orogen which includes the early Paleozoic North Qinling belt and the Triassic South Qinling belt underwent a long-term and multistage evolution (Zhang et al., 2001; Dong et al., 2011; Tang et al., 2015; Cao et al., 2015; Dong and Santosh, 2016) (Fig. 1b). The East Qinling orogenic belt shows typical features of a craton margin (Feng et al., 2005) and is composed of the Precambrian Huaxiong block and North Qinling belt, separated by the Luanchuan fault. The southern margin and northern margin of the East Qinling orogenic belt are marked by the Shangdan fault and the Sanbao fault respectively (Fig. 1b). The Middle Proterozoic Guandaokou Group, the Upper Proterozoic Luanchuan Group, Taowan Group, and the Neoproterozoic Kuanping Group are the main exposed strata in the Luanchuan ore district (Fig. 1c). The Guandaokou

Group

is

composed

of

fluvial-neritic

facies

rocks,

clastic-carbonate rocks and carbonate rocks containing stromatolites. From bottom to top, the Guandaokou Group consisted of the Gaoshanhe, Longjiayuan, Xunjiansi, Duguan, Fengjiawan and Baishugou Formations. The Luanchuan Group unconformably overlies the Guandaokou Group (Fig. 1c). The Luanchuan Group is composed of medium- to low-grade metamorphic neritic clastic and carbonate rocks and includes the Sanchuan, Nannihu, Meiyaogou, Dahongkou and Yuku Formations from bottom to top. The Luanchuan Group is unconformably overlain by Taowan Group which is made up metamorphic siltstone, quartzite, phyllite, conglomerate and argillaceous marble. Ores often occur in the Luanchuan Group (Yan and Liu, 2004; Wang et al., 2015).

The tectonic framework in the Luanchuan ore district shows a network structure of mainly WNW-ESE-trending faults and earlier NE-trending faults. The E-W-trending faults are the most common ones, with secondary NE-SW-trending faults (Fig. 1c). The network structure controls the distribution of small acid-intermediate plutons, and are the ore-bearing structures for vein-type Pb-Zn deposits (Li et al., 2012a). Magmatic suites in the Luanchuan ore district comprise Neoproterozoic gabbro dykes and late Jurassic-early Cretaceous granites. The meta-gabbro dykes show zircon SHRIMP U–Pb age of ca. 830 Ma, representing their emplacement age (Wang et al., 2011). Small-scale stocks, dikes, and pipes formed during the Jurassic, whereas large-scale batholiths were emplaced during the Cretaceous. The late Jurassic-early Cretaceous granites are most likely associated with the large-scale lithospheric thinning beneath the North China Craton (Mao et al., 2008; Li et al., 2012a; Li et al., 2012b; Santosh, 2013; Zhai and Santosh, 2013; Guo et al., 2013; Cao et al., 2015). The intrusions of ore-bearing porphyries at the center of the Nannihu and the Yuku ore fields intruded the Guandaokou and Luanchuan Groups, and occur as small, hypabyssal complex stocks (Fig. 2). The location of these porphyries was controlled by the WNW- and NEN-trending faults (Mao et al., 2011) (Fig. 1c).

3. Petrography and sampling Nine representative granite samples from the concealed ZYK intrusion and seventeen samples from the SBG were analysed in this study for whole-rock geochemical analysis. Sample G1 from borehole ZK1315 was used for the U-Pb dating and the Hf isotope analysis. The location of samples and salient details are listed in Supplementary Table 1 and Supplementary Table 2. Representative biotite grains were analysed by EPMA to obtain the compositional data (Supplementary Table 3 and Supplementary Table 4). The

geochemical data for the LJS intrusion are cited from Li et al. (2012a) and the biotite data are from Xu et al. (2015). 3.1 Shibaogou granitic pluton The Shibaogou granite porphyry has an exposed length of 2 km with a width of 1.5 km, and intrudes the meta-sandstone, marble, schist and quartzite of the Luanchuan Group and Guandaokou Group. The pluton is semi-circular in shape (Fig. 2) and is composed of porphyritic monzogranite and fine-medium grained monzogranite, with indistinct contact (Fig. 3a). The dominant lithology is porphyritic monzogranite with grain size ranging from 0.2 mm to 5 mm (Fig. 3a, c). Based on the field observation and petrography, a grain size decrease is noted in the porphyritic monzogranite from its southeastern to northwestern margin. Moreover, elliptical diorite enclaves composed of plagioclase, hornblende, and biotite occur within the monzogranite (Fig. 3b). The monzogranite is off-white in colour and exhibits massive structure and porphyritic texture (Fig. 3c), mainly composed of 20-40% K-feldspar, 15-30% plagioclase, 15-35% quartz and 2-5% biotite (Fig. 4d, e, f). The K-feldspar, quartz and plagioclase appear as phenocrysts. The K-feldspar grains display Carlsbad twins and euhedral to subhedral habit, with grain size ranging from 2-4 mm. Plagioclase shows polysynthetic twins, with grain size ranging from 2-4 mm. Occasionally weak sericitization is observed. Anhedral quartz commonly shows undulatory extinction. Biotite occurs as inclusions in hornblende (Fig. 4e). Anhedral laths of microcline with cross-hatch twins also occur (Fig. 4f). Sphene, apatite, zircon, and magnetite are the main accessory minerals. Zircon, sphene and apatite minerals sometimes are observed as inclusions in biotite (Fig. 4f). The biotite is medium to coarse grained and platy in nature, and occurs in association with plagioclase, hornblende, quartz and euhedral titanite (Fig. 4d, e, f). Chloritization of biotite is also common (Fig. 4d). Poikilitic biotite encloses

magnetite, titanite, and zircon. Typical biotite laths were selected for compositional analysis.

3.2 Zhongyuku concealed granitic pluton Fresh granite samples were collected from 3 boreholes at different depth (samples ZK1315, ZK1323 and ZK0715) in the ZYK intrusion (Fig. 1c) (Supplementary Table 2). The borehole core samples are generally medium to fine-grained, off-white to fleshy red and show massive structure in hand specimen (Fig. 3d). Under microscope, the rocks are characterized by equigranular texture, consisting mainly of 35-40% K-feldspar, 35-40% plagioclase, 10-20% quartz and 5-10% biotite corresponding to monzogranite (Fig. 3f), with sphene, apatite, zircon, ilmenite and magnetite as accessory minerals (Fig. 4a, b, c). The K-feldspar is subhedral to anhedral and shows Carlsbad twins and cross hatched twins (Fig. 4b). Euhedral to subhedral plagioclase minerals show polysynthetic twins, zoned nature and sometimes weak sericitization, enclosing euhedral to subhedral fine mica inclusions (Fig. 4b). Anhedral quartz commonly exhibits undulatory extinction (Fig. 4a). Biotite is typically fresh, medium- to fine-grained, flaky and euhedral to subhedral (Fig. 4a, b, c). Zircon, sphene and apatite sometimes occur as inclusions in the biotite (Fig. 4b). Chloritization of biotite has also been noticed in some samples (Fig. 4c).

4. Analytical methods 4.1 Petrology and chemical composition of biotite Fresh rock samples were selected to prepare thin sections for optical microscopy and electron microprobe analysis (EPMA). The microprobe data

were gathered through Shimadzu EPMA-1600 instrument housed at the Stage Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences in Beijing. The instrument was operated at a beam current of 20 nA and accelerating voltage of 15 kV. Electron beam diameter was kept at 1 μm. Structural formula based on 22 oxygen ions and partitioning of Fe3+ and Fe2+ from total iron as FeOT were carried out following the method of Lin and Peng (1994). The analytical error of main oxide is about 1%. 4.2 Whole rock geochemistry Fresh rock samples were crushed in a steel mortar and powdered in an agate mill to a grain size < 200 mesh. Major elements were analyzed at the Hubei Geological Analytical Center, Wuhan. The analytical uncertainty is generally <5%. Trace elements, including rare earth elements (REE), were measured using an Agilent 7500a ICP-MS system at the State Key Laboratory of Geological Processes and Mineral Resources (GPMR), China University of Geosciences, Wuhan. The sample-digestion procedure for ICP-MS analyses and analytical precision and accuracy are the same as those described by Liu et al. (2008).

4.3 Zircon U-Pb dating and trace elements of zircon Zircon grains were separated from crushed rocks by standard mineral separation techniques and were handpicked for analysis under a binocular microscope. Approximately 150 grains were mounted into an epoxy resin disc. Prior to isotope analysis, all grains were photographed under both transmitted and reflected light, and subsequently examined using the cathode luminescence (CL) image technique. Zircon U–Pb age dating and REE analysis were performed using a LA-ICP-MS instrument at the Key Laboratory of Crust-Mantle Materials and Environments, University of Science and Technology of China (USTC), Hefei. The laser-ablation system was a Geo Las

200 M equipped with a 193 nm laser. The diameter of a laser ablation pit was approximately 40 μm and the average power output was approximately 4 W. Zircon 91500 was used as an external calibration standard for age calculation, and NIST SRM 610 was analyzed twice for every 10 analyses for concentration calculations of U, Th and Pb. Common Pb correction was made by using the program Com Pb Corr#3-17 (Andersen, 2002). Trace elements were calibrated against NIST SRM 610 and using ZrO 2 (66.1%) as an internal standard. U–Pb isotopic ratios were calculated using the Glitter 4.0 program and U–Pb age calculation was done with the Isoplot program (Ludwig, 2003).

4.4 In situ zircon Hf isotope analysis Zircon Lu-Hf analysis was performed using a Neptune Plus MC-ICP-MS (Thermo Fisher Scientific, Germany) in combination with a Geolas 2005 excimer ArF laser ablation system (Lambda Physik, Göttingen, Germany) housed at the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences in Wuhan. The instrumental conditions and data acquisition were described by Hu et al. (2012). Off-line selection and integration of analyte signals, and mass bias calibrations were performed using ICPMS Data Cal (Liu, 2010).

5. Results 5.1 Chemical composition of biotite from ZYK and SBG The compositional data of biotite is listed in Supplementary Table 3 and Supplementary Table 4. The method of Lin and Peng (1994) was used to estimate the Fe3+ and Fe2+. Additional composition data for the LJS intrusion are from Xu et al. (2015).

Overall, biotite in the SBG and ZYK plutons are characterized by high and Mg, and low Al, similar to the characteristics of the LJS intrusion. In the plot of Mg-(Fe2++Mn)-(Fe3++AlVI+Ti), the data fall in the magnesian biotite field (Fig. 5). Biotites from the SBG rocks have SiO2 content varying from 35.77 to 38.46 wt. % with average content 37.18 wt. %; SiO2 content of ZYK biotite ranges from 35.99 to 39.72 wt. % with an average of 37.26 wt. %. Biotites in LJS have SiO2 content in the range of 35.81-38.77 wt. % (average 37.12 wt. %). Thus, biotites in the three plutons have similar SiO 2 content. All the biotite grains have high MgO content (SBG: 13.13-15.48 wt. % with average of 14.08%; ZYK: 12.29-15.62 wt. % with average of 13.44 wt. %; LJS: 11.47-15.14 wt. % with average of 12.73 wt. %). Biotite from LJS has the highest Al 2O3 content, ranging from 12.86 to 14.4 wt. % as compared to those from SBG (12.93-14.17 wt. %) and ZYK (12.05-13.74 wt. %). They show relatively higher TiO 2 content than those in LJS (1.88-3.81 wt. %). The AlVI of biotites from SBG (Al VI=0-0.11 apfu, average =0.04 apfu) and ZYK (Al VI=0-0.15 apfu, average=0.03 apfu) are lower than those biotites in LJS (Al VI=0-0.31 apfu, average=0.1 apfu). The high-Ti and low-AlVI in biotites indicate that they formed in relatively higher temperature and oxygen fugacity environment (De Albuquerque, 1973). The ratio of Fe2+/(Fe2++Mg2+), ranging from 0.61-0.68 for SBG, 0.56-0.67 for ZYK and 0.56-0.63 for LJS, is relatively homogeneous, indicating that post-magmatic alteration is negligible (Stone, 2000). Biotites from ZYK, SBG and LJS are Ca-free or Ca-poor, indicating that they were least affected by chloritization and sericitization through meteoric fluid circulation or post-magmatic deuteric alteration (Kumar and Pathak, 2010).

5.2 Geochemical features of the ZYK and SBG intrusions 5.2.1 Major elements

The

major

and

trace

elements

composition

data

are

listed in

Supplementary Table 1 and Supplementary Table 2. Additional data for LJS are from Li et al. (2012a). Rock samples from ZYK have the highest SiO 2 content, ranging from 71.52 to 75.34 wt. % compared with LJS (67.29-72.78 wt. %) and SBG (69.29-72.78 wt. %). SiO2 content of ore-related granite pluton (ZYK) are higher than those of the barren batholith (LJS). In the plot of SiO2 against K2O (Fig. 6a), the ore-related granitic plutons and barren LJS batholith show enrichment in K2O and span Shoshonite and High-K calc-alkaline Series fields, indicating that they can be grouped into the KCG type (K-rich calc-alkaline feldspar granite) (Barbarin, 1999). The ASI ratio index [molar Al 2O3/(CaO+Na2O+K2O)] can be used to distinguish the I-type granite and S-type granite (Fig. 6b) (Barbarin, 1999). The ASI ratios of ZYK and SBG are in a limited range of 0.90-1.05, and lower than the 0.95-1.13 for LJS. In the diagram of A/NK versus A/CNK, the ore-related plutons and LJS all correspond to I-type granites and they are characterized by metaluminous to peraluminous nature. Compared with ZYK and SBG, rocks from LJS are closer to S-type granites and one sample even falls in the S-type field, suggesting that the LJS batholith has transitional characteristics of I-type and S-type (Meng, 2010). The variable K2O+Na2O-CaO is an important index for the classification of granites, and is expressed as modified alkali-lime index (MALI) (Frost et al., 2001). On the plot of SiO2 vs. K2O+K2O-CaO, most spots of LJS and SBG correspond to the alkali-calcic field and some fall in the alkali field. In comparison, samples of ZYK are mostly calcic-alkalic (Fig. 6c). Frost et al. (2001) defined variable Fe*=[FeOT/(FeOT+MgO)] to distinguish the ferroan-type and magnesian-type felsic intrusions. In the diagram of SiO2-Fe*, almost all rocks are characterized by magnesian-type, which is a typical feature of I-type granites (Fig. 6d). Harker diagrams（Fig. 7）show similar evolutionary trends for ZYK, SBG and LJS intrusions. The Al 2O3, P2O5, Na2O and MgO show a negative

correlation with SiO2, consistent with magma mixing and possibly indicating that all granites originated from the same magma chamber. However, TiO 2, Fe2O3, K2O, and CaO do not exhibit clear linear variation with increasing SiO 2. And the data points show moderate scatter, suggesting the occurrence of AFC (assimilation and fractional crystallization) during emplacement of the ascending magma (Li et al., 2012a). 5.2.2 Trace elements In the primitive mantle normalized trace elements diagram (Fig. 8a, c), ZYK and SBG samples share similar trace element pattern, different from that of the LJS in some aspects (Fig. 8e), despite the common feature of strong negative P and Ti anomalies and Th-U enrichment, as well as positive Th and Hf anomalies. The LJS samples show obvious negative Sr anomalies and weak Nb negative anomalies. The ZYK samples have weak Ba positive anomalies whereas the SBG samples show negative Ba anomalies, possibly related to their mineralization potential. The chondrite-normalized rare earth element (REE) patterns (Fig. 8b, d, f) show total REE of 84.12-206.75 ppm (average is 132.17 ppm) for ZYK, 154.83-255.76 ppm (average is 206.68 ppm) for SBG and 105.08-243.29 ppm (average is 174.71 ppm) for LJS. The LREE/HREE ratios range from 11.28 to 16.23 for ZYK, 14.99 to 22.36 for SBG and 7.96 to 12.11 for LJS. A notable feature is the higher concentration of LREEs in ore-related plutons than that in the barren batholith, indicating strong fractionation of LREEs. The HREEs in LJS show higher concentration than those in the ore-related plutons, suggesting a different stage of magma evolution. The δEu ranges from 0.55-0.79 for ZYK, 0.73-1.07 for SBG and 0.47-0.62 for LJS. The three rock suites exhibit negative Eu anomalies, with the strongest in the LJS batholith. This feature suggests that plagioclase or alkali feldspar remained in the source region after fractional crystallization or partial melting. The REE patterns in the three rock suites show right dipping trend. The ore-bearing plutons have wider REE ranges. The similarity of the trends indicates that the magma chamber of

all rock types may be similar, although they underwent different magmatic evolutionary history (Li et al., 2012a). The (La/Yb)N and (La/Sm)N values are two important indices that reveal the level of fractionation of LREE and HREE. Compared with the ZYK (12.03-19.70, average 16.74) and LJS (7.61-13.57, average 9.40), the SBG shows the highest average value (35.07) and widest range (17.71-60.02) of (La/Yb)N. The (La/Yb)N values in ore-related plutons are markedly higher than those in the LJS batholith suggesting that the level of HREE differentiation in granite plutons is higher than in the LJS, consistent with the ratios of LREE/HREE. The (La/Sm)N values of ZYK are in the range of 4.56–8.95, those of SBG are 5.17-9.95 whereas those of LJS batholith show 3.75–5.77, confirming the interpretation that the ore-bearing granites have undergone a higher degree of differentiation.

5.3 Zircon U-Pb ages and rare earth element geochemistry The size of zircon grains in sample G1 from the ZYK intrusion ranges from 80 to 160 μm in length and 40 to 80 μm in width, with an aspect ratio of 1:1 to 2:1. They display euhedral to subhedral morphology. The grains are prismatic, colorless and transparent, and a few grains display oval shapes. As shown in the CL images, most zircon grains possess oscillatory zoning, which is a typical feature of magmatic zircons (Corfu, 2003), and some grains carry inherited cores (Fig. 9d). Twenty-four grains were analysed from sample G1 and the results are listed in Table 1. The Th contents range from 292 to 2742 ppm with average value 784 ppm and U contents have a range of 604 to 2330 ppm with average of 1245 ppm. The Th/U ratio ranges from 0.34 to 0.96 (with the exception of spot 10 with very high value of 1.92), typical of magmatic origin (Corfu, 2003). . The data yield a U–Pb weighted mean age of 149.6 ± 2.4 Ma (MSWD = 2.3,

Table 1, Fig. 9), suggesting magmatism during Late Jurassic- Early Cretaceous. The rare earth element analyses of zircons in sample G1 are presented in Table 2. On the chondrite-normalized REE plots (Fig. 10), the zircons exhibit typical positive Ce anomalies and weakly negative Eu anomalies, with HREE-enriched patterns. The δCe of zircons ranges from 3.326 to 511.191 with an average of 156.797. The δEu ranges from 0.297 to 0.607, defining a weakly negative Eu anomaly, typical of zircon grains in unaltered igneous rocks (Hoskin, 2003).

5.4 Zircon Lu-Hf isotopic compositions Nine of the dated zircon grains were also analysed for in situ Hf isotopic composition. The results are summarized in Table 3. The initial

176

Hf/177Hf

ratios are between 0.282126 and 0.282206 with an average of 0.282171. The initial

176

Lu/177Hf ranges from 0.000886 to 0.002853 with an average of

0.001542 and initial

176

Yb/177Hf ratios range from 0.021450 to 0.086536 with

mean at 0.041496. The calculated single stage Hf model age (T DM1) ranges from 1489 to 1589 Ma (mean 1546 Ma) and the two stage model age (TDM2) shows a range of 1998 to 2156 Ma with average at 2069 Ma. The mean εHf (t) values ranges from -16.8 to -19.7, suggesting that the source materials were evolved from reworked crustal components.

6. Discussion 6.1 Redox state Ishihara (1977) proposed that the redox state of magmas are related to the formation of magmatic-hydrothermal deposits. Thus, Ishihara (1977,1979) divided the granitoids into magnetite- and ilmenite-series. The more oxidized

magnetite-series granitoids are related to Cu, Mo, Pb-Zn and W (tungstite) mineralization, whereas the more reduced ilmenite-series granitoids relate to Sn and W (wolframite) deposits. Subsequently, many workers validated the relationship by using theoretical and experimental studies confirming that the redox state of magma exerts strong control on the nature of much mineralization (Lodders and Palme, 1991; Blevin and Chappell, 1992; Candela, 1992; Blevin et al., 1995; Blevin, 2004). Blevin (1992, 1995 and 2004) proposed that Sn mineralization is related to reduced rocks and Mo-Cu-Au is associated with oxidized rocks. Candela (1992) reported that primitive andesitic magma containing 1000×10-6 S and 20×10-6 Cu, 98% of Cu ma would be enriched in pyrrhotites, with only 1.8% of Cu coming into hydrothermal fluid related to the mineralization. This indicates that redox state may hinder the formation of ore deposits even though the magma has high content of metallogenic components. Lodders and Palme (1991) and Mengason et al. (2011) found that the partition coefficients of Mo among silicate melt and sulfur phase increase with decreasing oxygen fugacity. The oxidation state of Fe is generally used to represent the redox state in magmas. For typical granitic rocks at any given SiO 2 content, the range of possible Fe-bearing minerals and their relative proportions are very limited (Blevin, 2004). In the plot of redox classification scheme for igneous rocks, whole rock Fe, which is expressed as FeO *=FeO+0.9*Fe2O3, replaces SiO2, against log10 Fe2O3/ FeO (Fig. 11a). However, if SiO2 content is high (>72%) and related FeO* content is low (below 2%), the Fe 2O3/FeO ratios of most granitoids may not represent the real redox state of magma. In the present case, the samples of SBG mostly fall into the VSO field, whereas those of the ZYK correspond to SO field. The plots of LJS span SO and MO fields, indicating the complexity of the source magmas of this intrusion. Even though some plots of SBG are characterized by FeO*<2% and some of the ZYK samples are characterized by SiO2 >72%, the occurrence of magnetite in both ZYK and SBG intrusions (Fig. 3 and Fig. 4) suggest that their magmas were in

oxidized state. As a result, the more oxidized ZYK and SBG intrusion are favorable for the formation of Mo deposits, compared with the LJS. The plot of Fe2O3/FeO versus SiO2 shows the relationship among Cu, Mo, Sn and W mineralization and redox state of the related granites (Fig. 11b). Almost all plots fall into the Mo field and are characterized by magnetite series granites, suggesting that the ZYK, SBG and LJS may be related to the Mo deposits which is consistent with the previous studies. However, since the LJS is barren, other indicators should be considered. The nature and composition of biotite in granites also reveal the redox state of magma crystallization. Wones and Eugster (1965) estimated the oxygen fugacity of magma by investigating the content of Fe 3+, Fe2+ and Mg2+ in biotite coexisting with magnetite and K-feldspar. The ternary plot of Fe3+, Fe2+ and Mg2+ shows the three oxygen fugacity buffers: fayalite-magnetite-quartz (FMQ), nickel-nickel oxide (NNO), and magnetite-hematite (MH) (Fig. 11c). From FMQ, NNO to MH, the oxidation state increases (Blevin, 2004). In Fig. 11a, the division between oxidized (O) and reduced (R) igneous rocks is at or close to the FMQ buffer (Blevin, 2004). The boundary between MO and SO occurs immediately below the NNO buffer, whereas the boundary between MR and SR is at FMQ-1.3. In Fig. 11c, almost all the biotite samples fall within or above the NNO buffer, indicating high oxygen fugacity conditions consistent with results shown at Fig. 11a, favoring the formation of Mo mineralization. 6.2 P-T conditions 6.2.1 Temperature The chemical composition of biotite can be used to estimate the temperature, pressure and oxygen fugacity of intermediate-acid intrusive rocks, as has been confirmed from experimental petrology (Anderson et al., 2008). Oxygen fugacity and temperature can be estimated from Fe/(Fe+Mg) ratio of biotite in granite, coexisting with K-feldspar and magnetite by using the fO 2-T plot of Wones and Eugster (1965) at constant pressure of 207 Mpa. On the log

fO2-T plot, based on the oxygen fugacity buffers in triangle phase plot of Fe3+-Fe2+-Mg2+ (Fig. 11c) and the stability of biotite (Fig. 12a), in the form of 100×Fe/(Fe + Mg), some ellipses can be drawn, showing the range of temperature and oxygen fugacity. Temperature ranges from 790 to 925 ℃ for ZYK, 820 to 915 ℃ for SBG and 850 to 900 ℃ for LJS; log fO2 ranges from -12.8 to -10.4 for ZYK, -11.8 to -10 for SBG and -12.6 to -11.6 for LJS (Fig. 12). The ZYK has the widest temperature and oxygen fugacity ranges and SBG also shows wider range than those of LJS, indicating that the ore-related granites have wider temperature and oxygen fugacity ranges than the ore-barren granites. Hydrothermal extraction of minerals requires longer time and wide temperature range, aiding in the Mo, W and Pb-Zn mineralization. Solubility of zircon is highly sensitive to temperature and weakly sensitive to other factors. Zircon is a common mineral in crustal and the zircon saturation

temperature

approximates the

near-liquids temperature

of

granitoids (Miller et al., 2003). From high temperature experiments, Watson and Harrison (1983) obtained the following correlation among zircon solubility, temperature, and major element composition of melt: tZr = 12900/[ln (496000/Zrmelt)+0.85M+2.95]

(1)

where the DZr,496000/melt is the partition coefficient of Zr; M equals (2Ca+K+Na)/(Al*Si). Zr concentration (ppm) is 496000×10-6 ppm without the Zr and Hf corrections. Generally, whole rock Zr content approximates the Zr content in the melt. The Zr saturation temperatures for SBG and ZYK are listed in Supplementary Table 1 and Supplementary Table 2 respectively. The ZYK intrusion has the lowest TZr (average=762 ℃) compared with SBG (776 ℃) and LJS (805 ℃). Given that most zircons in these rocks show magmatic features, the zircon saturation temperature can be interpreted as minimum magma temperature, which is consistent with the crystallization temperature of biotites from LJS, SBG and ZYK (Bao et al., 2009).

6.2.2 Pressure Based on a systematic investigation of the chemical composition of biotites in representative granitic rocks in Japan, Uchida et al. (2007) established a positive relationship between total Al ( TAl) content of biotite and the solidification pressure of the granites through the application of sphalerite and hornblende geobarometers. The following empirical equation was proposed by these authors for biotite: P (kbar) =3.03×TAl-6.53 (±0.33)

(2)

where TAl designates the total Al content in biotite on the basis O = 22. The calculated pressure of ZYK, SBG and LJS intrusions are listed in Supplementary Table 3 and Supplementary Table 4 and shown in Fig. 13a. The solidification pressure is estimated as 6-86 Mpa (average=45 Mpa) for ZYK, 41-110 Mpa for SBG (average=74 Mpa) and 48-146 Mpa for LJS (average=91 Mpa). Almost all samples yield pressures below 100 Mpa (1 kbar), indicating the correlation with Mo and Pb-Zn deposits. Depth can also be estimated by applying the lithostatic pressure calculation with a mean pressure gradient of 27.5 Mpa/km (Fig. 13b). The emplacement depth of ZYK ranges from 0.20-3.14 km and average depth is 1.63 km; SBG ranges from 1.49 to 3.99 km with an average of 2.69 km; LJS ranges from 1.76 to 5.32 km with an average of 3.31 km. Obviously, the barren batholith of LJS shows the deepest emplacement conditions and solidification pressure than those of the ore-bearing plutons of SBG and ZYK. Only those magmas which reach the H2O-saturation form a discrete hydrothermal phase. The saturation of H2O in silicate melts is affected by pressure. The process whereby vapor-saturation is achieved by virtue of decreasing pressure is called “first boiling”, and is considered as a potential step

to

form

magmatic

hydrothermal

deposits

(Robb,

2005).

The

decompression process of intrusive rocks is therefore of great significance in the formation of an independent hydrothermal phase which is a prerequisite for forming hydrothermal deposits. Additionally, the volume of silicate melt plus the

hydrothermal phase per unit mass is much larger than that of molten silicate melts. The increase of volume can be up to 30%, leading to the formation of a large number of cracks in the intrusive body and the surrounding rocks. These cracks provide channels for the circulation of ore-bearing hydrothermal fluid, so that hydrothermal extraction of minerals is effective and conducive to mineralization (Xu et al., 2013). Comparing the solidification pressure of ore-related SBG (74 Mpa) and ZYK (45Mpa) and barren LJS (91 Mpa) intrusions, we infer that the ore-related plutons might have experienced decompression process favorable to develop magmatic hydrothermal deposits. The ZYK intrusion shows the most favorable conditions for forming ore deposits.

6.3 Compositional features The classification of granites based on their compositional features is important to investigate the abundance of elements and volatiles in granites (Blevin, 2004). I-type granitoids are often related to porphyry Cu, Mo, Pb, Zn and W mineralization, S-type granitoids are associated with Sn, W and U (Li, Be and B), and A-type granitoids are related to Zr, Hf , Nb, REE and so on enrichment (Ray et al., 1995; Christiansen and Keith, 1996; Gill, 2010). The ZYK and SBG are characterized by I-type features and show a tight correlation with Mo and Pb-Zn mineralization compared with the LJS. This inference is also consistent with the fact that the ZYK and SBG are ore-bearing plutons whereas the LJS is a barren batholith (Meng, 2010; Li et al., 2012a; Bao et al., 2014). Aluminium saturation and alkalinity are important parameters for evaluating the mineralogy of granites and their fractionation process (Blevin, 2004). Metaluminous granites (CNK>A>NK) are closely related to the porphyry deposits, peraluminous granitoids (A>CNK) relate to Sn-W-Cu and Be-B-Li-P deposits, and peralkaline granites (A
The TAl content is a useful indicator for mineral exploration with a positive correlation established between the content of total Al ( TAl) in biotite and mineralization type in hydrothermal ore deposits (Uchida et al., 2007). Biotite T

Al content increases as follows: Pb-Zn and Mo deposits, Cu-Fe and Sn

deposits, W deposits and non-mineralized granitic rocks (Fig. 14). This order reveals that the solidification pressure of granites is related to types of mineralization. Additionally, the relationship between TAl content in biotite and alumina saturation index of the granitic rocks has also been observed. As shown in the plots (Fig. 14), the ZYK and SBG fall into the Mo and Pb-Zn deposits field, exhibiting the potential for Mo and Pb-Zn hydrothermal ore deposits. Granitoids which have high-K compositions contribute to the formation of mineralization. As well known, most Sn- and Mo-mineralization are associated with high-K granitoids and porphyry Cu mineralization is associated with high-K or potassic rocks, or some cases with low- and medium-K rocks (Blevin, 2004). The high alkali content can significantly reduce the solidus temperature of the melt (Glyuk and Anfilogov, 1973) and simultaneously increase the miscibility of Mo in aqueous silicates close to the solidus temperature (Isuk and Carman, 1981). The plot of K2O against SiO2 (Fig. 6a) suggests that all granitic rocks of present study exhibit high-K feature, although ZYK shows the most evolved high-K characteristic, linking it with the Mo deposits.

6.4 Compositional evolution There is no single or easy index that defines the compositional evolution of granitoid magmas (Blevin, 2004). Possible parameters are the abundance of incompatible elements and the ratio of incompatible/compatible elements. Granitoids with high Rb/Sr ratios signify evolved nature. Intermediate values may suggest plagioclase accumulation and fractional crystallisation. The Cu-Au mineralization are related to I-type granites of high-oxidation and

low-differentiation, the Cu-Mo mineralization often occur in granites of high-oxidation and medium-differentiation, and Sn-W deposits are closely related to S-type granites of high reducibility and high evolution degree (Blevin et al., 2003). Similar view was also proposed by Ray et al. (1995) that Cu deposits are mainly related to undifferentiated I-type granites. With an increase in the degree of differentiation of siliceous magmas, the content of Cu decreases. The contamination with continental crust will dilute the metal content of magma. The Fe2O3/FeO versus Rb/Sr plot show the relationship among redox state, degree of evolution and mineralization type (Fig. 15a). On this plot, from SBG, LJS to ZYK, the degree of evolution increases. Additionally, samples of ZYK show the strongest relationship with W-Mo mineralization, compared with that of SBG and LJS which fall in the transition zones. The K/Rb ratio is also an important indicator for the degree of evolution (Blevin, 2002). Rb is more incompatible than K due to its larger ionic radius. Therefore, K/Rb can be used to evaluate the degree of evolution. With increasing degree of evolution, the K/Rb value decreases. In granites, K-feldspar, biotite and muscovite are the three important minerals that host K and Rb. And granites have been divided into three groups based on the K/Rb ratio (Blevin, 2004) as unevolved (>400), moderately evolved (200-400) and strongly evolved (<200) (Fig. 15b). Granites related to Mo, W-wolframite and Sn mineralization have K/Rb ratios below 200, whereas those associated with Cu and Cu-Au mineralization tend to have K/Rb ratios higher than 200. Granites with K/Rb ratios below 140 are termed as highly fractionated granites. Fig. 15b shows the classification scheme for granites. In this figure, the ZYK intrusion is characterized by strongly evolved nature, whereas SBG and LJS correspond to the moderately evolved granitoid field. This inference is also consistent with the result shown in Fig. 15a. With an increase in the SiO 2 content, the K/Rb ratios of ZYK, SBG and LJS tend to decrease, suggesting the role of K-feldspar in fractionation process. Thus, ZYK has the highest possibility of Mo mineralization compared with SBG and LJS.

6.5 Source of granites The composition of biotite also provides clues on the source region of magma, genetic type of rocks and tectonic setting. The Mg# of biotite (Mg/Mg+Fe*+Mn) in granite reveals the characteristics of source region. Granite with Mg# >0.45 is considered to represent deep source whereas those with Mg# <0.45 denote shallow source. In our study, the Mg # of ZYK, SBG and LJS are all above 0.45 (Supplementary Table 3 and Supplementary Table 4), suggesting deep source. Additionally the LJS, SBG and ZYK fall in the MC field, corresponding to mantle-crust mixed magma source, in the FeOT/ (FeOT+MgO) versus MgO ternary plot (Fig. 16a). Thus, magmas for these granitoids were sourced from depth with mantle-crust interaction, although the sources are similar for all the three intrusions. The characteristics of biotites from

non-orogenic

alkaline

rock

series,

subduction-related

orogenic

calc-alkaline rock series and peraluminous rock series were summarized by Abdelrahman (1994), showing that biotite composition can be used for tectonic discrimination. In the FeO*-Al2O3-MgO plot (Fig. 16b), all of our samples fall in the “C” field, representing orogenic calc-alkaline rock series. However, according to Shabani et al. (2003) and Tao et al. (2015), the composition of biotite reflects the nature of the source magmas whereas it does not have a good effect on discriminating tectonic setting of these rocks without the aid of other data, such as whole rock geochemistry, geochronology data and isotopic data. In our study, the εHf(t) of zircons in ZYK ranges from −16.81 to −19.74, TDM2 ranges from 1998 Ma to 2156 Ma and

176

Hf/177Hf ratios are in the range of

0.282126 to 0.282206 (Table 3). Zircons from the SBG have

176

Hf/177Hf ratios

of 0.281913-0.282444, εHf(t) values of −26.9 to −8.3 (average,−15.7), T DM2 of 1.73-2.36 Ga (Yang et al., 2012). Based on the available Nd (Bao et al., 2009) and Sr, O isotope data (Wu et al., 2007; Yang et al., 1997; Wang, 2000), we

can conclude that ZYK and SBG originated from lower crust with the involvement of mantle derived material. The

176

Hf/177Hf of the LJS are from

0.282633 to 0.282767. The εHf(t) ranges from −2.73 to 2.10, and the TDM2 ranges from 853 Ma to 1101 Ma, indicating that the sources were derived from melting of the crust with the involvement of mantle components (Wu et al., 2007; Meng, 2010). Generally speaking, granites in Luanchuan ore district originated from remelting of the crust with the involvement of mantle components (Li et al., 2012a). 6.6 Tectonic setting As shown in Table 4, most of the ore-related granitic plutons in the Luanchuan ore district formed during 157~141 Ma and the major metallogenic periods for the magmatic–hydrothermal systems are dated as 147~136 Ma during the late Jurassic. Zircon U-Pb mean age for LJS intrusion is about 110 Ma (Meng, 2010), for ZYK is 149.6±2.4 Ma and for SBG is 156±1 Ma (Yang et al., 2012). Thus, the ZYK and SBG were products of late Jurassic magmatism, which are different from barren batholith LJS which formed during the late stage of early Cretaceous. Trace elements of granites have been used to infer the tectonic settings. Fig. 17 and Fig. 18 show the tectonic setting of ZYK, SBG and LJS, displaying the differences and similarities. Plots of ZYK, SBG and LJS mostly fall in the Post-COLG field (Fig. 17a, b), suggesting that the ore-related plutons and barren batholith are of the same post-collisional setting. The ZYK and SBG fall across the WPG and syn-COLG fields whereas the LJS samples mostly fall within the WPG field (Fig. 17c, d), indicating the different tectonic settings of ore-related plutons and barren batholith. The plots of SBG and ZYK show a transitional trend, from syn-collision setting to within-plate setting. In the plot of lg[CaO/(K2O+Na2O)] versus SiO2 (Fig. 18), most of the ZYK and SBG samples fall in the intersection of extension and compression fields, attesting to a transforming tectonic setting. However, the LJS exhibits different characteristic

and plots within the extensional field near the margin of compression field. We therefore infer that the LJS formed in an extension-related geodynamic setting whereas the ZYK and SBG formed in a transitional setting during compression to extension. These different tectonic settings might have exerted control on their mineralization history. Three large-scale metallogenic pulses have been identified in the North China Craton, at 190-160 Ma, ca. 140 Ma and ca. 120 Ma, associated with post-collisional process following the collision between the North China Craton and the Yangtze Craton at ca. 210 Ma (Mao et al., 2005; Jiang et al., 2010; Li et al., 2012a). The lithosphere of eastern China has undergone major thinning process during 170-135 Ma (Zhou, 2009; Lu et al., 2002; Deng et al., 2007; Mengason et al., 2011; Li and Santosh, 2014), triggering remelting of the lower crust. The formation of ore-bearing plutons in East Qinling, including those in the Luanchuan ore district at 150~157 Ma are considered to be related to the remelted lower crust (Mao et al., 2008; Bao et al., 2009). At about 145 Ma, the tectonic regime began to transform from compression to extension (Li et al., 2012a) and this period is also marked by large-scale metallogenic explosion (Mao et al., 2005). By ~115 Ma, the transformation was completed into an extensional setting. The culmination of collision process between the North China Craton and the Yangtze Craton marks the formation of the barren batholith of LJS in a within-plate setting (Fig. 19).

7. Conclusions The salient conclusions arising from our present study are as follows. 1. Geochemical analyses of the ore-related ZYK and SBG plutons indicate that they are both characterized by high-Si, high-K, alkali-rich and metaluminous to peraluminous nature with I-type features, similar to the ore-barren LJS batholith. In addition, compositional data on biotite also exhibits similar characteristics of high Si and Mg and low Al and Fe. The ZYK pluton experienced the highest degree of differentiation.

2. Zircon grains from the ZYK intrusion yield

206

Pb/238U mean age of

149.6±2.4 Ma suggesting widespread Late Jurassic to Early Cretaceous magmatism. The zircon εHf (t) values and TDM2 range from -16.8 to -19.7and 1998 to 2156 Ma respectively. Source materials were evolved from re-melting of deep crustal material with minor input of mantle components. 3. The ore-related plutons were derived from oxidized magmas. The ZYK pluton shows the widest temperature and oxygen fugacity ranges as compared to the SBG pluton and LJS batholith, and is considered to be conductive for the formation of Mo-W deposits. The ZYK pluton with the least solidification pressure and emplacement depth experienced decompression favoring the formation of magmatic hydrothermal deposits. 4. Ore-related ZYK and SBG intrusions formed in a transitional tectonic setting at the stage from compression to extension, whereas the ore-barren LJS was formed in an extension-related geodynamic setting. The different tectonic settings exerted significant control on the contrasting mineralization potential of the granites in the Luanchuan ore district.

Acknowledgments We are grateful to Guest Editor Prof. E. Shaji and two anonymous reviewers for their constructive comments. Fei Xue also thanks Dr. Wenjuan Jia and Mr. Zhiqiang Zhang for their kind help during the field work. This research was jointly sponsored by the National Natural Science Foundation of China with Grant No. 41572318, the National Science and Technology Support Project of the 12th “Five-Year Plan” with the Grant No. 2011BAB04B06 and the Fundamental Research Funds for the Central Universities of China University of Geosciences, Beijing with Grant No. 2-9-2012-143.

References Abdelrahman, A.M., 1994. Nature of Biotite from Alkaline, Calc-alkaline, and Peraluminous Magmas. Journal of Petrology, 35(2): 525-541. Andersen, T., 2002. Correction of common lead in U–Pb analyses that do not report 204Pb. Chemical Geology, 192(1–2): 59-79. Anderson, J.L., Barth, A. P., Wooden, J.L., Mazdab, F., 2008. Thermometers and Thermobarometers in Granitic Systems. Reviews in Mineralogy & Geochemistry, 69(1): 121-142. Aydin, F., Karsli, O., Sadiklar, M.B., 2003. Mineralogy and Chemistry of Biotites from Eastern Pontide Granitoid Rocks, NE-Turkey: Some Petrological Implications for Granitoid Magmas. Chemie der Erde- Geochemistry, 63(2): 163-182. Bao, Z.W., Wang, C.Y., Zhao, T.P., Gao, X., Li, C.J., 2014. Petrogenesis of the Mesozoic granites and Mo mineralization of the Luanchuan ore field in the East Qinling Mo mineralization belt, Central China. Ore Geology Reviews, 57(3): 132-153. Bao, Z.W., Zeng, Q.S., Zhao, T.P., 2009. Geochemistry and petrogenesis of the ore-related Nannihu and Shangfanggou granite porphyries from east Qinling belt and their constaints on the molybdenum mineralization. Acta Petrologica Sinica, 25(10): 2523-2536 (in Chinese with English abstract). Barbarin, B., 1999. A review of the relationships between granitoid types, their origins and their geodynamic environments. Lithos, 46(3): 605-626. Blevin, P.L., 2002. The petrographic and compositional character of variably K-enriched magmatic suites associated with Ordovician porphyry Cu-Au mineralisation in the Lachlan Fold Belt, Australia. Mineralium Deposita, 37(1): 87-99. Blevin, P.L., Chappell, B.W., Jones, M., 2003. Magmas to mineralisation: the Ishihara Symposium. GEMOC, Macquarie University, July 22-24 2003. Abstract volume.

Blevin, P.L., 2004. Redox and compositional parameters for interpreting the granitoid metallogeny of eastern Australia: Implications for gold-rich ore systems. Resource Geology, 54(3): 241-252. Blevin, P.L., Chappell, B.W., 1992. The role of magma sources, oxidation states and fractionation in determing the granite metallogeny of easten Australia. Transactions of the Royal Society of Edinburgh. Earth sciences, 83(1-2): 305-316. Blevin, P.L., Chappell, B.W., 1995. Chemistry, origin, and evolution of mineralized granites in the Lachlan Fold Belt, Australia: the metallogeny of I- and S-type granites. Economic Geology, 90(6): 1604-1619. Borodina, N.S., Fershtater, G.B., Votyakov, S.L., 1999. The oxidation ratio of iron in coexisting biotite and hornblende from granitic and metamorphic rocks: The role of P, T and f(O2). Canadian Mineralogist, 37(6): 1423-1429. Brown, G.C., 1982. Calc-alkaline intrusive rocks: their diversity, evolution, and relation to volcanic arcs. Andesites, 437-461. Candela, P.A., 1992. Controls on ore metal ratios in granite-related ore systems: an experimental and computational approach. Transactions of the Royal Society of Edinburgh. Earth sciences, 83(1-2): 317-326. Cao, H.W., Zhang, S.T., Zheng, L., Liu, R.P., Tian, H.H., Zhang, X.H., Li, J.J., 2014. Trace element geochemical characteristics of sphalerite in the Zhongyuku (Pb)–Zndeposit of the Luanchuan, Southwest of China. Journal of Mineralogy & Petrology, 16: 50-59 (in Chinese with English abstract). Cao, H.W., Zhang, S.T., Santosh, M., Zheng, L., Tang, L., Li, D., Zhang, X.H., Zhang,

Y.H.,

2015.

The

Luanchuan

Mo-W-Pb-Zn-Ag

magmatic-

hydrothermal system in the East Qinling metallogenic belt, China: Constrains on metallogenesis from C-H-O-S-Pb isotope compositions and Rb-Sr isochron ages. Journal of Asian Earth Sciences, 111: 751-780. Christiansen, E.H., Keith, J.D., 1996. Trace element systematics in silicic

magmas: a metallogenic perspective. Trace element geochemistry of volcanic rocks: applications for massive sulphide exploration. Edited by DA Wyman. Geological Association of Canada, Short Course Notes, 12, 115-151. Corfu, F., Hanchar, J.M., Hoskin, P.W., Kinny, P., 2003. Atlas of Zircon Textures. Reviews in Mineralogy & Geochemistry, 53(1): 469-500. De Albuquerque, C.A.R., 1973. Geochemistry of biotites from granitic rocks, Northern

Portugal.

Geochimica

Et

Cosmochimica

Acta,

37(37):

1779-1802. Deng, J.F., Su, S.G., Niu, Y.L., Liu, C., Zhao, G.C., Zhao, X.G., Zhou, S., Wu, Z.X, 2007. A possible model for the lithospheric thinning of North China Craton: Evidence from the Yanshanian (Jura-Cretaceous) magmatism and tectonism. Lithos, 96(1): 22–35. Dong, Q., Du, Y.S., Cao, Y., Pang, Z.S., Song, L.X., Zheng, Z., 2011. Compositional characteristics of biotites in wushan granodiorite, Jiangxi Province: Implications for petrogenesis and mineralization. Journal of Mineralogy & Petrology, 31(2): 1-6. Dong, Y.P, Santosh, M., 2016. Tectonic architecture and multiple orogeny of theQinling orogenic belt, Central China. Gondwana Research, 29, 1-40. Dong, Y.P., Zhang, G.W., Neubauer, F., Liu, X.M., Genser, J., Hauzenberger, C., 2011. Tectonic evolution of the Qinling orogen, China: Review and synthesis. Journal of Asian Earth Sciences, 41(3): 213-237. Duan, S.G., Xue, C.J., Liu, G.Y., Yan, C.H., Feng, Q.W., Song, Y.W., Tu, Q.J., Gao, Y.B., Gao, B.Y., 2010. Geology and sulfur isotope geochemistry of lead-zinc deposits in Luanchuan district, Henan Province, China. Earth Science Frontiers, 17(2): 375-384 (in Chinese with English abstract). Duan, S.G., Xue, C.J., Feng, Q.W., Gao, B.Y., Liu, G.Y., Yan, C.H., Song, Y.W., 2011. Ore Geology, Fluid Inclusion, and S- and Pb-Isotopic Constraints on the Genesis of the Chitudian Zn-Pb Deposit, Southern Margin of the North China Craton. Resource Geology, 61(3): 224-240.

Feng, L.Y., Wen, M.J., Hu, H.B., Jian, G.B., Jun, A.B.F., 2005. Geology, distribution, types and tectonic settings of Mesozoic molybdenum deposits in East Qinling area. Mineral Deposits, 24(3): 292-304 (in Chinese with English abstract). Foster, M.D., 1960. Interpretation of the composition of trioctahedral micas. U.S. Geol. Surv. Prof. Paper 354-B, pp.1-49. Frost, B.R., Barnes, C.G., Collins, W.J., Arculus, R.J., Ellis, D.J., Frost, C.D., 2001. A Geochemical Classification for Granitic Rocks. Journal of Petrology, 42(11): 2033-2048. Gao, Y., Mao, J.W., Ye, H.S., Meng, F., Li, Y.F., 2015. A review of the geological characteristics and geodynamic setting of the late Early Cretaceous molybdenum deposits in the East Qinling–Dabie molybdenum belt, East China. Journal of Asian Earth Sciences, 108: 81-96. Gill, R., 2010. Igneous rocks and processes: a practical guide. WileyBlackwell, 521-554 pp. Glyuk, D.S., Anfilogov, V.N., 1973. Phase equilibria in the system graniteH2O-HF at a pressure of 1000 kg/cm2. Geochem. Int, 10(1), 321-25. Guo, P., Santosh, M., Li, S.R., 2013. Geodynamics of gold metallogeny in the Shandong Province, NE China: An integrated geological, geophysical and geochemical perspective. Gondwana Research, 24(3-4): 1172-1202. Han, Y.G., Zhang, S.H., Pirajno, F., Zhou, X.W., Zhao, G.C., Qü, W.J., Liu, S.H., Zhang, J.M., Liang, H.B., Yang, K., 2013. U–Pb and Re–Os isotopic systematics and zircon Ce4+/Ce3+ ratios in the Shiyaogou Mo deposit in eastern Qinling, central China: Insights into the oxidation state of granitoids and Mo (Au) mineralization. Ore Geology Reviews, 55(15): 29-47. Henry, D.J., Guidotti, C.V., Thomson, J. A., 2005. The Ti-saturation surface for low-to-medium

pressure

metapelitic

biotites:

Implications

for

geothermometry and Ti-substitution mechanisms. American Mineralogist, 90(2-3): 316-328.

Hoskin, P.W., Schaltegger, U., 2003. The composition of zircon and igneous and metamorphic petrogenesis. Reviews in Mineralogy & Geochemistry, 53(1): 27-62. Hu, Z.C., Liu, Y.S., Gao, S., Xiao, S.Q., Zhao, L.S., Günther, D., Li, M., Zhang, W., Zong, K.Q., 2012. A “wire” signal smoothing device for laser ablation inductively coupled plasma mass spectrometry analysis. Spectrochimica Acta Part B Atomic Spectroscopy, 78(78): 50-57. Ishihara, S., 1977. The magnetite-series and ilmenite-series granitic rocks. Shigen-Chishitsu, 27: 293-305. Ishihara, S., Sawata, H., Arpornsuwan, S., Busaracome, P., Bungbrakearti, N., 1979. The magnetite-series and ilmenite-series granitoids and their bearing on tin mineralization, particularly of the Malay Peninsula region. Bulletin of the Geological Society of Malaysia, 11, 103-110. Isuk, E.E., Carman, J.H., 1981. The system Na 2Si2O5-K2Si2O5MoS2-H2O with implications for molybdenum transport in silicate melts. Economic Geology, 76(8): 2222-2235. Jacobs, D.C. and Parry, W.T., 1979. Geochemistry of biotite in the Santa Rita porphyry copper deposit, New Mexico. Economic Geology, 74(4): 860-887. Jiang, Y.H., Jin, G.D., Liao, S.Y., Zhou, Q. and Zhao, P., 2010. Geochemical and Sr–Nd–Hf isotopic constraints on the origin of Late Triassic granitoids from the Qinling orogen, central China: Implications for a continental arc to continent–continent collision. Lithos, 117(1–4): 183-197. Kumar, S., Pathak, M., 2010. Mineralogy and geochemistry of biotites from Proterozoic granitoids of western Arunachal Himalaya: Evidence of bimodal granitogeny and tectonic affinity. Journal of the Geological Society of India, 75(5): 715-730. Lalonde, A.E., Bernard, P., 1993. Composition and color of biotite from granites: two useful properties in the characterization of plutonic suites from the Hepburn internal zone of Wopmay Orogen, Northwest Territories.

Lehmann, P.D.B., 1990. Metallogeny of Tin. Lecture Notes in Earth Sciences Berlin Springer Verlag, 32. Li, D., Zhang, S.T., Yan, C.H., Wang, G.W., Song, Y.W., Ma, Z.B., Han, J.W., 2012a. Late Mesozoic time constraints on tectonic changes of the Luanchuan Mo belt, East Qinling orogen, Central China. Journal of Geodynamics, 61(5): 94-104. Li, D., Han, J.W., Zhang, S.T., Yan, C.H., Cao, H.W., Song, Y.W., 2015. Temporal evolution of granitic magmas in the Luanchuan metallogenic belt, east Qinling Orogen, central China: Implications for Mo metallogenesis. Journal of Asian Earth Sciences, 111: 663-680. Li, J.W., Li, Z.K., Zhou, M.F., Chen, L., Bi, S.J., Deng, X.D., Qiu, H.N., Cohen, B., Selby, D., Zhao, X.F., 2012b. The Early Cretaceous Yangzhaiyu lode gold deposit, North China Craton: a link between craton reactivation and gold veining. Economic Geology, 107(1): 43-79. Li, N., Chen, Y.J., Zhang, H., Zhao, T.P., Deng, X.H., Wang, Y., Ni, Z.Y., 2007. Molybdenum deposits in East Qinling. Earth Science Frontiers, 14: 186-198 (in Chinese with English abstract). Li, N., Chen, Y.J., Santosh, M., Pirajno, F., 2015. Compositional polarity of Triassic granitoids in the Qinling Orogen, China: Implication for termination of the northernmost paleo-Tethys. Gondwana Research, 27(1): 244-257. Li, R.X., Wang, G.W., Carranza, E.J.M., 2016. GeoCube: A 3D mineral resources quantitative prediction and assessment system. Computers & Geosciences, 89: 161-173. Li, Y.F., Mao, J.W., Guo, B.J., Shao, Y.J., Fei, H.C., Hu, H.B., 2004. Re-Os Dating of Molybdenite from the Nannihu Mo (-W) Orefield in the East Qinling and Its Geodynamic Significance. Acta Geologica Sinica (English Edition), 78(2): 463-470. Li, Z.K., Li, J.W., Zhao, X.F., Zhou, M.F., Selby, D., Bi, S.J., Sui, J.X., Zhao, Z.J., 2013. Crustal-Extension Ag-Pb-Zn Veins in the Xiong’ershan District,

Southern North China Craton: Constraints from the Shagou Deposit. Economic Geology, 108(7): 1703-1729. Lin, W.W., Peng, L.J., 1994. The estimation of Fe 3+ and Fe2+ contents in amphibole and biotite from EMPA data. J Changchun Univ Earth Sci, 24(2): 155-162 (in Chinese with English abstract). Liu, G.Y., 2007. The Pb-Zn-Ag metallogeny and prospecting target in the south marge of North China Craton. China University of Geosciences (Beijing), Beijing (in Chinese with English abstract). Liu, Y.S., Gao, S., Hu, Z.C., Gao, C.G., Zong, K.Q., Wang, D.B., 2010. Continental

and

Oceanic

Crust

Recycling-induced

Melt-Peridotite

Interactions in the Trans-North China Orogen: U-Pb Dating, Hf Isotopes and Trace Elements in Zircons from Mantle Xenoliths. Journal of Petrology, 51(1-2): 392-9. Liu, Y.S., Zong, K.Q., Kelemen, P.B., Gao, S., 2008. Geochemistry and magmatic history of eclogites and ultramafic rocks from the Chinese continental scientific drill hole: subduction and ultrahigh-pressure metamorphism of lower crustal cumulates. Chemical Geology, 247(1): 133-153. Lodders, K., Palme, H., 1991. On the chalcophile character of molybdenum: determination of sulfide/silicate partition coefficients of Mo and W. Earth and Planetary Science Letters, 103(1-4): 311-324. Lu, X.X., Yu, Z.P., Feng, Y.L., Wang, Y.T., Ma, W., Cui, H.F., 2002. Mineralization and Tectonic Setting of Deep-hypabyssal Granites in East Qinling Mountain. Mineral Deposits, 21(2): 168-178 (in Chinese with English abstract). Ludwig, K.R., 2003. ISOPLOT, a geochronological toolkit for Microsoft Excel 3.00. Mao, J.W., Xie, G.Q., Pirajno, F., Ye, H.S., Wang, Y.B., Li, Y.F., Xiang, J.F., Zhao, H.J., 2010. Late Jurassic–Early Cretaceous granitoid magmatism in Eastern Qinling, central-eastern China: SHRIMP zircon U–Pb ages and

tectonic implications. Australian Journal of Earth Sciences, 57(1): 51-78. Mao, J.W., Xie, G.Q., Zhang, Z.H., Li, X.F., Wang, Y.T., Zhang, C.Q., Li, Y.F., 2005. Mesozoic large-scale metallogenic pulses in North China and corresponding geodynamic settings. Acta Petrologica Sinica, 21(1): 169-188 (in Chinese with English abstract). Mao, J.W., Xie, G.Q., Bierlein, F., Qü, W.J., Du, A.D., Ye, H.S., Pirajno, F., Li, H.M., Guo, B.J., Li, Y.F., 2008. Tectonic implications from Re–Os dating of Mesozoic molybdenum deposits in the East Qinling–Dabie orogenic belt. Geochimica Et Cosmochimica Acta, 72(18): 4607-4626. Mao, J.W., Pirajno, F., Xiang, J.F., Gao, J.J., Ye, H.S., Li, Y.F., Guo, B.J., 2011. Mesozoic molybdenum deposits in the east Qinling–Dabie orogenic belt: Characteristics and tectonic settings. Ore Geology Reviews, 43(1): 264-293. Meng, F., 2010. The characteristics of the Laojunshan intrusive and mineralization, western Henan Province, Masters Dissertation, China University of Geoscience (Beijing), Beijing (in Chinese with English abstract). Mengason, M.J., Candela, P.A., Piccoli, P.M., 2011. Molybdenum, tungsten and manganese partitioning in the system pyrrhotite-Fe-S-O melt-rhyolite melt: Impact of sulfide segregation on arc magma evolution. Geochimica et Cosmochimica Acta, 75(22): 7018-7030. Miller, C.F., Mcdowell, S.M., Mapes, R.W., 2003. Hot and cold granites? Implications of zircon saturation temperatures and preservation of inheritance. Geology, 31(2003): 529-532. Pearce, J., 1996. Sources and Settings of Granitic Rocks. Episodes, 19(4): 120-125. Pearce, J.A., 1984. Trace Element Discrimination Diagrams for the Tectonic Interpretation of Granitic Rocks. Journal of Petrology, 25(4): 956-983. Peccerillo, A., Taylor, S.R., 1975. Geochemistry of eocene calc-alkaline volcanic rocks from the Kastamonu area, Northern Turkey. Contributions

to Mineralogy & Petrology, 58(1): 63-81. Pirajno, F., 2013. The Geology and Tectonic Settings of China's Mineral Deposits, 909-910 pp. Qi, J.P., Song, Y.W., Li, S.Q., Chen, F.K., 2009. Single, grain Rb, Sr isotopic composition of the Xigou Pb, Zn, Ag deposit Luanchuan, Henan province. Acta Petrologica Sinica, 25(11): 2843-2854 (in Chinese with English abstract). Ray, G.E., Webster, I.C.L., Ettlinger, A.D., 1995. The distribution of skarns in British Columbia and the chemistry and ages of their related plutonic rocks. Economic Geology, 90(4): 920-937. Robb, L., 2005. Introduction to ore-forming processes. Blackwell Pub, 1-373 pp. Santosh, M., 2013. Evolution of continents, cratons and supercontinents: Building the habitable Earth. Current Science, 104(7): 871-879. Shabani, A.A.T., Lalonde, A.E., Whalen, J.B., 2003. Composition of biotite from granitic rocks of the Canadian Appalachian orogen: a potential tectonomagmatic indicator?. Canadian Mineralogist, 41(3): 1381-1396. Shand, S.J., 1948. Eruptive Rocks: Their Genesis, Composition, Classification, and Their Relation to Ore Deposits, with a Chapter on Meteorites. The Journal of Geology, 2(6): 259-259. Speer, J.A., 1984. Micas in igneous rocks. Reviews in Mineralogy, 13(6): 299-356. Stone, D., 2000. Temperature and pressure variations in suites of Archean felsic plutonic rocks, Berens River area, northwest Superior Province, Ontario, Canada. Canadian Mineralogist, 38(2): 455-470. Sun, S.S., Mcdonough, W.F., 1989. Chemical and Isotopic Systematics of Oceanic Basalts; Implications for Mantle Composition and Processes. Geological Society London Special Publications, 42(1): 313-345. Tang, L., Zhang, S.T., Cao, H.W., Li, D., Zhang, X.H., Zhang, Y.H., Tian, H.H., Zhang, H., 2014. Metallogenic system and evolutionary characteristics of

Mo-W-Pb-Zn-Ag

polymetallic

metallogenic

concentration

area

in

Luanchuan, Henan, China. Journal of Chengdu University of Technology, 41(3): 356-368 (in Chinese with English abstract). Tang, L., Santosh, M., Dong, Y.P., 2015. Tectonic evolution of a complex orogenic system: Evidence from the northern Qinling belt, Central China. Journal of Asian Earth Sciences, 113: 544-559. Tao, J.H., Tao, C., Long, W.G., Li, W.X., 2015. Mineral chemistry of biotites from the Indosinian weakly peraluminous and strongly peraluminous granites in South China and their constraints on petrogenesis. Earth Science Frontiers, 22: 64-78 (in Chinese with English abstract). Uchida, E., Endo, S., Makino, M., 2007. Relationship Between Solidification Depth of Granitic Rocks and Formation of Hydrothermal Ore Deposits. Resource Geology, 57(1): 47-56. Wang, C.M., He, X.Y., Yan, C.H., Lü, W.D., Sun, W.Z., 2013. Ore geology, and H, O, S, Pb, Ar isotopic constraints on the genesis of the Lengshuibeigou Pb-Zn-Ag deposit, China. Geosciences Journal, 17(2): 197-210. Wang, G.W., Zhang, S.T., Yan, C.H., Song, Y.W., Sun, Y., Li, D., Xu, F.M., 2011. Mineral potential targeting and resource assessment based on 3D geological modeling in Luanchuan region, China. Computers & Geosciences, 37(12): 1976-1988. Wang, G.W., Zhu, Y.Y., Zhang, S.T., Yan, C.H., Song, Y.W., Ma, Z.B., Hong, D.M., Chen, T.Z., 2012. 3D geological modeling based on gravitational and magnetic data inversion in the Luanchuan ore region, Henan Province, China. Journal of Applied Geophysics, 80(5): 1-11. Wang, G.W., Li, R.X., Carranza, E.J.M., Zhang, S.T., Yan, C.H., Zhu, Y.Y., Qu, J.N., Hong, D.M., Song, Y.W., Han, J.W., 2015. 3D geological modeling for prediction of subsurface Mo targets in the Luanchuan district, China. Ore Geology Reviews, 71(1): 270-274. Wang, T., 2000. Origin of hybrid granitoids and the implications for continental dynamics. Acta Petrologica Sinica, 16(2): 161-168 (in Chinese with

English abstract). Wang, X.L., Jiang, S.Y., Dai, B.Z., Griffin, W.L., Dai, M.N., Yang, Y.H., 2011. Age, geochemistry and tectonic setting of the Neoproterozoic (ca 830 Ma) gabbros on the southern margin of the North China Craton. Precambrian Research, 190(1–4): 35-47. Watson, E.B., Harrison, T.M., 1983. Zircon saturation revisited: temperature and composition effects in a variety of crustal magma types. Earth & Planetary Science Letters, 64(2): 295-304. Wones, D.R., Eugster, H.P., 1965. Stability of biotite-experiment theory and application. American Mineralogist, 50(9): 1228-1272. Wu, F.Y., Li, X.H., Zheng, Y.F., Gao, S., 2007. Lu-Hf isotopic systematics and their application in petrology. Acta Petrologica Sinica, 23(2): 185-220 (in Chinese with English abstract). Xiang, J.F., Pei, R.F., Ye, H.S., Wang, C.Y., Tian, Z.H., 2012. Source and evolution of the ore-forming fluid in the Nannihu-Sandaozhuang Mo (W) deposit: Constraints from C-H-O stable isotope data. Geology in China, 39(6): 1778-1789 (in Chinese with English abstract). Xu, T., Zhang, S.T., Yang, B., Cao, H.W., Zhang, Y.H., Pei, Q.M., Zhang, P., Tang, C.H., Wu, Z.L., 2015. Characteristics of biotites in two types of Yanshanian granitic pluton in Luanchuan ore concentration area of China and its significance. Journal of Chengdu University of Technology, 42(3): 257-267. Xu, Y.M., Xu, Y.M., Jiang, S.Y., Zhu, Z.Y., Zhou, W., Kong, F.B., Sun, M.Z., Xiong, Y.G., 2013. Geochronology, geochemistry and mineralogy of ore-bearing and ore-barren intermediate-acid intrusive rocks from the Jiurui ore district, Jiangxi Province and their geological implications. Acta Petrologica Sinica, 29(12): 4291-4310 (in Chinese with English abstract). Yan, C.H., Liu, G.Y., 2004. Metallogenic characteristics and ore-prospecting suggestions of lead–zinc polymetallic deposits in southwestern Henan Province of China. Geological Bulletin of China, 23: 1143-1148 (in

Chinese with English abstract). Yang, F., Wang, G.W., Cao, H.W., Li, R.X., Tang, L., Huang, Y.F., Zhang, H., Xue, F., Jia, W.J., Guo, N.N., 2016. Timing of formation of the Hongdonggou Pb-Zn polymetallic ore deposit, Henan Province, China: Evidence from Rb-Sr isotopic dating of sphalerites. Geoscience Frontiers. http://dx.doi.org/10.1016/j.gsf.2016.06.001. Yang, R.Y., Xu, Z.W., Ren, Q.J., 1997. Ages and magma sources of Shi bao gou and Huo shen miao complexes in East Qinling. Bulletin of Mineralogy Petrology & Geochemistry, 16, 397-407 (in Chinese with English abstract). Yang, Y., Chen, Y.J., Zhang, J., Zhang, C., 2013. Ore geology, fluid inclusions and four-stage hydrothermal mineralization of the Shangfanggou giant Mo–Fe deposit in Eastern Qinling, central China. Ore Geology Reviews, 55(4): 146-161. Yang, Y., Wang, X.X., Ke, C.H., Li, J.B., 2012. Zircon U-Pb age, geochemistry and Hf isotopic compositions of Shibaogou granitoid pluton in the Nannihu ore district, western Henan Province. Geology in China, 39(6): 1525-1542 (in Chinese with English abstract). Zhai, M.G., Santosh, M., 2013. Metallogeny of the North China Craton: Link with secular changes in the evolving Earth. Gondwana Research, 24(1): 275-297. Zhang, G.W., Zhang, B.R., Yuan, X.C., Xiao, Q.H., 2001. Qinling orogenic belt and continental dynamics. Sci. Press, Beijing: 1-806 (in Chinese). Zhang, Y.H., 2014. Late-Mesozoic tectonic-magma evolution and its relationship with mineralization in Luanchuan County. China University of Geosciences (Beijing), Beijing: 1-79 (in Chinese with English abstract). Zhang, Y.H., Zhang, S.T., Xu, M., Jiang, X.K., Li, J.J., Wang, S.Y., Li, D., Cao, H.W., Zou, H., Fang, Yi., 2015. Geochronology, geochemistry, and hf isotopes of the jiudinggou molybdenum deposit, central china, and their geological significance. Geochemical Journal, 49(4): 321-342. Zhou, X.H., 2009. Major Transformation of Subcontinental Lithosphere

beneath North China in Cenozoic-Mesozoic: Revisited. Geological Journal of China Universities, 15(1): 1-18 (in Chinese with English abstract). Zhou, Z.X., 1986. The origin of intrusive mass in fengshandong, Hubei province. Acta Petrologica Sinica, 2(1): 59-70 (in Chinese with English abstract). Zhu, Y.D., 2014. Diagenesis and Metallogeny of Ore-bearing Granites in Tongcun Porphyry Mo-Cu Deposit, Zhejiang. China University of Geosciences (Beijing), Beijing: 1-148 (in Chinese with English abstract). Zhu, Y.D., Ye, X.F., Zhang, D.H., Wang, K.Q., 2012. A Comparative Study of Granites in Tongcun Porphyry Molybdenum-Copper Deposit in West of Zhejiang Province and Dexing Porphyry Copper Deposit. Advances in Earth Science, 27(10): 1043-1053 (in Chinese with English abstract).

Figure captions Fig. 1 (a) Tectonic map of China, showing the location of Central China belt and North China Craton; (b) the tectonic subdivision of the Qinling Orogen, showing the location of Luanchuan ore district; (c) geological map of Luanchuan ore district displaying the geology and the distribution of granites. Modified after Duan et al. (2010), Mao et al. (2011) and Yang et al. (2016). YK, Yuku;

SBG,

Shibaogou;

HBL,

Huangbeiling;

NNH,

Nannihu;

SFG,

Shangfanggou; MJ, Majuan; DP, Daping; HSM, Huoshenmiao; LJS, Laojunshan.

Fig. 2 Geological map of the Shibaogou granitic pluton, showing the locations of samples.

Fig. 3 Field photos of SBG (a, b). (a) Contact zone of fine-grained biotite monzogranite and porphyritic monzogranite; (b) diorite enclaves in porphyritic monzogranite. Photographs of typical samples of SBG and ZYK (c, d). (c) Sample from SBG, porphyritic monzogranite; (d) borehole core sample of ZYK, medium-grained monzogranite. Photomicrographs exhibiting textures and minerals of typical samples of SBG and ZYK (e, f). (e) A typical porphyritic texture of quartz+K-feldspar phenocryst and biotite+quartz+plagioclase+ K-feldspar groundmass in porphyritic monzogranite from SBG (sample S06), exhibiting the Carlsbad twins in K-feldspar and the polysynthetic twins of plagioclase. (f) Equigranular texture in medium-grained monzogranite from ZYK (sample Y06), showing euhedral strip biotite, subhedral quartz, Carlsbad twins of K-feldspar and the polysynthetic twins of plagioclase. Qtz- Quartz, KfsK-feldspar, Pl- Plagioclase, Bt- Biotite.

Fig. 4 Photomicrographs of thin sections from ZYK (a, b, c) and SBG (d, e, f). (a) Euhedral strip biotite, rhombic sphene, non-transparent magnetite and K-feldspar with surface carbonation and plagioclase of polysynthetic twins from ZYK. (b) Tabular subhedral biotite coexisting with transparent apatite and rhombic sphene inclusions. (c) Altered biotite with partly altered to chlorite in monzogranite from ZYK. (d) A primary biotite and altered biotite, part chloritization. (e) Rhombic hornblende and anhedral altered biotite enclave. (f) Anhedral biotite with apatite and sphene inclusions, showing cross hatched twins of microcline. Qtz- Quartz, Kfs- K-feldspar, Pl- Plagioclase, Bt- Biotite, Mc- Microcline, Hbl- Hornblende, Sph- Sphene, Mag- Magnetite, Ap- Apatite, Chl- Chlorite.

Fig. 5 Mg-(Fe2++Mn)-(AlVI+Fe3++Ti) ternary classification plot of biotite for the ZYK, SBG and LJS (modified after Foster, 1960). Data of LJS are from Xu et al. (2015).

Fig. 6 Geochemical classification diagrams of samples from SBG, ZYK and LJS. (a) Plot of K2O versus SiO2 (after Peccerillo and Taylor, 1975); (b) Diagram of A/NK-ASI (after Shand, 1948); (c) Plot of K2O+Na2O–CaO vs SiO2 for ZYK, SBG and LJS (after Frost et al., 2001); (d) Plot of SiO2 versus Fe*(after Frost et al., 2001). A/NK=mol [Al2O3/(Na2O+K2O)], ASI=mol [Al2O3/(Na2O+K2O+CaO)], Fe*=[FeOT/(FeOT+MgO)]. Data of LJS are from Bao et al. (2009) and the following LJS major and trace elements data have the same source.

Fig. 7 Harker diagrams of major elements of rocks from ZYK, SBG and LJS.

Fig. 8 (a), (c) and (e) are plots of primitive mantle-normalized trace element patterns. (d), (e) and (f) are chondrite-normalized rare earth element spider plots. Normalization values are from Sun and Mcdonough (1989).

Fig. 9 (a) and (b) are Zircon U-Pb concordia plots of G1 sample from ZYK. (c) Histogram of zircon age data with relative probability curve of G1 sample from ZYK. (d) Cathodoluminescence (CL) images of zircon grains of G1 sample from ZYK pluton. Yellow smaller circles are the locations for U-Pb analysis and the larger red circles are for Lu-Hf analyses. U-Pb ages in Ma and εHf(t) values are also shown.

Fig. 10 Plot of chondrite-normalized REE of zircons of G1 and the normalization values are from Sun and Mcdonough (1989).

Fig. 11 Plots indicating the redox state. (a) FeO* versus log 10 (Fe2O3/FeO) plot for rocks from ZYK, SBG and LJS, exhibiting the redox state of ZYK, SBG and LJS. FeO*= FeO+0.9*Fe2O3. Labels: VSO - very strongly oxidised, SO strongly oxidised, MO - moderately oxidised, MR - moderately reduced, SR strongly reduced (Blevin et al., 2003). (b) SiO 2 versus Fe2O3/FeO plot for rocks

from ZYK, SBG and LJS (Lehmann, 1990). (c) Fe 2+-Fe3+-Mg2+ ternary plot for composition of biotites from ZYK, SBG and LJS (Wones and Eugster, 1965). Three common oxygen fugacity buffers: Fe 2SiO4-SiO2-Fe3O4 (QFM), Ni-NiO (NNO), Fe2O3-Fe3O4 (HM).

Fig. 12 Log f(O2) - Temperature diagram for the biotite + sanidine + magnetite + gas equilibrium at Ptotal = 2070 bars (after Wones and Eugster, 1965). The detailed explanation are shown in the article.

Fig. 13 Histograms of solidification pressure values using biotite geobarometer (a) and depth values of the diagenesis based on the pressure (b) for ZYK, SBG and LJS.

Fig. 14 Plot showing relationship between the ASI of rocks and total Al content of biotite (O=22) from ZYK and SBG by metal type (after Uchida et al., 2007).

Fig. 15 Diagrams showing the composition evolution for ZYK, SBG and LJS. Fe2O3/FeO - Rb/Sr plot (Blevin et al., 2003) and K/Rb-SiO2 plot (b, after Blevin, 2004) for rocks from ZYK, SBG and LJS. UE - Unevolved, ME - moderately evolved, SE - strongly evolved.

Fig. 16 (a) FeOT/(FeOT+ MgO) vs. MgO diagram of biotite from ZYK, SBG and LJS (Zhou, 1986). C-crust source, M-C-mantle-crust mixed source, M-mantle source. (b) FeO*-Al2O3-MgO ternary plot of biotite from ZYK, SBG and LJS (Abdelrahman, 1994), discriminating the tectonic setting of rocks. A: alkaline, C: calc-alkaline, and P: peraluminous granite fields.

Fig. 17 Tectonic discrimination diagrams for ZYK, SBG and LJS samples. (a) Nb versus Y plot; (b) Ta versus Yb plot; (c) Rb versus Y+Nb plot; (d) Rb versus Yb+Ta plot (Pearce, 1996; Pearce, 1984).

Fig. 18 Plot of lg [CaO/ (K2O+Na2O)] versus SiO2 of rocks from ZYK, SBG and LJS, exhibiting the different tectonic settings (Brown, 1982).

Fig. 19 Tectonic transformation of the East Qinling orogen during Late Jurassic- Early Cretaceous (after Li et al., 2012). (a) At 157~150 Ma, transition from syn-collision stage to post-collision stage, forming the granite that they derived from lower crust triggered by lithospheric mantle delamination. (b) At ~145 Ma, tectonic regime began to translate from compression to extension, forming Mo-bearing granites ascend to the upper crust heated by the slab melts. (c) Post-orogeny stage ends in the East Qinling, with the formation of the LJS, ore-unrelated batholith, at about 110 Ma.

Table captions Supplementary Table 1 Major and trace element compositions of the SBG, wt. % for major elements and ppm for trace elements.

Supplementary Table 2 Major and trace element compositions of the ZYK , wt. % for major elements and ppm for trace elements.

Supplementary Table 3 Electron microprobe analyses (wt. %) and structural formulae (apfu) of representative primary biotites from SBG.

Supplementary Table 4 Electron microprobe analyses (wt. %) and structural formulae (apfu) of representative primary biotites from ZYK.

Table 1 LA-MC-ICPMS zircon U-Pb data of sample G1 sample from ZYK.

Table 2 Zircon trace element concentrations (ppm) of G1 sample.

Table 3 LA-MC-ICPMS zircon Hf isotopic compositions of the G1 sample.

Table 4 Isotopic ages recorded in granitic plutons and typical deposits in the Luanchuan ore district (modified after Cao et al., 2015, Li et al., 2015 and Yang et al., 2016).

Table 1

Sample

Isotope ratios (±1σ)

Element concentration (ppm)

Age (Ma±1σ) Concordance(%)

spots Pb*

232

Th

238

U

Th/U

207

206

Pb/

Pb

207

235

Pb/

U

206

238

Pb/

U

207

206

Pb/

Pb

207

235

Pb/

U

206

238

Pb/

U

G1-01

18.07

292.02

611.85

0.48

0.04906±0.00319

0.16472±0.01073

0.02435±0.0006

151±149

155±9

155±4

100

G1-02

36.97

595.12

1387.31

0.43

0.05066±0.0042

0.15859±0.01496

0.0227±0.00057

226±192

149±13

145±4

97

G1-03

34.14

648.53

1272.70

0.51

0.06292±0.00385

0.19148±0.01171

0.02207±0.00051

706±144

178±10

141±3

79

G1-04

35.46

700.04

1368.07

0.51

0.05114±0.00305

0.1557±0.00929

0.02208±0.00051

247±147

147±8

141±3

96

G1-05

25.64

409.52

920.45

0.44

0.04866±0.00432

0.15235±0.01528

0.02271±0.00057

131±203

144±13

145±4

99

G1-06

36.76

665.33

1313.23

0.51

0.04904±0.00293

0.15762±0.00949

0.02331±0.00054

150±143

149±8

149±3

100

G1-07

20.45

620.48

733.09

0.85

0.0528±0.00367

0.17798±0.01234

0.02445±0.0006

320±172

166±11

156±4

94

G1-08

65.84

1493.83

2330.33

0.64

0.04989±0.00517

0.14989±0.01755

0.02179±0.00055

190±236

142±15

139±3

98

G1-09

22.28

610.88

737.37

0.83

0.05637±0.00374

0.17806±0.01162

0.02291±0.00055

467±162

166±10

146±3

88

G1-10

52.80

2742.51

1424.70

1.92

0.04799±0.01066

0.1544±0.03776

0.02333±0.00075

99±371

146±33

149±5

98

G1-11

40.04

665.62

1383.31

0.48

0.05487±0.00327

0.18508±0.01094

0.02446±0.00056

407±146

172±9

156±4

91

G1-12

36.50

713.79

1339.84

0.53

0.04986±0.00316

0.15813±0.00981

0.023±0.00053

189±153

149±9

147±3

99

G1-13

28.02

475.50

1036.85

0.46

0.04689±0.00359

0.15424±0.01144

0.02386±0.00059

44±173

146±10

152±4

96

G1-14

29.91

774.98

986.16

0.79

0.05236±0.00365

0.17536±0.01222

0.02429±0.0006

301±172

164±11

155±4

95

G1-15

40.34

1066.91

1285.77

0.83

0.05451±0.00333

0.18403±0.01111

0.02448±0.00056

392±151

172±10

156±4

91

G1-16

36.81

449.25

1247.77

0.36

0.05223±0.00328

0.19546±0.01239

0.02714±0.00065

295±155

181±11

173±4

96

G1-17

51.41

1692.77

1770.46

0.96

0.05183±0.00404

0.18028±0.014

0.02523±0.00065

278±184

168±12

161±4

96

G1-18

43.85

918.60

1582.95

0.58

0.05446±0.00357

0.17327±0.01118

0.02308±0.00054

390±162

162±10

147±3

91

G1-19

29.35

431.30

999.15

0.43

0.04989±0.00486

0.16225±0.01761

0.02359±0.0006

190±226

153±15

150±4

98

G1-20

32.19

533.22

1178.76

0.45

0.05106±0.00819

0.16447±0.02895

0.02336±0.0007

244±323

155±25

149±4

96

G1-21

17.54

422.37

603.64

0.70

0.05179±0.00367

0.16583±0.01172

0.02322±0.00056

276±174

156±10

148±4

95

G1-22

27.54

325.78

951.33

0.34

0.05148±0.00491

0.17334±0.01777

0.02442±0.00061

263±224

162±15

156±4

96

G1-23

57.94

759.87

1925.42

0.39

0.04895±0.00372

0.16716±0.01442

0.02477±0.0006

146±173

157±13

158±4

99

G1-24

40.72

802.74

1481.29

0.54

0.05221±0.00327

0.16856±0.01056

0.02341±0.00053

295±155

158±9

149±3

94

Table 2

Sample

La

Ce

Pr

Nd

Sm

Eu

Gd

Tb

Dy

Ho

Er

Tm

Yb

Lu

δEu

δCe

G1-01

0.112

28.678

0.080

0.493

1.157

0.553

6.802

2.378

34.026

15.617

86.565

22.791

260.266

61.716

0.469

71.464

G1-02

0.153

39.649

0.123

0.526

1.112

0.557

6.844

2.543

37.254

18.378

112.224

31.391

394.348

103.160

0.474

66.891

G1-03

3.763

40.390

1.184

5.902

4.015

1.119

12.838

3.274

38.925

15.684

83.449

21.084

245.171

62.290

0.435

4.657

G1-04

0.002

37.993

0.080

1.840

3.133

0.962

15.368

5.188

65.762

30.185

167.084

44.264

510.815

127.039

0.348

145.270

G1-05

0.138

36.043

0.139

1.192

1.383

0.468

8.312

2.663

38.395

18.102

106.834

29.818

362.874

93.342

0.326

57.616

G1-06

0.000

34.724

0.033

0.386

1.147

0.330

6.347

2.081

28.950

13.646

78.726

21.516

266.649

66.717

0.297

322.967

G1-07

1.122

55.648

0.277

2.213

1.807

0.711

11.910

4.403

54.599

23.001

116.066

27.540

284.704

60.480

0.351

23.757

spots

G1-08

4.554

79.568

1.538

9.261

7.480

2.627

20.623

6.399

73.593

30.473

157.501

40.776

478.039

113.773

0.607

7.345

G1-09

1.270

52.387

0.308

2.140

1.590

0.676

9.802

3.883

51.277

21.493

112.135

27.409

293.237

65.150

0.401

19.905

G1-10

0.157

44.614

0.125

0.817

1.505

0.583

9.045

3.155

45.422

20.282

124.674

34.573

420.514

106.547

0.373

110.991

G1-11

0.078

41.291

0.090

0.829

1.148

0.586

7.889

2.874

37.602

17.390

100.876

27.332

336.110

88.168

0.440

105.363

G1-12

0.022

37.029

0.035

0.753

1.134

0.454

6.803

2.335

31.296

14.315

83.392

22.237

276.192

71.950

0.386

263.619

G1-13

0.017

33.626

0.031

0.538

0.920

0.438

5.764

2.217

30.440

14.397

84.164

23.262

289.146

73.528

0.444

275.022

G1-14

0.010

63.737

0.060

0.928

2.539

0.875

14.028

4.895

68.423

29.566

160.534

40.612

439.141

100.322

0.356

308.395

G1-15

0.017

64.504

0.078

1.136

1.831

0.733

10.992

4.344

57.958

25.293

135.275

34.971

379.531

86.667

0.386

256.416

G1-16

0.029

33.272

0.033

0.516

0.860

0.365

5.982

2.289

32.079

15.634

94.285

26.989

342.169

92.323

0.363

233.895

G1-17

0.014

79.217

0.054

2.166

2.703

0.951

15.158

4.773

61.837

26.112

135.384

33.984

372.437

85.104

0.359

511.191

G1-18

0.031

51.577

0.063

0.959

1.464

0.667

10.247

3.572

46.653

21.731

123.724

34.559

422.075

108.989

0.387

252.592

G1-19

0.025

31.274

0.046

0.376

0.844

0.416

5.296

2.057

28.269

13.183

78.237

21.898

268.001

70.385

0.459

171.692

G1-20

7.717

50.078

1.581

6.043

1.838

0.548

7.587

2.105

31.062

14.181

84.341

22.802

286.736

74.427

0.386

3.326

G1-21

0.000

37.692

0.035

0.598

1.038

0.370

7.348

2.569

37.866

16.257

88.024

22.035

248.045

56.758

0.300

336.417

G1-22

0.118

31.828

0.084

0.992

1.019

0.490

6.633

2.262

32.136

15.336

93.141

26.701

332.637

89.231

0.434

75.365

G1-23

0.251

58.899

0.171

1.042

2.245

0.658

11.391

4.003

56.237

26.577

156.959

43.305

537.917

142.223

0.324

67.277

G1-24

0.122

38.808

0.119

0.893

0.894

0.657

7.560

2.425

33.968

14.951

85.959

23.048

282.250

71.542

0.531

71.690

Table 3

Sample spots

176

Hf/177Hf

176

Lu/177Hf

176

Yb/177Hf

Age(Ma)

εHf(0)

εHf(t)

TDM1(Ma)

TDM2(Ma)

fLu/Hf

G1-06

0.282142

0.001051

0.027104

149

-22.29384

-19.13294

1566.416

2123.498

-0.968351

G1-09

0.282179

0.002853

0.086536

146

-20.959

-18.03544

1589.437

2060.018

-0.914071

G1-10

0.282206

0.002772

0.083200

149

-20.01312

-17.02113

1546.846

2006.748

-0.916496

G1-13

0.282206

0.001371

0.033239

152

-20.0073

-16.81411

1488.896

1998.392

-0.958694

G1-18

0.282175

0.000956

0.022688

147

-21.10805

-17.98002

1515.887

2058.741

-0.971218

G1-19

0.282162

0.000886

0.021450

150

-21.57606

-18.37731

1531.474

2082.902

-0.973319

G1-20

0.282162

0.001340

0.030336

149

-21.57765

-18.44504

1550.042

2085.612

-0.959635

G1-21

0.282126

0.001299

0.036813

148

-22.86042

-19.74521

1599.182

2156.159

-0.960885

G1-24

0.282182

0.001347

0.032095

149

-20.87361

-17.74142

1522.353

2046.997

-0.959434

Table 4 Deposits/granites

Sample Types

Methods

Age (Ma)

Reference

(Xiang et al., 2012)

Porphyry–skarn Mo–W deposit Nannihu

Sandaozhuang

Shangfanggou

Molybdenite

Re–Os

143.9 ± 2.1

Molybdenite

Re–Os

144.4 ± 2.2

Molybdenite

Re–Os

145.8 ± 2.3

Molybdenite

Re–Os

145.8 ± 2.2

Molybdenite

Re–Os

143.4 ± 2.0

Molybdenite

Re–Os

139.3 ± 2.3

(Mao et al., 2008)

Molybdenite

Re–Os

144.8 ± 2.1

(Li et al., 2004)

Molybdenite

Re–Os

145 ± 2.2

(Li et al., 2004)

Molybdenite

Re–Os

143.5 ± 2.9

(Mao et al., 2008)

Molybdenite

Re–Os

144.2 ± 1.5

Molybdenite

Re–Os

143.8 ± 1.8

Molybdenite

Re–Os

144.6 ± 2.5

Molybdenite

Re–Os

146.5 ± 2.3

Molybdenite

Re–Os

146.0 ± 2.3

Molybdenite

Re–Os

144.5 ± 2.3

Molybdenite

Re–Os

146.0 ± 2.2

Molybdenite

Re–Os

144.8 ± 2.1

(Li et al., 2004)

Molybdenite

Re–Os

142.9 ± 1.6

(Mao et al., 2008)

(Xiang et al., 2012)

Molybdenite

Re–Os

141.8 ± 3.6

Molybdenite

Re–Os

146.9 ± 2.1

Molybdenite

Re–Os

145.9 ± 2.1

Molybdenite

Re–Os

147.1 ± 2.1

Molybdenite

Re–Os

146.3 ± 2.2

Molybdenite

Re–Os

146.7 ± 2.2

Molybdenite

Re–Os

144.6 ± 2.2

Majuan

Molybdenite

Re–Os

141.8 ± 2.1

(Li et al., 2007)

Dongyuku

Molybdenite

Re–Os

146.6 ± 0.9

(Zhang, 2014)

Jiudinggou

Molybdenite

Re–Os

141 ± 2.5

Dawanggou

Molybdenite

Re–Os

147.3 ± 2.5

Molybdenite

Re–Os

146.8 ± 2.3

Molybdenite

Re–Os

147.5 ± 2.2

Molybdenite

Re–Os

147.5 ± 2.1

Molybdenite

Re–Os

142.9 ± 1.9

Molybdenite

Re–Os

141.5 ± 2.0

Yuku

(Li et al., 2015)

(Mao et al., 2008)

Hydrothermal-vein Pb–Zn–Ag deposit Lengshuibeigou

Quartz

Ar–Ar

136.1 ± 0.4

(Wang et al., 2013)

Sandaogou

Sphalerite

Rb–Sr

137.3 ± 5.4

(Cao et al., 2015)

Xigou

Sphalerite

Rb–Sr

137.7 ± 5.7

Hongdonggou

Sphalerite

Rb–Sr

135.7 ± 3.2

Ore-related granites

(Yang et al., 2016)

Nannihu

Shangfanggou

Shibaogou

Granite porphyry,Zircon

LA-ICP-MS U–Pb

146.7 ± 1.2

(Xiang et al., 2012)

Granite porphyry,Zircon

LA-ICP-MS U–Pb

145.2 ± 1.5

Granite porphyry.Zircon

LA-ICP-MS U–Pb

176.3 ± 1.7

Granite porphyry.Zircon

LA-ICP-MS U–Pb

158.2 ± 1.2

Granite porphyry.Zircon

LA-ICP-MS U–Pb

145.7 ± 1.2

Porphyritic granite,Zircon

LA-ICP-MS U–Pb

149.6 ± 0.4

(Bao et al., 2014)

Granite porphyry.Zircon

SHRIMP U–Pb

157 ± 3

(Mao et al., 2010)

Porphyritic granite,Zircon

SHRIMP U–Pb

158.2 ± 3.1

(Mao et al., 2005)

Granite porphyry.Zircon

LA-ICP-MS U–Pb

135.4 ± 0.3

(Bao et al., 2014)

Granite porphyry.Zircon

SHRIMP U–Pb

158 ± 3

(Mao et al., 2010)

Porphyritic granite,Zircon

SHRIMP U–Pb

157.6 ± 2.7

(Mao et al., 2005)

Granite porphyry.Zircon

LA-ICP-MS U–Pb

135.4 ± 0.3

(Bao et al., 2009)

Porphyritic granite,Zircon

LA-ICP-MS U–Pb

153.2 ± 1.3

(Li et al., 2015)

Monzonite granite,Zircon

LA-ICP-MS U–Pb

156 ± 1

(Yang et al., 2012)

Monzonite granite,Zircon

LA-ICP-MS U–Pb

157 ± 1

Monzonite granite,Zircon

SHRIMP U–Pb

147.2 ± 1.7

SHRIMP U–Pb

145.3 ± 1.4

Monzonite granite,Zircon

SHRIMP U–Pb

150.3 ± 1.5

(Liu, 2007)

Granite porphyry.Zircon

LA-ICP-MS U–Pb

150.5 ± 0.8

(Zhang, 2014)

Granite porphyry.Zircon

LA-ICP-MS U–Pb

154.1 ± 1.8

Granite porphyry.Zircon

LA-ICP-MS U–Pb

148.3 ± 1

(Bao et al., 2014)

Syenogranite porphyry, Zircon

Yuku

Granite porphyry.Zircon

LA-ICP-MS U–Pb

154.1 ± 1.8

(Li et al., 2015)

Granite porphyry.Zircon

LA-ICP-MS U–Pb

148.3 ± 1.0

Zhongyuku

Monzonite granite,Zircon

LA-ICP-MS U–Pb

149.6±2.4

This paper

Daping

Granite porphyry.Zircon

LA-ICP-MS U–Pb

141.2 ± 0.5

(Zhang, 2014)

Graphical abstract

Highlights

 U-Pb age of zircons from the Zhongyuku granitic pluton yields an age of 149.6±2.4 Ma.  Tectono-magmatic and metallogenic events of the East Qinling orogen during Late Jurassic- Early Cretaceous.  Results

from

petrology,

mineral

chemistry,

and

zircon

U-Pb

geochronology were used to evaluate the physico-chemical conditions, compositional characteristics, petrogenesis and tectonic setting of the intrusions and evaluate their implication and mineral exploration.