Geochronology and origin of the Qi189 porphyry gold deposit in Qiyugou Orefield, Qinling Orogen, China

Ore Geology Reviews 114 (2019) 103121

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Geochronology and origin of the Qi189 porphyry gold deposit in Qiyugou Orefield, Qinling Orogen, China Nan Qia, Pin Wangb, Jie Yua, Yan-Jing Chena, a b

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MOE Key Laboratory of Crust and Orogen Evolution, School of Earth and Space Sciences, Peking University, Beijing 100871, China CAS Key Laboratory of Ocean and Marginal Sea Geology, South China Sea Institute of Oceanology, Chinese Academy of Sciences, Guangzhou 510301, Guangdong, China

A R T I C LE I N FO

A B S T R A C T

Keywords: Zircon U–Pb age Re–Os age Qi189 porphyry gold deposit Qiyugou Orefield Qinling Orogen

The Qi189 gold deposit is a recently discovered porphyry system in the Qiyugou Orefield, located in the northeastern Qinling Orogen along the southern margin of North China Craton. The orebodies are hosted in the porphyritic granite emplaced in the Taihua Supergroup. Three molybdenite and five pyrite samples from the ores yield Re–Os isochron ages of 129.5 ± 2.8 Ma and 127.5 ± 8.2 Ma, respectively, which are coincident with the zircon U–Pb age of the porphyritic granite within analytical error (128.6 ± 0.8 Ma). Zircon grains from the post-ore quartz monzonite yield weighted mean 206Pb/238U age of 124.7 ± 0.6 Ma (n = 31, 1σ, MSWD = 0.23). These ages constrain that the Qi189 gold system was formed in the period of 130–127 Ma. The porphyritic granite and quartz monzonite show high-K calc-alkaline affinity, enrichment of LREE and LILE, depletion of HREE and HFSE, and negligible Eu anomaly. Zircon grains show negative εHf(t) values of −20.7 to −14.9, with TDM2(Hf) ages of 2.49–2.13 Ga. This indicates that the Qi189 porphyry system originated from a source mixed by the materials from the North Qinling Accretion Belt and the basement of North China Craton, with minor contribution from the mantle, and developed under a post-collisional tectonic setting.

1. Introduction The majority of porphyry deposits are considered to be formed in subduction-related magmatic arcs (Sillitoe, 1972; Pirajno, 2009; Richards, 2011). However, most of the porphyry-type Mo-only or Modominated poly-metallic deposits in the eastern Qinling Orogen, Dabie Shan and other areas have been reported in syn- to post-collisional tectonic settings (Chen et al., 2000, 2007, 2017a,b; Li et al., 2007; Chen and Li, 2009; Li et al., 2012a; Li et al., 2013). This shows that continental collision regime and/or intra-continental settings are also favorable for porphyry deposits including Mo, Sn, W, and Cu. Nevertheless, few porphyry Au deposits have been reported in the Qinling Orogen and other collisional orogens. The Qinling Orogen hosts the second largest Au province in China (Chen et al., 2009a). The Au deposits in Qinling Orogen are mainly classified as orogenic-type (e.g. Shanggong, Dahu, Wenyu, and Qiangma; Chen et al., 2004a; Ni et al., 2012; Zhou et al., 2014a; Zhou et al., 2015), Carlin-type represented by Yangshan and Jinlongshan (Chen et al., 2004b; Li et al., 2007) and breccia pipes-type exemplified by Qiyugou and Dianfang deposits (Fan et al., 2000, 2011; Guo et al., 2007; Chen et al., 2009b; Li et al., 2012b; Tian et al., 2017). Recently, the Qi189 porphyry Au deposit has been discovered in the Qiyugou

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Orefield (Qi et al., 2019). As a new type of gold mineralization in the orefield, it has been proven to contain a reserve of 8.03 t Au metal, grading at 2.15 g/t (Zhang and Chen, 2018), and is potential for future exploration in the Qiyugou Orefield. In this contribution, we report isotope ages obtained from the porphyry-type deposit for the first time, including the molybdenite and pyrite Re–Os isochron ages, and the zircon U–Pb ages from the syn-ore and post-ore intrusions. We also present a systematic geochemical dataset for the syn-ore porphyritic granite and post-ore quartz monzonite, including zircon Hf isotope composition, whole rock major and trace element contents, and thereby, define the genesis and tectonic setting of the porphyry Au system. 2. Regional geology The Qinling Orogen is the central portion of the E-W-trending Central China Orogen (CCO) that evolved from the northernmost PaleoTethys Ocean and was finally built up by the Mesozoic Collision between the North China Craton (NCC) and Yangtze Craton (Fig. 1a; Zhang et al., 2001; Chen et al., 2009a; Dong et al., 2011; Zheng et al., 2013; Li et al., 2015b, 2018; Zhou et al., 2016). The Qinling Orogen is composed of four tectonic units from north to south: the Huaxiong

Corresponding author at: Key Laboratory of Crustal and Orogenic Evolution, Peking University, Beijing 100871, China. E-mail addresses: [email protected], [email protected] (Y.-J. Chen).

https://doi.org/10.1016/j.oregeorev.2019.103121 Received 6 May 2019; Received in revised form 22 August 2019; Accepted 10 September 2019 Available online 11 September 2019 0169-1368/ © 2019 Elsevier B.V. All rights reserved.

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Fig. 1. Generalized geological maps showing (a) the major tectonic subdivisions of China, with the location of Qinling Orogen; (b) tectonic framework of the Qinling Orogen; (c) distribution of ore deposits in the Xiong’ershan region, with the location of the Qiyugou Orefield (modified after Chen et al., 2009b, and references therein; Li et al., 2014). Abbreviation for faults: SBF, Sanmenxia-Baofeng Fault; MF, Machaoying Fault; LF, Luanchuan Fault; SDF, Shangdan Fault; STF, SanmenTieluping Fault; KQF, Kangshan-Qiliping Fault; HQF, Hongzhuang-Qingangping Fault; TMF, Taocun-Mayuan Fault. For pluton: JSM, Jinshanmiao; HP, Haoping; WZS, Wuzhangshan. For deposits: a, Shagou (Ag-Pb-Zn); b, Haopinggou (Ag-Zn); c, Tieluping (Ag-Pb); d, Xiaochigou (Au); e, Kangshan (Au-Ag); f, Shanggong (Au); g, Hugou (Au); h, Hongzhuang (Au); I, Qingangping (Au); j, Tantou (Au); k, Yaogou (Au); l, Qianhe (Au); m, Leimengou (Mo); n, Qiyugou (Au).

overlain by the Late Paleozoic to Early Mesozoic sediments. The basement is composed of volcanic-sedimentary assemblages commonly metamorphosed to greenschist to amphibolite facies (Ling et al., 2008; Dong et al., 2011). The overlying strata include Neoproterozoic clasticcarbonate sediments, Cambrian–Ordovician carbonate rocks, Silurian shales, Devonian to Carboniferous clastic-carbonate sediments and Permian–Triassic sandstones intercalated with limestones (Dong et al., 2011; Chen and Santosh, 2014; Zhang et al., 2014). The Xiong’er Terrain is bounded by the Machaoying Fault to the south and the San-Bao Fault to the north (Fig. 1c). The EW-trending Machaoying Fault has been interpreted as a north-dipping thrust zone formed during a Mesozoic continental collision (Chen and Fu, 1992; Zhang et al., 1998; Chen et al., 2004b). Its subsidiary faults are commonly NE- to NNE-trending compressive shears, and generally spaced at more or less regular intervals and spatially control the locations of mineral systems and shallow intrusions (Fig. 1c; Chen et al., 2009b; Li et al., 2011). Structural analysis shows that these NE-trending structures have undergone early compression, followed by a tensional regime and late extensional shearing (Chen et al., 2008). The regional San-Bao Fault is regarded as the reverse boundary thrust of the Qinling Orogen. The main lithostratigraphic units in the Xiong’er Terrain are the basement of Late Neoarchean-Paleoproterozoic Taihua Supergroup and

Block representing the reactivated southern margin of the NCC, the North Qinling Accretion Belt, South Qinling Fold Belt, and a foreland fold-and-thrust belt (e.g., Songpan Fold Belt) along the northern margin of the Yangtze Craton, with the San-Bao, Luanchuan, Shang-Dan, MianLue and Longmenshan faults as their boundaries (Fig. 1b; Chen and Santosh, 2014). The Huaxiong Block is the reactivated southernmost margin of the North China Craton, which is bounded by the Luanchuan Fault to the south and the San-Bao Fault to the north (Fig. 1b). The Huaxiong Block includes several terrains characterized by the Early Precambrian crystalline basement, i.e., eastwardly termed Lantian, Xiaoqingling, Xiaoshan, Xiong’er, Lushan, and Wuyang terrains (Fig. 1b; Chen and Fu, 1992). The North Qinling Acceretion Belt is mainly composed of the ophiolite slices within the Kuanping Group, the metamorphosed sedimentary and volcanics of the Erlangping Group with ages ranging from Neoproterozoic to Ordovician, the amphibolite to granulite facies metamorphic rocks of Qinling Group with ages in the range of Paleoproterozoic to Early Paleozoic, and the Songshugou Proterozoic ophiolite from north to south, separated from each other by thrusts or ductile shear zones (Chen and Fu, 1992; Dong et al., 2011; Zhou et al., 2016 and references therein). The South Qinling Fold Belt consists of a Precambrian basement 2

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amphibolite), Paleoproterozoic Xiong’er Group volcanic rocks and Mesozoic granitic rocks. The clasts range in size from a few centimeters to meters, with angular to round shapes, suggesting multiple phases of hydraulic fracturing (Zhang et al., 2007). The orebodies of Qi189 deposit are hosted in the porphyritic granite near No. 4 and No. 5 breccia pipes, with an average grade of 2.15 g/t Au (Zhang and Chen, 2018). The ore-hosting porphyritic granite occurs along the NW-trending faults, and dips to the northeast at 85°–90°, intruding the gneisses of Taihua Supergroup. It was discovered by the underground tunneling at a depth of 580 m to 280 m above sea level (ASL, Fig. 3), striking 370 m with a width of 150–164 m (Fig. 2). The porphyritic granite contains 70–80 vol% phenocrysts consisting of Kfeldspar, plagioclase and quartz, with the matrix composed of quartz, Kfeldspar and plagioclase (Fig. 4a,b). Accessory minerals include sphene, apatite, and zircon. The ore-hosting porphyritic granite is crosscut by post-ore quartz monzonite dike (Fig. 2) that displays fine- to mediumgrain subhedral texture (Fig. 4c, d) and is mainly composed of K-feldspar, plagioclase, quartz and hornblende, with accessory minerals of sphene, zircon and apatite. The ores are altered porphyritic granite. Prime ore minerals are pyrite, native gold (Fig. 5a) and electrum, with minor chalcopyrite, galena, molybdenite (Fig. 5b), and telluride. Gold and telluride are mainly observed within pyrite and quartz as inclusions (Fig. 5f) and fissure-fillings (Fig. 5h, i). Gangue minerals are quartz, K-feldspar, sericite, chlorite, epidote, and calcite. According to crosscutting relationships of veinlets, the hydrothermal alteration and mineralization can be divided into four stages characterized by mineral assemblages of (1) quartz-K-feldspar, (2) quartz-pyrite-molybdenite (Fig. 5b,g), (3) quartz-polymetallic sulfides and (4) quartz-carbonate. The quartz-polymetallic sulfide stage is most crucial to gold mineralization. Wall-rock alteration minerals associated with the stockworks at the Qi189 gold deposit are K-feldspar, quartz, biotite, sericite, epidote, chlorite and carbonate (Fig. 5c,d), outwardly forming potassic, phyllic, propylitic zones from the core of the porphyritic granite (Fig. 5c,e).

the cover of the Statherian (1.8–1.6 Ga) Xiong’er Group (Chen et al., 2004a). The Taihua Supergroup is a suite of metamorphic volcanicsedimentary sequence, and divided into the Caogou (biotite plagioclase gneiss, 3.0–2.55 Ga), Shibangou (amphibolite-bearing gneiss, amphibolite, biotite-plagioclase gneiss and granulite, 2.5–2.3 Ga) and Duangou Formations (khondalite series, 2.3–2.1 Ga; Chen and Zhao, 1997; Li et al., 2015b). The Xiong’er Group, unconformably overlying the Taihua Supergroup, is divided into the Dagushi, Xushan, Jidanping and Majiahe formations in ascending sequence (Hu et al., 1988; Zhao et al., 2009). It is composed predominantly of basaltic andesite and dacite, followed by rhyolite and andesitic basalt, interlayered with minor sedimentary rocks (Sun et al., 1985; Deng et al., 2013a,b). As indicated by isotope ages including SHRIMP and LA-ICP-MS zircon U–Pb dates, the Xiong’er Group volcanic rocks erupted mainly at 1.78–1.75 Ga, but intermittently over a protracted interval from 1.84 Ga, through 1.76–1.75 Ga and 1.65 Ga, to 1.45 Ga (Hu et al., 1988; Sun et al., 1991; Zhao et al., 2009). The tectonic setting of the Xiong’er Group is still debated between continental rift (Sun et al., 1985) or mantle plume (Zhao et al., 2002; Peng et al., 2008), and Andean-type continental arc (Hu et al., 1988; Zhao et al., 2009; Deng et al., 2013a, b). A few researchers also suggested an Andean-type continental arc setting coexisting with a simultaneously passive continental rift (Chen and Fu, 1992). The Xiong’er Group volcanic sequence is unconformably overlain by the Mesoproterozoic clastic-carbonate rocks of the Ruyang Group and Guandaokou Group along the northern and southern margins of the Xiong’er Terrain, respectively. Intrusions in the Xiong’er Terrain are characterized by the Yanshanian granite batholiths which are usually associated with gold mineralization (Li et al., 2018 and references therein), including Wuzhangshan pluton (163–156 Ma; Li, 2005; Han et al., 2007;), Huashan Complex (143–128 Ma; Guo et al., 2009; Gao et al., 2010; Mao et al., 2010; Nie et al., 2015), and Heyu Complex (148–133 Ma; Guo et al., 2009; Gao et al., 2010; Li et al., 2012c). Moreover, a number of smallsized porphyries and breccia pipes are genetically and spatially associated with important mineral systems in both the Xiong’er Terrain and the whole Huaxiong Blocks, as exemplified by Shangfanggou (158–135 Ma; Bao et al., 2009; Mao et al., 2010; Yang et al., 2013, 2017), Nannihu-Sandaozhuang (158–145 Ma; Xiang et al., 2012; Yang et al., 2012), Leimengou (143–125 Ma; Li et al., 2006; Deng et al., 2014), Jinduicheng (143–140 Ma; Zhu et al., 2008; Jiao et al., 2010) and Qiyugou (150–134 Ma; Yao et al., 2009; Deng et al., 2014).

4. Sampling and analytical methods 4.1. Samples Six porphyritic granite and eight quartz monzonite samples collected from tunnels at levels of 280, 340, 400 and 580 m ASL (above sea level) are used for major and trace element analyses (Table 1). One quartz monzonite sample (ZR-3) is used for U–Pb dating (Table 2) and Hf isotope analysis. Three molybdenite samples and five pyrite samples from the ores are selected for Re–Os isotopic analyses. Molybdenite samples are separated from the quartz-molybdenite stockworks (400A-4, 280B-1 and 280C-1) where molybdenite occurs as coarse-grained flakes. Pyrite samples (280A-5, 280A-5b, 400A-7, 400A-7b and 580B-1) are selected from the quartz-polymetallic sulfide veins.

3. Deposit geology The Qiyugou Orefield includes at least ten auriferous breccia pipes on the west side of a Cenozoic basin bounded by Taocun–Mayuan Fault (Fig. 2). It is widespread of the Taihua Supergroup, followed by the Xiong’er Group and Yanshanian intrusive rocks (Fig. 2). The Taihua Supergroup is mainly composed of hornblende-plagioclase gneiss, while the Xiong’er Group consists of andesite, basaltic andesite, and andesitic porphyrite. These rocks are intruded by granite porphyry, quartz porphyry, diorite and porphyritic granite (Fig. 2). The quartz porphyries in the Qiyugou Orefield present as small-sized dikes and stocks and yield LA-ICP-MS zircon U-Pb age of 150 ± 1 Ma (Deng et al., 2014). The granite porphyry yields LA-ICP-MS zircon U-Pb ages of 136 ± 2 Ma (Li et al., 2006) and 134 ± 2 Ma (Yao et al., 2009). The porphyritic granite with LA-ICP-MS zircon U-Pb age of 128.6 ± 0.8 Ma (Zhang and Chen, 2018) hosts gold mineralization of the Qi189 deposit and locally presents as ores if strongly altered. The NW- and NE-trending faults formed by NE-SW and NW-SE compression in the Mesozoic (Gao et al., 1994; Chen et al., 2009b) controlled the spatial distribution and occurrence of the breccia pipes and related porphyry dikes and stocks. The pipes are spindle or elliptical in plan with long axes ranging from < 40 m to > 1 km and have been traced vertically for more than 300 m. The breccia pipes contain clasts of Early Precambrian basement rocks (migmatite, gneiss and

4.2. Major and trace element analysis Major element analyses were performed by a PANalytical Axios Xray fluorescence spectrometer (XRF) at the ALS Chemex (Guangzhou) Co. Ltd., and details of the procedures were given by Lee (1997). Trace element analyses were performed using an ICP-MS at the ALS Chemex (Guangzhou) Co. Ltd., and detailed analytical procedures were given by Zhou et al. (2014b). Accuracies of analyses are within 5% for major elements and within 10% for trace elements. 4.3. LA-ICP-MS zircon U–Pb dating Zircons were separated by conventional heavy liquid and magnetic separation techniques and then handpicked under the binocular 3

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111°56

111°57

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men

189 J4

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gou

D10 34°12

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J19

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Andesite of Xiong’er Gp.

Gneiss of Taihua Sgp.

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Quartz monzonite

Diorite

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Breccia pipe and its number

Quartz porphyry

Granite porphyry

Fault zone

Fault

Village

Fig. 2. Simplified geological map of the Qiyugou Orefield (modified after Chen et al., 2009b; Deng et al., 2014).

for preparing to mix the spike were acquired from Oak Ridge National Laboratory. The weighted sample is loaded in a carius tube through a thin neck long funnel. The weighted 190Os–185Re spike and 3 mL HCl, 5 mL HNO3 and 1 mL H2O2 are loaded when the bottom of the tube is frozen during the −50 to −80 °C in an ethanol-liquid nitrogen slush. The top is sealed using a natural gas torch, and then the tube is placed in a stainless-steel jacket and heated for 24 h at 230 °C. Upon cooling, keeping the bottom of tube frozen, and then we break the neck of the tube. The Os is separated by the method of direct distillation from carius tube for 50 min and is trapped in 5 mL 50% HBr. Then the HBr solution containing Os is purified by the micro-distillation method (Creaser et al., 1991). The purified solution is used for the N-TIMS (Triton plus) determination of Os isotope ratio. The residual Re-bearing solution is saved in a 150 mL Teflon beaker for Re separation. The residual Re-bearing solution is heated to near-dryness twice. 10 mL of 25% NaOH is added to the residue followed by Re extraction with 10 mL of acetone in a 120 mL Teflon separation funnel. Discarding the water phase and washing the acetone phase with 2 mL of 25% NaOH. Transfer the acetone phase to 100 mL beaker that contains 2 mL of water. Evaporating to dryness, and picked up in 2% HNO3 that is used for the N-TIMS (Triton plus) determination of Re isotope ratio. Average blanks for the method are ~3 pg Re and ~0.5 pg Os. The analytical reliability was tested by analyses of Certified Reference Materials JCBY. Model ages were calculated using the equation: t = [Ln (1 + 187Os/187Re)]/λ, and λ = 1.666 × yr−1 (Smoliar et al., 1996), where λ is the decay constant of 187Re. Concordia diagrams and the weighted average were calculated by the ISOPLOT 3.0 (Ludwig, 2003).

microscope. Representative zircon grains were mounted on adhesive tape and then polished in order to expose the centers of individual crystals. Zircon U–Pb and trace element analyses were carried out at the State Key Laboratory of Continental Dynamics in the Northwest University (Xi’an, China). LA-ICP-MS zircon U–Pb dating and trace element analyses were conducted on an Agilent7500a ICP-MS coupled with Geolas 2005 laser ablation system with a 193 nm laser. During the analyses, a spot size of 32 μm was employed. Standard zircons 91500, GJ-1 and NIST 610 and were used as the reference for calibration and controlling the analytical instrument. The U, Th, and Pb concentrations were calibrated using 29Si as an internal standard and NIST 610 as the external standard. 207Pb/206Pb, 206Pb/238U, 207Pb/235U, and 208 Pb/232Th ratios were obtained by the GLITTER 4.4 (GEMOC, Macquarie University, Sydney, Australia) and corrected for both instrumental mass bias and depth-dependent element and isotope fractionation using zircon 91,500 as the external standard. No common Pb was corrected because of the high 206Pb/204Pb ratios (> 1000). Uncertainties on analytical results were reported at a 1σ level. The weighted average mean U–Pb ages (with 95% confidence) and concordia plots were performed using ISOPLOT 3.0 (Ludwig, 2003). 4.4. Re–Os analytical method Molybdenite separates were obtained after crushing the samples in a porcelain mill, gravity sorting, electromagnetic separation and finally handpicked under the binocular microscope (purity > 99%). Re–Os sample dissolution and preparation were performed at the National Research Center of Geoanalysis, Chinese Academy of Geological Sciences. The detailed chemical separation procedure is described by (Du et al., 1995; Qu, 2003; Qu et al., 2009; Li et al., 2009; Li et al., 2010; Zhou et al., 2012; Li et al., 2015a). The enriched 190Os and 185Re

4.5. Zircon Lu–Hf isotope analytical method Zircon Lu-Hf isotope analyses were carried out at the State Key 4

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166°

Laboratory of Continental Dynamics in the Northwest University (Xi’an, China). In-situ zircon Hf isotopic analysis was conducted using a Nu Plasma HR multi-collector MC-ICP-MS coupled with Geolas 2005 laser ablation system equipped with a 193 nm laser. In this study, a beam diameter 44 μm was selected during the ablation with a repetition rate of 10 Hz. Interference of 176Lu and 176Yb on 176Hf was corrected by the recommended 176Lu/175Lu (0.02669) (DeBievre and Taylor, 1993) and 176 Yb/172Yb (0.5886) (Chu et al., 2002), respectively. The detailed analytical procedure can be found in (Wu et al., 2006). The Hf isotope composition is processed using a Hf Calculate program-8.6 provided by the library. Standard zircons MON-1, 91,500 and GJ-1 were analyzed every ten zircons. During analyses, the acquired 176Hf/177Hf isotope ratios are 0.282318 ± 0.000012 (n = 5, 1σ) for 91,500, 0.282028 ± 0.000019 (n = 5, 1σ) for GJ-1, and 0.282732 ± 0.000026 (n = 10, 1σ) for MON-1, which is in good agreement with the recommended values of 0.282295 ± 0.000018 (1σ) for 91,500 (Griffin et al., 2006), 0.282013 ± 0.000019 (1σ) for GJ-1(Elhlou et al., 2006), and 0.282738 ± 0.000009 (1σ) for MON1(Woodhead and Hergt, 2005). Data processing using a decay constant for 176Lu of 1.867 × 10−11 y−1 (Söderlund et al., 2004) and the present-day chondritic values of 176Lu/177Hf (0.0332) and 176Hf/177Hf (0.282732) were adopted in calculating εHf(t) (Blichert-Toft et al., 1999). Single-stage Hf model ages (TDM1) are calculated relative to the depleted mantle with a present-day 176Hf/177Hf ratios of 0.28325 and 176 Lu/177Hf of 0.0384 (Griffin et al., 2000). Two-stage Hf model ages (TDM2) are calculated with references to a 176Lu/177Hf value of 0.015 for the average continental crust (Amelin et al., 1999; Griffin et al., 2000). The fLu/Hf value of average continental crust is − 0.55 (Griffin et al., 2002). The fLu/Hf ratio equals to (176Lu/177Hf)S/ (176Lu/177Hf)CHUR − 1, where the (176Lu/177Hf)CHUR = 0.0332, and two-stage model age (TDM2) for other young zircon grains was calculated by projecting the initial 176Hf/177Hf of zircon back to the depleted mantle growth curve with references to a 176Lu/177Hf value of 0.015 for the average continental crust (Amelin et al., 1999; Griffin et al., 2000).

400 340m 300

280m

400 200 340m 300

No.3

280m

Elevation (m)

200

300

280m

200

No.2

No.0

Prospecting line and No. Orebody

50 m

No.2

Fig. 3. Generalized geological cross-section of the Qi189 gold deposit (modified after Henan Jinyuan Gold Mining Co. LTD, unpublished confidential data).

a

b Ser Qz

Qz

Kfs

Pl Chl

300 m

c

d Hb

Kfs

Kfs

Pl

Pl Qz

Qz Hb

Spn

5

300 m

Fig. 4. Photographs showing petrography of the igneous rocks at the Qi189 gold deposit. (a) Porphyritic granite (hand specimen); (b) porphyritic granite, composed of K-feldspar, plagioclase and quartz (cross-polarized light); (c) quartz monzonite (hand specimen); (d) quartz monzonite, composed of K-feldspar, plagioclase, quartz, hornblende and sphene (cross-polarized light). Abbreviation: Qz, Quartz, Kfs, K, feldspar, Pl, Plagioclase, Hb, Hornblende, Ser, Sericite, Chl, Chlorite, Spn, Sphene.

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Fig. 5. Photographs showing ore petrography of the Qi189 gold deposit. (a) Quartz-molybdenite veinlet cut by auriferous quartz-pyrite vein in potassic-altered porphyritic granite; (b) quartz-molybdenite veinlet cut by quartz-pyrite veinlet in porphyritic granite; (c) potassic and propylitic alterations cut by quartz-pyrite veinlet; (d) potassic alteration, characterized by K-feldspar and biotite; (e) epidotization; (f) native gold occurring as inclusion in pyrite; (g) flaky molybdenite, coexisting with coarse-grained pyrite; (h) tetradymite, coexisting with quartz and pyrite; (i) electrum and hessite, occurring as fissure-fillings in pyrite. Abbreviation: Py, Pyrite, Gl, Gold, Qz, Quartz, Mo, Molybdenite, Kfs, K, feldspar, Ep, Epidote, Chl, Chlorite, Cal, Calcite, Bt, Biotite, Tet, Tetradymite, Elc, Electrum, Hes, Hessite.

5. Analytical results

The quartz monzonite samples are characterized by high contents of SiO2 (61.81–66.90 wt%, av. 65.16 wt%), alkalis (K2O + Na2O = 8.56–9.22 wt%, av. 8.94 wt%), and Al2O3 (15.61–17.12 wt%, av. 16.24 wt%), but low contents of TiO2 (0.36–0.59 wt%, av. 0.44 wt%) and MgO (0.58–1.16 wt%, av. 0.73 wt %). The values of K2O/Na2O and Mg# are 0.75–1.11 (av. 0.96) and 40.2–48.9 (av. 43.8), respectively. In the K2O–SiO2 plot (Fig. 6a), the samples cluster in the high-K calc-alkaline field. Their A/NK and A/CNK values range from 1.27 to 1.42 (av. 1.33) and 0.87 to 0.97 (av. 0.92), respectively (Fig. 6b), demonstrating metaluminous characteristics. The samples have higher contents of ∑REE + Y (219–335 ppm, av. 270 ppm), and are enriched in LREE and depleted in HREE, without obvious Eu anomalies (δEu = 0.82–1.00, av. 0.91) (Fig. 7a). They are enriched in large ion lithophile elements (LILE) such as Sr, Pb, and Ba, and depleted in high field strength elements (HFSE), as shown by Th, Nb, Ta, Ti and P (Fig. 7b).

5.1. Element geochemistry Analytical results of major and trace elements for the porphyritic granite and quartz monzonite of the Qi189 gold deposit are listed in Table 1. The porphyritic granite has high contents of SiO2 (68.29–73.65 wt %, av. 70.04 wt%), K2O (5.12–7.15 wt%, av. 6.13 wt%), and Al2O3 (11.28–15.33 wt%, av. 13.72 wt%), but low contents of TiO2 (0.19–0.27 wt%, av. 0.24 wt%), MgO (0.22–0.46 wt%, av. 0.32 wt%) and CaO (0.79–1.67 wt%, av. 1.18 wt%). The values of K2O/Na2O, A/ CNK, and Mg# are 1.41–2.58 (av. 2.11), 0.95–1.05 (av. 1.00), and 22.0–47.6 (av. 35.5), respectively. All porphyritic granite samples show high-K calc-alkaline (Fig. 6a) and metaluminous to peraluminous (Fig. 6b) characteristics, suggesting that the porphyritic granite belongs to the metaluminous to peraluminous high-K calc-alkaline series. The samples show steep LREE (light rare earth elements) and flat HREE (heavy rare earth elements) patterns with negligible Eu anomalies (Fig. 7a). They exhibit apparent peaks of K, Rb, Pb, and Ba, and depleted of Th, Nb, Ta, Ti, and P in a primitive mantle-normalized trace element diagram (Fig. 7b) The porphyritic granite has ∑REE + Y contents of 137–200 ppm (av. 164 ppm), δEu values of 0.69–0.92 (av. 0.85), and (La/Yb)N ratios of 15.6–25.9 (Table 1).

5.2. LA-ICP-MS zircon U–Pb age Zircon grains from sample ZR-3 (quartz monzonite) are colorless and euhedral elongated, prismatic in shape (Fig. 8). The crystals range from 50 to 150 μm in length, with length/width ratios from 2:1 to 3:1. Cathodoluminescent (CL) images show that most of the zircons have clear oscillating zonation structure (Fig. 8) and are magmatic in origin. 6

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Table 1 Chemical compositions of the porphyritic granite and quartz monzonite at Qi189 deposit (oxides in wt. %, elements in ppm). Sample no.

SiO2 TiO2 Al2O3 TFe2O3 MnO MgO CaO Na2O K2O P2O5 LOI Total K2O + Na2O K2O/Na2O A/CNK A/NK σ Mg# Au Li Be Sc V Cr Co Ni Cu Zn Ga Ge As Rb Sr Y Zr Nb Mo Ag Cd In Sn Sb Cs Ba La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Hf Ta W Tl Pb Bi Th U ∑REE ∑REE + Y LREE HREE LREE/HREE (La/Yb)N

porphyritic granite

quartz monzonite

280A-6

340B-9

280B-1

340A-14

280A-11

280A-13

ZR-1

400B-13

400B-15

580B-6

580B-8

ZR-2

ZR-3

580A-8

68.34 0.21 13.00 4.49 0.02 0.32 1.19 3.35 5.12 0.08 3.12 99.24 8.47 1.53 0.98 1.18 2.83 22.0 0.044 3.60 2.75 1.60 12.0 4.00 14.4 0.60 68.6 7.00 16.9 0.21 2.00 180 404 11.6 165 18.5 503 0.57 < 0.02 0.03 0.90 0.11 2.19 1695 35.0 63.8 7.00 24.1 3.51 0.85 2.54 0.36 1.89 0.40 1.11 0.19 1.34 0.23 4.50 1.40 8.00 1.19 54.6 2.00 13.8 6.99 142 154 134 8.10 16.66 18.74

68.61 0.27 15.28 2.01 0.03 0.46 1.67 3.87 5.44 0.11 2.07 99.82 9.31 1.41 1.00 1.25 3.38 47.6 < 0.001 4.80 3.32 2.40 27.0 2.00 1.30 0.60 3.20 10.0 20.4 0.45 0.80 177 567 15.1 206 19.7 0.34 0.02 < 0.02 0.01 1.20 < 0.05 1.64 1900 47.5 83.4 8.65 29.7 4.53 1.17 3.47 0.44 2.48 0.48 1.31 0.19 1.44 0.22 5.40 1.50 1.00 1.02 44.9 0.41 12.6 7.50 185 200 175 10.0 17.44 23.66

68.29 0.27 15.33 1.37 0.02 0.25 1.21 2.94 7.15 0.11 1.59 98.53 10.09 2.43 1.04 1.22 4.03 42.0 0.043 3.90 1.82 2.20 22.0 <1 7.40 0.40 66.1 12.0 21.3 0.20 1.70 252 421 14.6 207 23.6 3.82 0.44 0.03 0.07 1.60 0.14 4.21 2650 31.3 56.9 6.47 22.2 4.08 0.81 2.85 0.39 2.32 0.49 1.41 0.22 1.44 0.22 5.00 1.34 6.40 1.57 61.6 6.71 12.8 8.37 131 146 122 9.30 13.04 15.59

68.65 0.25 14.60 2.23 0.03 0.38 1.14 3.25 7.11 0.10 2.13 99.87 10.36 2.19 0.97 1.12 4.18 40.3 0.212 2.70 1.97 2.50 23.0 4.00 9.80 1.30 377 18.0 18.9 0.23 1.60 219 371 14.7 179 21.7 0.69 0.43 0.03 0.17 1.10 0.25 2.87 2270 43.1 79.1 8.75 29.9 4.22 1.12 3.18 0.45 2.23 0.47 1.32 0.20 1.33 0.22 4.60 1.40 10.0 1.45 44.1 2.66 13.1 7.67 176 190 166 9.40 17.68 23.24

72.72 0.19 11.28 3.21 0.03 0.31 1.09 2.25 5.68 0.08 2.04 98.88 7.93 2.52 0.95 1.15 2.12 27.7 0.541 5.40 1.91 1.60 8.00 1.00 12.7 1.90 789 12.0 15.6 0.43 1.40 189 289 12.4 142 16.3 7.11 1.65 0.09 0.18 1.00 0.13 2.12 1750 35.7 65.2 7.04 24.3 3.65 0.99 2.74 0.36 1.91 0.39 1.04 0.15 0.99 0.16 3.90 1.10 6.90 1.20 27.6 1.25 10.1 4.74 145 157 137 7.70 17.68 25.87

73.65 0.22 12.85 1.75 0.02 0.22 0.79 2.44 6.30 0.09 1.86 100.19 8.74 2.58 1.05 1.19 2.49 33.2 0.084 3.50 1.69 1.50 12.0 2.00 11.1 1.20 68.1 8.00 16.9 0.23 1.80 220 238 11.7 153 17.7 10.9 0.22 < 0.02 0.08 1.50 0.14 2.68 1940 30.8 55.7 6.13 21.0 3.22 0.87 2.52 0.33 1.83 0.38 1.04 0.15 1.14 0.18 4.20 1.20 8.00 1.46 34.0 1.78 11.9 7.17 125 137 118 7.60 15.55 19.38

62.81 0.53 17.12 4.46 0.08 0.91 3.79 4.65 4.05 0.34 0.61 99.35 8.70 0.87 0.90 1.42 3.82 44.7 0.002 5.30 2.78 4.10 55.0 <1 3.50 0.60 7.60 29.0 23.6 0.20 1.20 127 1695 26.0 240 22.7 0.46 0.01 < 0.02 0.02 1.50 0.11 2.47 2740 61.8 105 13.0 46.4 8.27 2.08 6.42 0.86 4.73 0.91 2.46 0.35 2.26 0.34 5.30 1.18 1.30 0.61 39.1 0.26 12.1 3.93 254 280 236 18.3 12.88 19.61

65.71 0.42 16.28 3.44 0.06 0.65 3.15 4.51 4.45 0.19 1.02 99.88 8.96 0.99 0.91 1.33 3.54 42.8 0.006 4.60 3.40 3.00 35.0 2.00 3.70 0.90 8.60 21.0 20.8 0.28 2.00 138 1085 23.2 213 24.1 0.72 0.07 0.03 0.03 1.70 0.08 1.45 2060 60.1 113 12.6 44.2 6.68 1.77 5.18 0.70 3.82 0.77 2.10 0.32 2.06 0.33 5.30 1.20 7.00 0.79 44.7 0.30 11.6 4.06 254 277 238 15.3 15.60 20.93

61.81 0.59 16.84 4.80 0.10 1.16 4.03 4.90 3.66 0.33 0.69 98.91 8.56 0.75 0.87 1.40 3.90 48.9 0.003 4.30 2.72 4.20 57.0 2.00 5.80 1.20 8.50 41.0 22.3 0.39 1.30 93.9 1395 27.2 248 32.3 1.10 0.01 0.03 0.03 2.00 0.05 0.69 2320 67.5 141 15.7 54.6 7.97 2.29 6.33 0.85 4.50 0.91 2.44 0.38 2.51 0.38 6.10 1.70 1.00 0.42 36.7 0.11 11.1 3.37 307 335 289 18.3 15.79 19.29

65.27 0.42 16.21 3.48 0.07 0.62 2.73 4.67 4.37 0.18 0.93 98.95 9.04 0.94 0.93 1.31 3.67 41.4 0.006 6.00 4.13 2.70 28.0 1.00 2.90 0.60 3.00 20.0 21.2 0.44 0.90 130 1145 21.7 252 26.8 1.39 0.06 0.02 0.03 1.70 0.08 1.77 2395 59.9 115 12.9 46.9 6.40 1.91 4.89 0.68 3.54 0.72 1.81 0.28 1.87 0.28 6.00 1.34 0.30 0.73 38.4 0.23 12.2 4.41 257 278 242 14.1 17.23 22.98

65.62 0.41 16.28 3.42 0.07 0.58 2.70 4.65 4.50 0.17 0.87 99.27 9.15 0.97 0.93 1.30 3.70 40.2 0.002 4.80 3.72 2.80 27.0 1.00 2.70 0.50 2.20 19.0 21.1 0.50 1.70 127 1175 21.4 249 26.4 0.66 0.04 < 0.02 0.03 1.60 0.23 1.71 2505 59.9 113 12.9 45.3 6.52 1.91 5.09 0.68 3.52 0.72 1.89 0.29 1.92 0.30 6.10 1.25 0.30 0.73 39.6 0.16 12.6 4.40 253 275 239 14.4 16.58 22.38

66.9 0.37 15.92 3.14 0.05 0.65 2.31 4.50 4.72 0.18 1.08 99.82 9.22 1.05 0.95 1.27 3.56 45.1 0.001 11.2 2.73 3.00 37.0 <1 2.50 0.70 3.50 22.0 22.5 0.20 1.20 134 1205 18.8 249 25.0 0.44 < 0.01 < 0.02 0.02 1.40 0.11 2.69 2200 54.2 91 10.5 34.9 5.86 1.44 4.26 0.59 3.36 0.65 1.80 0.27 1.79 0.28 6.00 1.27 0.30 0.6 38.3 0.16 16.5 4.97 211 230 198 13.0 15.22 21.72

66.51 0.36 15.69 3.17 0.04 0.63 2.13 4.31 4.78 0.18 1.18 98.98 9.09 1.11 0.97 1.28 3.51 44.1 0.015 11.7 2.57 3.00 50.0 1 2.70 0.70 12.3 24.0 21.9 0.19 1.80 142 1230 17.9 241 24.2 1.98 0.02 0.05 0.02 1.30 0.10 2.20 2120 51.1 86.6 10.1 33.8 5.72 1.38 4.19 0.57 3.20 0.64 1.70 0.27 1.78 0.28 6.10 1.30 1.80 0.65 40.0 0.93 17.7 5.51 201 219 189 12.6 14.94 20.59

66.68 0.38 15.61 3.26 0.07 0.62 2.59 4.43 4.35 0.17 0.81 98.97 8.78 0.98 0.93 1.30 3.26 43.0 < 0.001 4.80 3.11 3.10 27.0 2.00 3.20 0.60 1.10 35.0 21.0 0.25 0.90 144 1050 20.2 232 24.4 0.94 0.01 < 0.02 0.03 1.50 < 0.05 1.25 2240 59.7 110 12.4 42.6 6.16 1.71 4.76 0.62 3.32 0.68 1.80 0.28 1.83 0.28 5.60 1.20 1.00 0.64 45.6 0.67 14.7 3.20 246 266 232 13.6 17.10 23.40

(continued on next page) 7

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Table 1 (continued) Sample no.

δEu Tzr (°C)*

porphyritic granite

quartz monzonite

280A-6

340B-9

280B-1

340A-14

280A-11

280A-13

ZR-1

400B-13

400B-15

580B-6

580B-8

ZR-2

ZR-3

580A-8

0.83 780

0.87 772

0.69 804

0.90 795

0.92 791

0.90 779

0.84 786

0.89 782

0.95 782

1.00 801

0.98 794

0.84 805

0.82 805

0.93 803

*TZr was calculated using the calibration of Watson and Harrison (1983): ln DZr, [M = (Na + K + 2Ca)/(Al × Si)] and the temperature, T, is in kelvins.

zircon/melt

= {−3.8 − [0.85(M − 1)]} + 12,900/T, M is a compositional factor

129.6 ± 2.6 Ma (MSWD = 0.21, 2σ; Fig. 10a). The model ages are consistent with the isochron age, indicating that molybdenites were crystallized in the period from 127.9 ± 2.9 Ma to 130.1 ± 2.0 Ma, coinciding with the zircon U–Pb age of 128.6 ± 0.8 Ma obtained from the porphyritic granite (Zhang and Chen, 2018, unpublished confidential document). Pyrite separates from stage 3 auriferous quartz-pyrite or quartzpolymetallic sulfide veins have Re and 187Os contents of 1.143 to 3.312 ppb and 2.29 to 4.51 ppt, respectively. They contain common Os ranging from 0.719 to 4.09 ppt and have 187Re/188Os ratios between 1349 and 16309. Samples 280A-5b, 400A-7a and 400A-7b have high value of 187Re/188Os, and yield model ages of 135.4 ± 1.4 Ma, 138.1 ± 0.7 Ma, and 133.1 ± 1.4 Ma, respectively. These model ages indicate that the mineralization time is not earlier than 133 Ma due to the initial 187Os/188Os ratios are not as zero as supposed in calculation. All five analyses define a 187Re/188Os vs. 187Os/188Os isochron age of 127.5 ± 8.2 Ma (MSWD = 6.4) with an initial 187Os/188Os ratio of

Thirty-five zircon grains of quartz monzonite (ZR-3) were analyzed. They yield U, Th and common Pb concentrations of 204–1105 ppm, 155–1777 ppm, and 6.1–30.6 ppm, respectively, with Th/U ratios of 0.46–1.64 (Table 2). The 31 analyses yield a weighted average 206 Pb/238U age of 124.7 ± 0.6 Ma (MSWD = 0.23, 1σ) (Fig. 9; Table 2). The younger 206Pb/238U age defines the time for post-ore magmatic activity.

5.3. Molybdenite and pyrite Re–Os dating Three Re–Os analyses of three molybdenite and five Re–Os analyses of three pyrite samples are listed in Table 3 and Table 4, respectively. Total Re and 187Os concentrations of the molybdenite samples vary from 2.63 to 95.21 ppm and 3.55 to 127.6 ppb, respectively (Table 3). The molybdenite samples yield individual ages ranging from 127.9 ± 2.9 Ma to 130.1 ± 2.0 Ma, with an isochron age of 129.5 ± 2.8 Ma (MSWD = 0.51, 2σ) and a weighted average age of

Table 2 Results of LA-ICP-MS U–Pb dating for the single-grain zircon from quartz monzonite (ZR-3) at Qi189 deposit. Sample no.

ZR-3-1 ZR-3-2 ZR-3-3 ZR-3-4 ZR-3-5 ZR-3-6 ZR-3-7 ZR-3-8 ZR-3-9 ZR-3-10 ZR-3-11 ZR-3-12 ZR-3-13 ZR-3-14 ZR-3-15 ZR-3-16 ZR-3-17 ZR-3-18 ZR-3-19 ZR-3-20 ZR-3-21 ZR-3-22 ZR-3-23 ZR-3-24 ZR-3-25 ZR-3-26 ZR-3-27 ZR-3-28 ZR-3-29 ZR-3-30 ZR-3-31 ZR-3-32 ZR-3-33 ZR-3-34 ZR-3-35 ZR-3-36

Content (ppm)

Ratios

Age (Ma)

Pb*

Th

U

Th/U

207

Pb/235U

1σ

206

Pb/238U

1σ

207

Pb/206Pb

1σ

207

11.4 12.0 7.60 8.40 16.7 25.9 7.60 8.20 30.6 8.50 17.3 7.00 28.4 8.90 27.2 10.5 13.0 13.6 22.9 6.20 6.20 9.90 14.2 28.5 19.4 6.10 16.4 14.7 11.5 21.4 18.6 15.8 8.00 16.6 7.10 25.3

221 335 214 231 472 1089 252 184 1777 278 611 190 1012 188 673 179 258 248 582 202 155 483 464 1178 329 241 430 327 324 773 483 370 165 567 256 660

404 429 258 304 654 964 284 298 1085 313 643 253 970 322 988 364 497 521 852 226 204 382 577 1030 714 230 585 634 353 694 772 584 298 689 273 1105

0.55 0.78 0.83 0.76 0.72 1.13 0.89 0.62 1.64 0.89 0.95 0.75 1.04 0.58 0.68 0.49 0.52 0.48 0.68 0.90 0.76 1.26 0.80 1.14 0.46 1.05 0.74 0.52 0.92 1.11 0.63 0.63 0.55 0.82 0.94 0.60

0.1317 0.1338 0.1421 0.1312 0.1327 0.1361 0.1311 0.1319 0.1348 0.1385 0.1306 0.1349 0.1375 0.1341 0.1321 0.1327 0.1372 0.1311 0.1349 0.1475 0.1321 0.1308 0.1328 0.1302 0.4054 0.1275 0.1366 0.1325 0.1478 0.1977 0.1343 0.1321 0.1333 0.1314 0.1364 0.1304

0.0045 0.0052 0.0045 0.0059 0.0051 0.0036 0.0064 0.0056 0.0029 0.0071 0.0034 0.0072 0.0052 0.0043 0.0052 0.0044 0.0043 0.0036 0.0042 0.0084 0.0075 0.0049 0.0049 0.0028 0.0079 0.0061 0.0046 0.0044 0.0064 0.0040 0.0036 0.0042 0.0057 0.0040 0.0082 0.0029

0.0196 0.0198 0.0195 0.0194 0.0197 0.0195 0.0196 0.0197 0.0194 0.0198 0.0194 0.0198 0.0196 0.0195 0.0197 0.0194 0.0195 0.0197 0.0195 0.0196 0.0195 0.0194 0.0196 0.0194 0.0308 0.0189 0.0197 0.0195 0.0195 0.0206 0.0194 0.0195 0.0195 0.0196 0.0196 0.0194

0.0003 0.0003 0.0002 0.0003 0.0003 0.0002 0.0003 0.0003 0.0002 0.0003 0.0002 0.0003 0.0003 0.0002 0.0003 0.0003 0.0002 0.0002 0.0002 0.0003 0.0003 0.0003 0.0003 0.0002 0.0004 0.0003 0.0003 0.0003 0.0003 0.0002 0.0002 0.0002 0.0003 0.0002 0.0003 0.0002

0.0489 0.0490 0.0530 0.0490 0.0488 0.0506 0.0486 0.0486 0.0503 0.0507 0.0488 0.0493 0.0509 0.0499 0.0486 0.0495 0.0511 0.0482 0.0501 0.0545 0.0491 0.0488 0.0493 0.0486 0.0956 0.0489 0.0503 0.0494 0.0550 0.0696 0.0501 0.0491 0.0497 0.0486 0.0504 0.0486

0.0019 0.0021 0.0020 0.0024 0.0021 0.0016 0.0026 0.0023 0.0014 0.0028 0.0015 0.0028 0.0022 0.0018 0.0021 0.0019 0.0019 0.0016 0.0018 0.0033 0.0030 0.0020 0.0020 0.0013 0.0025 0.0025 0.0019 0.0019 0.0026 0.0019 0.0016 0.0018 0.0023 0.0017 0.0032 0.0014

125.7 127.5 134.9 125.2 126.5 129.6 125.1 125.8 128.4 131.7 124.6 128.5 130.8 127.8 126.0 126.5 130.5 125.1 128.5 139.7 126.0 124.8 126.6 124.3 345.6 121.9 130.0 126.3 140.0 183.2 128.0 126.0 127.0 125.3 129.8 124.4

Pb* indicates common Pb. 8

Pb/235U

1σ

206

Pb/238U

4.0 4.6 4.0 5.3 4.6 3.3 5.7 5.0 2.6 6.4 3.1 6.5 4.7 3.9 4.6 4.0 3.9 3.2 3.7 7.4 6.7 4.4 4.4 2.5 5.7 5.5 4.1 3.9 5.7 3.4 3.2 3.8 5.1 3.6 7.3 2.6

124.8 126.4 124.2 124.0 125.8 124.5 124.9 125.7 124.1 126.4 123.8 126.6 125.2 124.5 125.9 124.0 124.4 125.9 124.6 125.2 124.5 124.0 124.8 124.1 195.3 120.8 125.8 124.2 124.4 131.3 124.1 124.6 124.2 125.2 125.3 124.1

1σ

207

Pb/206Pb

1.6 1.7 1.5 1.7 1.7 1.5 1.8 1.7 1.4 1.9 1.4 2.0 1.7 1.5 1.7 1.6 1.5 1.5 1.5 2.1 2.0 1.6 1.6 1.4 2.3 1.7 1.6 1.6 1.8 1.5 1.5 1.5 1.7 1.5 2.1 1.4

141.1 147.5 326.5 146.9 139.9 222.6 128.2 127.9 207.8 227.4 139.6 163.3 234.3 189.2 126.9 173.4 242.9 108.8 200.7 392.9 153.3 139.3 159.6 128.7 1539 141.9 206.9 165.6 411.7 917.9 200.8 151.3 178.4 127.5 213.3 130.4

1σ 88.6 97.3 81.4 110.4 97.1 72.6 119.0 105.5 63.6 122.7 72.6 128.3 94.7 83.5 99.1 86.4 81.8 74.9 81.1 129.9 134.7 94.5 94.0 63.2 48.7 116.8 86.9 85.9 102.9 53.8 72.3 83.3 106.1 81.3 140.3 65.2

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8

a

3.0 Porphyritic granite Quartz monzonite

b

2.6

6 2.2

Hig

h-

alc K (c

2

55

Low-K (tholeiite) series

0.6

75

65 SiO 2 (wt.%)

Peralkaline

1.0

0.5

85

1.5

Syenite

10 Monzonite

8

Monzodiorite

6 4

tz Quar onite n o m z

Al

k

g ali

ran

45

55 SiO 2 (wt.%)

Granite

65

1 syenogranite 2 monzogranite 3 quartz syenite 4 quartz monzonite

ite

1

Gabbro- Diorite Granodiorite Gabbro diorite

2

2.0

A/CNK Q

d

12

0 35

Peraluminous

1.4 1.0

lk a li n e

Metaluminous

1.8

c

14

Na 2 O+K 2 O(wt.%)

alin

es

s e r ie s

C a lc - a

0 45

-alk

eri e) s

A/NK

K 2 O(wt.%)

Shoshonite series 4

2

3 75

A

4

P

Fig. 6. (a) SiO2-K2O diagram; (b) A/NK [molar Al2O3/(Na2O + K2O)] vs. A/CNK [molar Al2O3/(CaO + Na2O + K2O)] diagram (Maniar and Piccoli, 1989); (c) total alkalis vs. silica diagrams (Middlemost, 1994); (d) Q-A-P diagram (Streckeisen, 1976).

a

1000 Porphyritic granite Quartz monzonite

Rock/Primitive Mantle

1000

Rock/Chondrite

100

10

100

10

1

1

0.1

b

0.1 Rb Th Nb K Ce Pr P Zr Sm Ti Tb Y Er Yb Ba U Ta La Pb Sr Nd Hf Eu Gd Dy Ho Tm Lu

La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu

Fig. 7. (a) Chondrite-normalized REE diagram and (b) primitive mantle-normalized trace element spider diagrams of the intrusions at Qi189 gold deposit in Qiyugou Orefield. Chondrite and primitive mantle compositions are from Sun and McDonough (1989). 9

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Quartz monzonite

ZR-3 -20.2 126.4±1.7 Ma

-16.0 124.8±1.6 Ma

124.0±1.7 Ma

125.8±1.7 Ma

124.2±1.5 Ma

-14.9

-20.7

124.5±1.5 Ma

-19.6

124.9±1.8 Ma

125.7±1.7 Ma

124.1±1.4 Ma

126.4±1.9 Ma

123.8±1.4 Ma

126.6±2.0 Ma

125.2±1.7 Ma

124.5±1.5 Ma

125.9±1.7 Ma

124.0±1.6 Ma

124.4±1.5 Ma

125.9±1.5 Ma

124.6±1.5 Ma

125.2±2.1 Ma

124.5±2.0 Ma

-15.1 -18.1 124.0±1.6 Ma

124.8±1.6 Ma

124.1±1.4 Ma

195.3±2.3 Ma?

120.8±1.7 Ma

125.8±1.6 Ma

124.2±1.6 Ma

124.4±1.8 Ma

131.3±1.5 Ma

124.1±1.5 Ma

125.3±2.1 Ma

124.1±1.4 Ma

-16.3

124.6±1.5 Ma

124.2±1.7 Ma

-20.6

125.2±1.5 Ma

100μm Fig. 8. Cathodoluminescent images of zircon grains from quartz monzonite (ZR-3) at Qi189 gold deposit.

132 Intercepts at124.9±0.8 Ma (n=31) MSWD=0.23

a

0.0204

128

0.0200 0.0196

124

206

Pb/ 2 3 8 U

129

Pb/ 2 3 8 U age (Ma)

0.0208

206

0.0192 120

0.0188 0.0184 0.10

0.12 207

0.14 Pb/ 2 3 5 U

0.16

0.18

b

Quartz monzonite Mean=124.7±0.6Ma (n=31) MSWD=0.23

127

125

123

121

Fig. 9. LA-ICP-MS zircon U–Pb concordia diagram for the quartz monzonite (ZR-3) at Qi189 gold deposit. 10

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Table 3 Results of the Re–Os dating of molybdenite from the Qi189 deposit. Sample no.

Weight (g)

Re (ppm)

2σ

187

280C-1 400A-4 280B-1

0.00926 0.01134 0.01054

2.63 95.21 23.83

0.02 1.82 0.22

1.64 59.84 14.98

Re(ppm)

2σ

187

2σ

Age (Ma)

2σ

0.01 1.14 0.14

3.55 127.60 32.49

0.04 0.80 0.21

129.9 127.9 130.1

2.3 2.9 2.0

Os (ppt)

Table 4 Results of the Re–Os dating of pyrite from the Qi189 deposit. Sample no.

Weight (g)

Re (ppb)

580B-1 280A-5a 280A-5b 400A-7a 400A-7b

0.7009 0.7001 0.3009 0.7002 0.3077

1.143 1.550 1.638 3.115 3.312

*n.a. no model age was calculated as the

± ± ± ± ±

187

0.008 0.011 0.012 0.009 0.023

Common Os (ppt)

187

4.09 ± 0.04 1.79 ± 0.01 0.719 ± 0.009 2.14 ± 0.03 0.928 ± 0.015

2.34 2.29 2.33 4.51 4.37

Zircon Hf isotopic compositions of the quartz monzonite (ZR-3) at the Qi189 gold deposit are presented in Table 5 and Fig. 11. The 176 Hf/177Hf values for the Cretaceous zircons from sample ZR-3 range from 0.282112 to 0.282275. The calculated εHf(t) values range from −20.7 to −14.9, corresponding to TDM2 ages of 2.49–2.13 Ga. 6. Discussion 6.1. Geochronology of the Qi189 gold deposit The Re–Os isotopic data of three molybdenite samples from Stage 2 define a weighted average age of 129.6 ± 2.6 Ma and an isochron age of 129.5 ± 2.8 Ma, which unambiguously shows that molybdenite precipitated at ca. 129.5 Ma. The Re–Os age coincides with the crystallization age of the ore-hosting porphyritic granite (128.6 ± 0.8 Ma), powerfully suggesting a causative relationship between the ores and the spatially associated porphyritic granite. Five pyrite samples from the stage 3 auriferous quartz-pyrite veins and quartz-polymetallic sulfide veins yield model ages of 135–131 Ma and an isochron age of 127.5 ± 8.2 Ma, which more directly suggesting that the gold mineralization occurred at ca. 127.5 Ma. It is in good agreement with the porphyritic granite crystallization age and molybdenite Re–Os isochron

a

40

Age= 129.5±2.8 Ma Initial 1 8 7 Os/ 1 8 8 Os=0.01±0.14 MSWD= 0.51

1349 ± 15 4195 ± 44 11004 ± 161 7049 ± 130 16309 ± 289

Os/188Os

Model age (Ma)

4.42 ± 0.04 9.85 ± 0.04 24.84 ± 0.27 16.25 ± 0.26 36.37 ± 0.53

n.a. n.a. 135.4 ± 1.4 138.1 ± 0.7 133.1 ± 1.4

b Initial

Age= 127.5±8.2 Ma 187 188 Os/ Os=1.29±0.81 MSWD= 6.4

188

Os/ Os

30

187

80

187

Os (ppb)

0.02 0.02 0.02 0.02 0.04

187

age within error. Therefore, it is concluded that the mineralization occurred during 130–127 Ma. The CL images and Th/U ratios of zircon from barren quartz monzonite sample ZR-3 indicate that zircons were crystallized from magma, and the zircon U–Pb ages can represent the emplacement time of the granitoids. The ore-barren quartz monzonite dike cuts the porphyritic granite stock (Fig. 2), and Sample ZR-3 yields a weighted average 206 Pb/238U age of 124.7 ± 0.6 Ma (MSWD = 0.23, 1σ), which shows that the quartz monzonite crystallized at ~125 Ma, and that gold mineralization occurred before 125 Ma. Available data show that three episodes of Yanshanian mineralization and granitic magmatism aged 160–150 Ma, 145–130 Ma and 130–110 Ma in the Qiyugou breccia pipe-porphyry orefield (Li et al., 2006; Mao et al., 2008; Yao et al., 2009; Deng et al., 2014) and the Qinling Orogen (Li et al., 2018). The first episode might be around 160–150 Ma from the quartz porphyry near J3 pipe in the southern part of the Qiyugou Orefield (Deng et al., 2014), which is coincident with SHRIMP zircon U–Pb age of 157 ± 1 Ma from Wuzhangshan granite batholith (Mao et al., 2010). Recent study obtained an age of 153 Ma for zircons from the matrix of J5 porphyry-breccia pipe system by insitu LA-ICP-MS U–Pb dating method (Deng Ke, personal communication). These geochronological data indicate the 160–150 Ma mineralization event in the Qiyugou Orefield. The second episode occurred during 145–130 Ma, exemplified by the molybdenite Re–Os isochron age of 135.6 ± 5.6 Ma (n = 5) in the J7 pipe, granite porphyry beneath the J16 pipe with a U–Pb age of 134.1 ± 2.3 Ma (Yao et al.,

5.4. Zircon Hf isotope

120

± ± ± ± ±

Re/188Os

Re/188Os < 5000.

1.29 ± 0.81 (Fig. 10b).

160

187

Os (ppt)

132

20

130 40

128

10

126 0

Mean= 129.6±2.6Ma 124 MSWD=0.21

0

20

187

40 Re (ppm)

60

80

0 0

4000

8000 12000 16000 20000 187 188 Re/ Os

Fig. 10. Molybdenite (a) and pyrite (b) Re–Os isochron age and weighted average age for the Qi189 gold deposit. 11

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Table 5 Lu–Hf isotopic data for quartz monzonite (ZR-3) at Qi189 deposit. Spot no.

Age (Ma)

176

Yb/177Hf

ZR-3-24 ZR-3-1 ZR-3-8 ZR-3-4 ZR-3-33 ZR-3-11 ZR-3-34 ZR-3-22 ZR-3-10

124.1 124.8 125.7 124.0 124.2 123.8 125.2 124.0 126.4

0.061777 0.034969 0.034726 0.041452 0.058975 0.049955 0.023912 0.034107 0.030516

176

176

± 1σ

εHf(0)

εHf(t)

(176Hf/177Hf)i

TDM1/Ma

TDM2/Ma

fLu/Hf

0.002582 0.001719 0.001524 0.001869 0.002528 0.002357 0.001134 0.001471 0.001495

0.282274 0.282247 0.282112 0.282128 0.282239 0.282146 0.282114 0.282187 0.282275

0.000009 0.000009 0.000005 0.000009 0.000007 0.000008 0.000006 0.000008 0.000006

−17.6 −18.6 −23.3 −22.8 −18.9 −22.1 −23.3 −20.7 −17.6

−15.1 −16.0 −20.7 −20.2 −16.3 −19.6 −20.6 −18.1 −14.9

0.282268 0.282243 0.282109 0.282123 0.282233 0.282140 0.282112 0.282184 0.282271

1441 1445 1628 1621 1489 1616 1608 1520 1397

2134 2189 2486 2454 2211 2417 2481 2321 2126

−0.92 −0.95 −0.95 −0.94 −0.92 −0.93 −0.97 −0.96 −0.95

Lu/177Hf

Hf/177Hf

rocks (Huang et al., 2017). The contents of Rb and Sr in quartz monzonite are not positively related with LOI, suggesting that little hydrothermal alteration happened with the post-ore quartz monzonite. As shown in the Th/Sm vs. Th diagram (Fig. 12c), the porphyritic granite and quartz monzonite samples at the Qi189 deposit display a distinct partial melting trend, suggesting that they might be derived from different batches of partial melting of continental crust. The ore-hosting porphyritic granite contains a lot of inherited zircons with ages being up to > 3.5 Ga (Zhang and Chen, 2018), but the post-ore quartz monzonite has no inherited zircon, suggesting that that they were likely generated from Zr-saturated and Zr-undersaturation sources, respectively. However, the inheritance-rich porphyritic granite has lower Zr concentrations (142–207 ppm, av. 175 ppm) than the inheritance-free quartz monzonite (213–252 ppm, av. 241 ppm) (Table 1), which is worthy of further discussion. As addressed by Miller et al. (2003) and Mao et al. (2014), hot felsic magmas generated from high-temperature partial melting of the crust with additional heat input usually contain no or minimal inherited zircon crystals, because inherited zircon crystals can be completely dissolved due to high-temperature conditions and the Zr-undersaturation in melts; whereas cold felsic magmas generated from low-temperature partial melting of the crust with additional fluid influx are commonly inheritance-rich, because some inherited crystals can keep stable in the cold magmas. Coincidently, using the model proposed by Waston and Harrison (1983), the estimated Zr-saturation temperatures (TZr) of the inheritance-rich syn-ore porphyritic granite is ~787 °C, clearly lower than ~795 °C

2009), and SHRIMP zircon U–Pb ages of 131 ± 1 Ma and 132 ± 2 Ma from Huashan granite batholith (Mao et al., 2010). The third episode event occurred in the span of 130–110 Ma, respectively, exemplified by K-feldspar Ar–Ar plateau ages of 125–115 Ma in the K-feldspar-quartz veins of J2 pipe (Wang et al., 2001) and pyrite Rb–Sr isochron age of 126 ± 11 Ma from pyrite in J4 pipe (Han et al., 2007). The ages of 130–127 Ma reported herewith support the third episode of mineralization associated with magmatism in the Qiyugou Orefield. 6.2. Petrogenesis of the igneous rocks The syn-ore porphyritic granite and post-ore quartz monzonite belong to metaluminous to peraluminous high-K calc-alkaline series, which are characterized by high contents of SiO2 and K2O, and low CaO (Table 1; Fig. 6). Samples of the ore-hosting porphyritic granite plot in the granite domain, more exactly, in the porphyritic syenogranite domain; the samples from the post-ore quartz monzonite dike plot in the domain of quartz monzonite in TAS diagram and quartz syenite or quartz monzonite in QAP diagram (Fig. 6c, d). Some samples with clear hydrothermal alteration show relatively high LOI (loss on ignition) values of 1.59–3.12, implying for an addition of H2O and CO2 into the rocks during wall-rock alteration. Such processes could change the contents of mobile elements (e.g., Rb, Ba; Fig. 12a, b). For example, the Rb contents in porphyritic granite decrease along with increasing LOI. This implies that the immobile elements such as HFSE and REE are more reliable than LILE to trace petrogenesis and source of the altered

Fig. 11. Plot of zircon εHf(t) values vs. U–Pb ages for zircons from quartz monzonite (ZR-3) at Qi189 deposit. Also shown are data for the Taihua Supergroup (Diwu et al., 2010; Diwu et al., 2007; Xu et al., 2009; Yu et al., 2013); Xiong’er Group (Liu et al., 2011; Wang, 2010); Qinling Group (Shi et al., 2013); Kuanping Group (Shi et al., 2013; Zhu et al., 2011); Guandaokou Group (Zhu et al., 2011).

12

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1600

a

Supergroup. The Paleoproterozoic TDM2(Hf) (2.49–2.13 Ga) of the quartz monzonite suggests that the rocks were unlikely to be derived from the partial melting of the Kuanping Group (Mesoproterozoic) or Qinling Group (Mesoproterozoic to early Neoproterozoic) alone (Shi et al., 2009, 2013; Yang et al., 2010; Wan et al., 2011; Liu et al., 2013), but may require the involvement of a more ancient crust. Available geochronological data shows that the Taihua Supergroup was mainly formed during the Neoarchean to the Paleoproterozoic (3.0–2.1 Ga; Li et al., 2015b and references therein), which agrees with the zircon TDM2(Hf) ages of the quartz monzonite. Therefore, the quartz monzonite may have sourced from the Kuanping and Qinling groups that mixed with a more ancient crust (e.g., the Taihua Supergroup).

Porphyritic granite Quartz monzonite

Sr(ppm)

1200 800 400 0

0

1

2 LOI

3

4

Rb(ppm)

b 250

6.3. Ore genesis and tectonic setting

200

Re content in molybdenite can provide clues for the original source of a deposit. The atomic Re/Mo ratios of molybdenite are negatively correlated with the fractionation degree of the related granites. Molybdenite with low Re/Mo ratios or Re contents is associated with Mo-dominant porphyry systems, which are genetically related to more evolved granites, and represented by the Mactung (Canada) and Pogo (Alaska) deposits (Selby et al., 2002, 2003). Re contents in molybdenite from mantle-sourced rocks or deposits are significantly higher than those from crust-sourced ones (Stein et al., 2001). Mao et al. (1999) suggested that the Re contents in molybdenite from mantle- and crustsourced mineral systems are commonly > 100 ppm and < 10 ppm, respectively. Recent summaries of Mo deposits in Dabie Shan (Chen et al., 2017a), Northeast China (Chen et al., 2017b), Northwest China (Wu et al., 2017a,b), South China (Zhong et al., 2017) and Southwest China including Tibet (Yang and Wang, 2017) reached a consensus that the Re contents in molybdenites from porphyry or porphyry-skarn Cu-Mo systems are higher than 50 ppm, mainly > 100 ppm, indicating a significant mantle contribution; whereas the Re contents in molybdenites from Mo-only or W-Mo deposits are lower than 100 ppm, mainly < 50 ppm. Therefore, the Re content of molybdenite can be used to trace the metal sources, ore-associated intrusion, the degree of magma fractionation, and the redox property of the magma-fluid system (Chen et al., 2017a). Re contents of three molybdenite samples from the Qi189 gold deposit vary from 2.63 ppm to 95.63 ppm (Table 3), indicating that the ores might originate from a crust-dominated source with a minor contribution from the mantle. As known, Au and Os are noble metals and share some geochemical similarities, which make Os an isotopic tracer to Au mineralization. Furthermore, the obvious differences between Os isotopic compositions of the crust and the mantle make the system particularly desirable for discerning the ultimate source of Os contained in ore deposits (Shirey and Walker, 1998). The initial 187Os/188Os (1.29 ± 0.81) ratio of pyrite at 127 Ma from the Qi189 gold deposit is higher than the mantle 187 Os/188Os ratios (0.12–0.13) (Shirey and Walker, 1998). The contained Os with high radioactivity might demonstrate two end-member (crust and mantle) mixing isotopic composition. Combined with zircon Hf isotopic compositions, it is suggested that the Qi189 deposit may have sourced from the basement of North China Craton (Taihua Supergroup) and crustal material of the North Qinling Accretion Belt (Kuanping and Qinling groups), with minor contribution of mantle material. To interpret the origin of the Qi189 porphyry system, we present a tectonic model showing that an A-type subduction of the North Qinling Accretion Belt beneath the Huaxiong Block along the Machaoying Fault may have been a critical factor for the metallogenesis of porphyry deposits in the Qiyugou Orefield (Fig. 13). This underthrusting of the southern margin of North China Craton and the North Qinling Accretion Belt (A-type subduction) was accompanied by imbricate stacking of crustal slices, and then the detachment and sinking of the lithospheric mantle, which induced upwelling of the asthenospheric mantle and the emplacement of granitic magma. Partial melting of the crustal stacking materials of the North Qinling Accretion

150 100 50 0 0

1

2 LOI

3

4

c

4

Th/Sm

3 2 1 0

0

10 Th(ppm)

20

Fig. 12. (a) LOI against the Sr diagram (Huang et al., 2017); (b) LOI against the Rb diagram (Huang et al., 2017); (c) Th/Sm vs. Th diagram (Schiano et al., 2010) at the Qi189 gold deposit.

estimated for the inheritance-free post-ore quartz monzonite (Table 1). Moreover, the inheritance-free rocks represent Zr-undersaturation magmas whose temperatures are no lower than the estimated Zr-saturation temperature, whereas the temperature of magmas forming the inheritance-rich rocks must be lower than the estimated Zr-saturation temperature because a part of Zr concentration of the rocks is contributed from inherited zircon crystals rather than melt (Miller et al., 2003). It is suggested that the zircon inheritance can elevate TZr by a maximum of 70 °C at a constant parameter of M ((Na + K + 2Ca)/ (Al·Si)) (Siégel et al., 2018). Therefore, the syn-ore porphyritic granite was crystallized from magmas with temperature lower than 787 °C; whereas the post-ore quartz monzonite was originated from magmas with temperature higher than ~795 °C. Zircons can effectively preserve the initial Lu–Hf isotopic characteristics because they have extremely low contents of Lu, which resulted in negligible radiogenic Hf (Wu et al., 2006). Zircons from the quartz monzonite show negative εHf(t) values of −20.7 to −14.9 and ancient TDM2 ages of 2.49 to 2.13 Ga. In Fig. 11, all the zircon εHf(t) data of the quartz monzonite are entirely bracketed by the Lu–Hf evolution lines (176Lu/176Hf = 0.015) developed from the Kuanping Group, and also from the lower limit of Qinling Group and the upper limit of Taihua Supergroup, indicating that the magma may have been sourced from the Kuanping or Qinling groups or the Taihua 13

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Fig. 13. Conceptual model showing the tectonic setting of the Qi189 gold deposit.

tectonic setting, and thus is proposed to be a collisional-type porphyry ore system.

Belt and North China Craton triggered the development of the Qi189 porphyry system. The Qinling-Dabie Orogen formed during Late Triassic–Early Cretaceous caused by the collision of the Yangtze and North China cratons, following the Triassic closure of the northernmost PaleoTethyan Ocean (Chen et al., 2017b). The subsequent Early Cretaceous geodynamic setting in the Qinling-Dabie belt was one of post-collisional extension (Jahn et al., 1999; Chen et al., 2007, 2009b). Both the Cretaceous intrusions and hydrothermal metallogenic systems are specifically related to the post-collisional regime (Chen and Fu, 1992; Chen et al., 2000; Mao et al., 2011; Mi et al., 2015). Our new zircon U–Pb data and molybdenite and pyrite Re–Os dates confirm that the mineralization at the Qi189 deposit occurred in a post-collision tectonic setting, which is supported by the nature and genesis of the ore-hosting granitic rocks originated mainly from partial melting of the continental crust in a post-collisional setting. Therefore, the tectonic setting in the Qiyugou Orefield at 130 Ma was considered to represent a post-collisional tectonic setting (Li et al., 2007; Chen et al., 2009b). As such, the Qi189 gold deposit emplaced at 130–127 Ma may be considered as a collisional-type porphyry gold system.

Acknowledgment This is a contribution to celebrate the 90th birthday of Yusheng Zhai, a professor with CUGB and academician of CAS. Professor Zhai is an excellent teacher, researcher and leader in the field of earth sciences. The authors have the pleasure to be supervised in the scientific studies including those presented in this paper. This work was jointly granted by the National Natural Science Foundation of China (Nos. 41630313) and China National Gold Group. The field work was supported by Henan Jinyuan Co. Ltd., and Drs. Qiangwei Xu, Jing Fang, Ke Deng and Jianming Yan. We are grateful for Drs. Huadong Gong, Hong Zhang, Sun-Ping Shu and Chao Li for assistance with analytical work. References Amelin, Y., Lee, D.C., Halliday, A.N., Pidgeon, R.T., 1999. Nature of the Earth’s earliest crust from hafnium isotopes in single detrital zircons. Nature 399, 1497–1503. Bao, Z.W., Zeng, Q.S., Zhao, T.P., Yuan, Z.L., 2009. Geochemistry and petrogenesis of the ore-related Nannihu and Shangfanggou granite PorPhyries from east Qinling belt and their constraints on the molybdenum mineralization. Acta Petrol. Sin. 25, 2523–2536 (in Chinese with English abstract). Blichert-Toft, J., Gleason, J.D., Télouk, P., Albarède, F., 1999. The Lu–Hf isotope geochemistry of shergottites and the evolution of the Martian mantle-crust system. Earth Planet. Sci. Lett. 173, 243–258. Chen, Y.J., Fu, S.G., 1992. Gold Mineralization in West Henan, China. China Seismological Press, Beijing pp. 1–234 (in Chinese with English abstract). Chen, Y.J., Zhao, Y.C., 1997. Geochemical characteristics and evolution of REE in the Early Precambrian sediments: evidences from the southern margin of the North China craton. Episodes 20, 109–116. Chen, Y.J., Li, C., Zhang, J., Li, Z., Wang, H., 2000. Sr and O isotopic characteristics of porphyries in the Qinling molybdenum deposit belt and their implication to genetic mechanism and type. Sci. China Ser. D Earth Sci. 43, 82–94 (in Chinese with English abstract). Chen, Y.J., Zhang, J., Zhang, F., Pirajno, F., Li, C., 2004b. Carlin and Carlin-like gold deposits in Western Qinling Mountains and their metallogenic time, tectonic setting and model. Geol. Rev. 50, 134–152. Chen, Y.J., Pirajno, F., Sui, Y.H., 2004a. Isotope geochemistry of the Tieluping silver-lead deposit, Henan, China: a case study of orogenic silver-dominated deposits and related tectonic setting. Mineral. Deposita 39, 560–575. Chen, Y.J., Chen, H.Y., Zaw, K., Pirajno, F., Zhang, Z.J., 2007. Geodynamic settings and tectonic model of skarn gold deposits in China: an overview. Ore Geol. Rev. 31, 139–169. Chen, Y.J., Li, N., 2009. Diagnostic fluid inclusion and wallrock alteration of intrusion-

7. Conclusion (1) Re–Os isochron ages of 129.5 ± 2.8 Ma and 127.5 ± 8.2 Ma for molybdenite and auriferous pyrite define the timing of metallogenesis. The post-ore quartz monzonite at the Qi189 gold deposit was emplaced at 124.7 ± 0.6 Ma. The Qi189 gold system was formed during a magmatic-hydrothermal event around 130–127 Ma. (2) The ore-associated porphyritic granite and post-ore quartz monzonite are derived from distinct batches of partial melting of the same magma source and show enrichment in LREE and LILE (e.g., K, Rb, Pb, Ba) and depletion in HREE and HFSE (e.g., Th, Nb, Ta, Ti, P), belonging to high-K calc-alkaline series. (3) The Re concent, the initial Os isotope, and zircon Hf isotope indicate a crust-dominated source both from the North Qinling Accretion Belt and basement rocks of North China Craton, with minor mantle component. (4) The Qi189 porphyry gold system was formed in a post-collisional 14

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