Economic Geology Volume 115, Number 2 › uploadCms › file › 20600 › ... · 2020-05-18 ·...

IntroductionThe Jiaodong gold province in eastern China (Fig. 1) contains an estimated pre-mining resource of at least 4,000-t Au (Guo et al., 2013). The Jiaodong deposits have many features that are typical of orogenic gold deposits but differ in that they represent very young gold deposits in very old rocks (Gold-farb et al., 2001; Chen, 2006; Fan et al., 2007). Ages for the gold mineralization are broadly bracketed between ca. 125 and 110 Ma (Chen et al., 2005; Li et al., 2006, 2008; Yang et al., 2013; Goldfarb and Santosh, 2014; Deng and Wang, 2016). However, as noted below, many published dates are questionable, and some dates are even slightly younger or older than the majority that define this 15-m.y.-wide range. Most genetic models consider ore formation to be related to fluid release below the Precambrian crust during widespread Yanshanian orogenesis that included decratonization, exten-sion, core complex exhumation, and Izanagi plate subduction (Chen et al., 2005; Goldfarb et al., 2007; Faure et al., 2012; Zhai and Santosh, 2013). The specific fluid source reservoir(s) remains debated, partly reflecting controversies on abso-lute timing of the numerous complex events during the late Mesozoic orogeny.

The ages of the gold deposits have been determined by many workers during the past 35 years in an attempt to relate the ore-forming episode to the evolution of the Yanshanian orogen. More than 10 different dating methods have been ap-plied to the Jiaodong deposits (Appendix Table A1). The most robust methods include 40Ar/39Ar dating of hydrothermal ser-icite/muscovite and U-Pb ages measured on suspected hydro-thermal zircon in the ore zones (e.g., Li et al., 2003, 2006; Zhang et al., 2003; Hu et al., 2006; Yang et al., 2014). Ad-ditional age constraints come from 40Ar/39Ar measurements of fluids extracted from inclusions in ore-related quartz, and from application of the Rb-Sr method to sericite-pyrite–al-tered rock, muscovite, sericite, and fluid inclusions in quartz. Together all these data yield a wide range for hypothesized hydrothermal activity from 130~80 Ma (e.g., Li, 1993; Zhao et al., 1996; Zhang et al., 2002; Li et al., 2003). The range, however, partly reflects the fact that many of the applied chro-nometers are susceptible to isotopic resetting during thermal events and deformation (e.g., Kerrich and Cassidy, 1994; Chesley et al., 1999). The 40Ar/39Ar geochronology of sericite from the gold ores provides by itself a somewhat narrower but, nevertheless, still wide range of ages for the gold episode from 133.4 ± 0.6 to 115.2 ± 0.2 Ma, and 109.3 ± 0.3 to 107.7 ± 0.5 Ma (e.g., Li, J.W., et al., 2003, 2006; Li, Q.L., 2008; Zhang et

©2020 Society of Economic Geologists, Inc.Economic Geology, v. 115, no. 3, pp. 671–685

ISSN 0361-0128; doi:10.5382/econgeo.4711; 15 p.Digital appendices are available in the online Supplements section. 671

†Corresponding author: e-mail, [email protected]

Submitted: January 9, 2019 / Accepted: October 31, 2019

SCIENTIFIC COMMUNICATIONS

IN SITU DATING OF HYDROTHERMAL MONAZITE AND IMPLICATIONS FOR THE GEODYNAMIC CONTROLS ON ORE FORMATION IN THE JIAODONG GOLD PROVINCE, EASTERN CHINA

Jun Deng,1,† Kun-Feng Qiu,1,2 Qing-Fei Wang,1 Richard Goldfarb,1,2 Li-Qiang Yang,1 Jian-Wei Zi,3,4 Jian-Zhen Geng,1,5 and Yao Ma1

1 State Key Laboratory of Geological Processes and Mineral Resources, School of Earth Sciences and Resources, China University of Geosciences, Beijing 100083, China

2 Department of Geology and Geological Engineering, Colorado School of Mines, Golden, Colorado 80401, USA3 State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Wuhan 430074, China

4 John de Laeter Centre, Curtin University, Kent Street, Bentley, Perth, Western Australia 6102, Australia5 Tianjin Center, China Geological Survey, Tianjin 300170, China

AbstractThe Jiaodong gold province, the largest gold producer in China, formed in a setting dominated by a 30-m.y. episode of Izanagi plate rollback and widespread extension, concomitant with late Mesozoic craton destruction. This study presents new high precision in situ sensitive high-resolution ion microprobe (SHRIMP) U-Th-Pb and laser ablation-inductively coupled plasma-mass spectrometry (LA-ICP-MS) U-Pb ages for hydrothermal monazite from the largest of the Jiaodong gold deposits, which were previously dated as indicating ore forma-tion over a few tens of millions of years when applying sericite Ar-Ar, zircon U-Pb, and less robust analytical techniques. Our U-Pb dating on monazite from the Jiaojia and Linglong deposits in western Jiaodong yielded consistent ages at ca. 120 Ma. The new geochronologic results, coupled with recently reported in situ monazite dates from smaller deposits in western Jiaodong, reveal that the deposits that host most of the ≥4,000-t Au resource formed during a relatively brief period at ca. 120 Ma. In eastern Jiaodong, the much smaller resource may have formed about 5 m.y. later, recorded by 114.2 ± 1.5 Ma gold mineralization at the Rushan deposit. The postsubduction opening of a slab gap at ca. 120 Ma is the most likely cause of the extensive gold mineralization in Jiaodong. The gap induced a local and rapid devolatilization of the hydrated mantle wedge at submelt tem-peratures. The transient event included release of a major volume of gold-transporting aqueous-carbonic fluid that was stored in the wedge into major NNE-trending structures in the overlying lithosphere.

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672 SCIENTIFIC COMMUNICATIONS.

al., 2003; Hu et al., 2006; Yang et al., 2014). This is, at least in part, because issues of whether some sericite may be pre-gold in origin or the sericite may have suffered later modification are commonly not well addressed or difficult to determine. It is clear that the gold formation accompanied rapid crustal exhumation and thus cooling through mica-blocking tempera-tures would be a critical issue. Zircons from a few ores ana-lyzed using laser ablation-inductively coupled plasma-mass spectrometry (LA-ICP-MS) and sensitive high-resolution ion microprobe (SHRIMP) methods yielded U-Pb ages of 123.0 ± 11.0 and 117.0 ± 3.0 Ma, respectively (Hu et al., 2004; Li et al., 2010). But questions remain as to whether these are truly hydrothermal zircons that formed at relatively low tempera-tures or represent material from igneous country rocks.

Therefore, the timing of gold precipitation in Jiaodong is not well constrained, which hinders our understanding of the exact geodynamics controlling regional gold metallogeny. Was the duration of this giant gold event gradual over at least 15 to 20 m.y., or was it a shorter event that represents a rapid fluid

flux into an upper plate regime? To address this, we conducted new microscopic research on some of the largest Jiaodong gold deposits and identified trace amounts of monazite intergrown with or enclosed in gold and related sulfide minerals. Mona-zite is a robust chronometer because in addition to excluding common Pb, it can incorporate significant amounts of Th and U (Spear and Pyle, 2002). Diffusion of Pb in monazite is negli-gible at temperatures up to 750°C (Harrison et al., 2002; Cher-niak, 2010). Monazite can form from hydrothermal activity by dissolution and reprecipitation reactions at temperatures even below 400°C (Townsend et al., 2000; Rasmussen and Muh-ling, 2007). Monazite is also highly resistant to metamictization (Meldrum et al., 1997), resulting in the probability of Pb loss due to accumulated lattice damage being small. Using samples from the major orebodies in the Jiaodong gold province, we carried out geochemical and geochronological analyses on the associated monazite to address questions related to absolute timing of gold mineralization and its relationship to known tec-tonothermal events in the region.

Fig. 1. (A) Index map showing the location of the Jiaodong Peninsula (modified after Chough et al., 2010; Deng et al., 2015). (B) Simplified geologic map of the Jiaodong gold province, showing the distribution of Mesozoic granitoids (modified after Yang et al., 2014; Deng and Wang, 2016). Abbreviations: OIB = ocean island basalt, UHP = ultra high pressure.

B 120°E 121°E

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Geologic Setting and Previous Dating of the Gold Deposits

Regional geology

The peninsula hosting the giant Jiaodong gold province (Fig. 1) comprises a part of the eastern margin of the North China block (or Jiaobei terrane) and an accreted fragment of the South China block (Sulu orogenic belt). It is bounded by the NNE-trending Tan-Lu fault to the west and the Huanghai Sea on its other sides (Fig. 1A). The western part of Jiaodong comprises the major Sanshandao, Jiaojia, and Linglong ore belts or dis-tricts, as well as the economically less significant Penglai-Qixia belt, whereas gold in eastern Jiaodong is concentrated in the Muping-Rushan belt. The deposits in Jiaodong are controlled by NE- to NNE-trending faults (Qiu et al., 2002; Deng et al., 2018), and more than 90% of the gold resources are concen-trated in the three major belts of western Jiaodong.

The Jiaodong gold province is underlain by Precambrian high-grade metamorphic rocks, which are intruded by Me-sozoic granitoid suites (Fig. 1B). The Precambrian rocks in the North China block include those of the Neoarchean Jia-odong Group that are dominated by tonalite-trondhjemite-granodiorite (TTG) gneisses, the Paleoproterozoic Fenzishan and Jinshan Groups that are dominated by amphibolite-grade metasedimentary rocks, and the Meso-Neoproterozoic Peng-lai Group of metasedimentary rocks (Tang et al., 2008; Zhao et al., 2016). The basement rocks of the South China block in Jiaodong are dominantly Neoproterozoic high-pressure/low temperature (HP-LT) assemblages, although nearer the suture they comprise a mélange of material from both blocks (Liu et al., 2018). The Mesozoic magmatism in the Jiaodong gold province is dominated by the 160~145 Ma Linglong bio-tite granites and 130~122 Ma Guojialing porphyritic grano-diorites (Wang et al., 1998; Goldfarb and Santosh, 2014).

The existing range of Early Cretaceous ages for the gold mineralization in Jiaodong postdates a period when the stress field in eastern China switched from NNW-trending conver-gence to NW-trending extension (Goldfarb et al., 2014). Most workers put the tectonic transition at the start of the Creta-ceous (e.g., Wu et al., 2019), with the extensional deformation continuing from about 136 to 100 Ma (Deng et al., 2017, 2019; Liu et al., 2017), which overlaps almost all of the 40Ar/39Ar ages measured on sericite grains from the gold deposits in Jiaodong. The transition is commonly correlated to the east-ward retreat of the Izanagi slab below the Asian continental margin (Goldfarb et al., 2007; Pirajno and Zhou, 2015). The extensional regime was marked by widespread development of metamorphic core complexes and basin-and-range type NNE-striking features throughout eastern Asia (Qiu et al., 2002; Goldfarb et al., 2014). The early stage of the extensional regime was likely driven by increasing spreading rates and resultant high-speed motion between the Farallon, Izanagi, Phoenix, and newly formed Pacific plates in the Cretaceous Panthalassa Ocean (Goldfarb and Santosh, 2014). At about 120 Ma, however, the movement of all continental plates sta-bilized or slowed down (Liu et al., 2017) as the Phoenix plate was captured by the Pacific plate. During this process, the subduction of the retreating Izanagi plate may have abruptly shifted to a significantly more northerly direction (Goldfarb et al., 2007; Sun et al., 2007).

Geology of the Jiaodong gold deposits

The gold ores are widespread, mainly along NNE- to NE-striking normal faults distributed from west to east across the Jiaodong Peninsula and thus on both sides of the Wulian-Qin-gdao-Sulu suture between the North China and South China blocks (Fig. 1A). The geology of the Jiaodong deposits has been well described, beginning with province overviews by Wang et al. (1998), Qiu et al. (2002), and Fan et al. (2003), and with dozens of deposit-specific papers published during the past 15 years. The larger deposits are generally restricted to the large-scale normal faults on the margins of the NE-striking Jurassic batholiths. The faults separate the Jurassic batholiths from Precambrian high-grade metamorphic rocks or Early Cretaceous granodiorites.

Two styles of mineralization are consistently described in the Jiaodong gold province. The first is represented by the Jiaojia gold deposit, and thus is named as Jiaojia-type (Fig. 1B), in which disseminated and veinlet mineralization is confined to wide cataclastic zones with well-developed al-teration halos. The Jiaojia deposit is controlled by the Jiao-jia fault zone, which is NE trending and NW dipping, and its subsidiary faults. The other mineralization style is called the Linglong-type (Fig. 1B), which is represented by deposits such as Linglong and Rushan. In the Linglong and Rushan deposits, auriferous quartz veins are the primary mineraliza-tion style with less abundant disseminated sulfide zones and/or stockwork veinlets. The veins are structurally controlled by the NEE- to NNE-trending fault zones (Zhang et al., 2007; Yang et al., 2016b).

Quartz-sericite-pyrite alteration dominates both styles of mineralization along the fault zones (Fig. 2A). Chlorite may also be common, whereas carbonate alteration in the gran-itoid hosts is not well developed. Potassium-feldspar altera-tion generally exists as a broader halo surrounding the quartz-sericite-pyrite assemblage and may be the first stage of the hydrothermal activity. The sulfide minerals are mainly pyrite, which is commonly massive, with lesser sphalerite, galena, and chalcopyrite (Fig. 2A); tellurides are rare. Gold in these deposits mainly occurs as microscopic grains of native gold and electrum within pyrite-quartz-sericite assemblages or within microfractures in the veins.

The two styles of mineralization share similar stable isotope and fluid inclusion features. Fluid inclusion studies on ore-stage quartz reveal the dominance of H2O-CO2-NaCl ± CH4 fluids with low salinities of <10 wt % NaCl equiv and local evidence of immiscibility. Homogenization temperatures are in the range of 170°~335°C and estimated entrapment pres-sures are cited as 70~250 MPa. Heavy oxygen and hydrogen isotope data for the ore fluids suggest little surface water in-volvement and 34S values of consistently +7 to +12‰ argue against any type of unaltered mantle source for the sulfur (Qiu et al., 2002; Fan et al., 2003, 2007; Mao et al., 2008; Li and Santosh, 2014).

Existing geochronology

Prior to the middle 1980s, gold deposits on the Jiaodong Pen-insula were assumed by many workers to be Precambrian in age because of the old host rocks. However, more recent age data, collected from the late 1980s onward, showed that the



gold-forming episode is related to the Yanshanian orogenesis, as summarized by Qiu et al. (2002), Zhai et al. (2004), and Chen et al. (2005). They showed that most data indicated ore formation between ca. 130 and 100 Ma, with dating methods dominated by K-Ar and Ar-Ar on mica and Rb-Sr isochrons on multiple mineral phases. These reported ages are from de-posits in three of the four largest districts in the western part of the Jiaodong gold province, including 126.5 ± 5.7 to 100.7 ± 3.6 Ma for Linglong and 134 ± 8 to 88.1 ± 0.1 Ma for Jiaojia, both in the North China block, as well as 121.3 ± 0.6 to 101.8 ± 3.4 Ma for Rushan in the eastern part of the province, which belongs to the South China block.

Geochronology studies have continued to evaluate the tim-ing of the Jiaodong mineralization through an abundance of 40Ar/39Ar dating studies up until the present day. Sericite from many deposits in the western part of Jiaodong yielded argon plateau ages scattered within 5 and 10 m.y. of a 120 Ma mode

in the Sanshandao (Cangshang: Zhang et al., 2003), Jiaojia (Ji-aojia: Li et al., 2003; Wangershan: Li et al., 2015), and Lin-glong districts (Linglong: Li et al., 2008), which together host most of the gold resource in the province. However, this is a time of rapid exhumation of the Precambrian basement and it remains unclear if this age mode truly represents the main part of a very broad gold event. In fact, at Dayingezhuang, to the south of the Linglong district along the same major structure, Yang et al. (2014) dated hydrothermal sericite by 40Ar/39Ar at 130 ± 4 Ma. In the Jiaojia district, although the sericite is dated at 120 Ma, Wang et al. (2015) note that Rb-Sr measurements on pyrite separates from the Xincheng de-posit are about 5 m.y. older and argue that the older age of ca. 125 Ma best reflects the gold event. In contrast, at Dongji in the Jiaojia district, sericite and muscovite yielded younger 40Ar/39Ar ages at ca. 115 Ma (Li et al., 2003). Because of the variability of the reported 40Ar/39Ar data, many workers have

Fig. 2. Simplified geologic profile maps of Jiaojia, Linglong, and Rushan deposits (modified after Hu et al., 2006; Wang et al., 2015; Wen et al., 2015; Yang et al., 2016a; Guo et al., 2017).

Late JurassicLinglong biotite granite

Neoarchean Jiaodong Groupmetamorphic rock

Paleogene sedimentary rock

Fault

K-f eldspar alteration zone

Late JurassicKunyushan monzogranite

Quartz vein

Lamprophyre dike

Orebody

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A JiaojiaA Jiaojia



concluded that the gold event took place from 130 to 110 Ma, thus still arguing for at least a 15- to 20-m.y. duration of hy-drothermal activity in the western part of the province (e.g., Yang et al., 2014).

In the eastern part of Jiaodong, Hu et al. (2004) used SHRIMP U-Pb methods to date zircons from veins in the Jin-qinding deposit in the Rushan district at 117 ± 3 Ma. Howev-er, questions remain as to whether the dated zircons are really hydrothermal in origin. The 40Ar/39Ar ages of hydrothermal mica from the same deposit are reported as ca. 110 to 108 Ma (Li et al., 2006).

Cai et al. (2018) dated molybdenite associated with gold at the Shangzhuang deposit in the Jiaojia district. A well-defined five-point Re-Os isochron age of 126 ± 2 Ma was determined for ores that are hosted in the 129.8 ± 0.5 Ma Guojialing granodiorite. However, there are questions as to whether the molybdenum in the molybdenite is recording the gold event, an earlier (pre-gold) hydrothermal event, or partly the age of granite crystallization, particularly given the generally younger ages of previous studies on gold deposits in the district. Fur-thermore, Ma et al. (2017) noted that molybdenum-bearing quartz veins predated the gold event in the Xiadian deposit (see below) by about 5 m.y. Li et al. (2014) applied Re-Os techniques to three pyrite separates from the Dayingezhuang gold ores and calculated an isochron age of 144.8 ± 1.8 Ma, 15 m.y. older than the 40Ar/39Ar age from the deposit and even older than the host granitoid.

Ma et al. (2017) carried out monazite LA-ICP-MS U-Pb dating at the >200 t Au Xiadian deposit, about 50 km south of the Linglong district and obtained an age of 120.0 ± 1.4 Ma. Li et al. (2018) dated gold-related hydrothermal monazite from the small Zhuangzi deposit located about 25 km east of the Linglong district in the Penglai-Qixia belt. A 207Pb-corrected mean age of 119.0 ± 3.1 Ma was obtained based on analyses of 22 spots on the monazite grains. The adjacent Daliuhang de-posit has a monazite age of 120.5 ± 1.7 Ma (Feng et al., 2018). Similarly, in the 30-t Au Hushan deposit located 20 km south of Zhuangzi in the same belt, Yang et al. (2018) also measured an age of ca. 120 ± 3 Ma by in situ LA-ICP-MS methods on monazite in the gold ores. Collectively and importantly, these new, precise monazite dates from deposits scattered around the gold province are all very consistent at ca. 120 Ma and contrast with the broad spread of previous age data. Thus, it is unclear as to whether the Jiaodong gold deposits in the east-ern and western parts of the province formed over a few tens of millions of years, or during a significantly shorter duration. More high-precision age data for some of the giant Jiaodong deposits are required to address this issue.

Sampling and Analytical Techniques

Sampling description

Three representative ore samples were collected underground from the Jiaojia, Linglong, and Rushan gold deposits for this study. The Jiaojia deposit is characterized by the disseminated and stockwork veinlet ore style controlled by the NE-trend-ing and NW-dipping Jiaojia fault and its subsidiary faults (Fig. 2A). The representative auriferous quartz-sericite-pyrite–al-tered granite sample at Jiaojia was collected from the main orebody at the –270 m level. Monazite grains in the sample

are anhedral and occur in clusters associated with hydrother-mal pyrite in silicified granite (Fig. 3A, B). The Linglong de-posit is distinguished by quartz-sulfide veins hosted within the Late Jurassic Linglong biotite granite. The veins are structur-ally controlled by the NEE- to NNE-trending Potouqing fault zone and the NNE-trending Linglong fault zone (Fig. 2B), vary from 5~120 cm in width, and are surrounded by sericit-ized and silicified granite within a broader halo of K-feldspar alteration. The representative auriferous quartz vein sample at Linglong was collected from the Au50 orebody at the –370 m level. Monazite crystals in this sample are present as small anhedral or subhedral inclusions in hydrothermal quartz (Fig. 3C, D). The Rushan deposit, also referred to as the Jinqing-ding deposit, is in the middle part of the Muping-Rushan gold belt. This quartz vein-type mineralization is stated to include China’s largest lode gold endowment in a single vein (Fig. 2C; Hu et al., 2006). The representative auriferous quartz vein sample, with alteration of surrounding granite similar to that at Linglong, was collected from the main orebody at the –865 m level. Anhedral monazite crystals in this sample are commonly associated with pyrite or occur along fractures and grain boundaries of quartz (Fig. 3E, F).

Doubly polished thin sections (100-μm thick) were prepared for petrographic analysis and examined using a standard optical microscope to investigate their texture, chemistry, and mineral composition. The JEOL JSM-5800LV scanning electron microscope (SEM) at the U.S. Geological Survey (USGS) in Denver, Colorado, was used to automatically identify and locate suitable monazite grains for in situ geochronology. In addition, back-scattered electron (BSE) imaging was performed using SEM facilities at the USGS in Denver and the Development and Research Center of China Geological Survey (CGS) to further characterize microscale textures of monazite grains and associated minerals (Fig. 4).

Electron probe microanalysis of monazite

The geochemical compositions of monazite grains from sam-pled ores at the Jiaojia, Linglong, and Rushan deposits were determined on the doubly polished thin sections by using a JEOL JXA-8100 electron probe microanalyzer equipped with four wavelength dispersive-type spectrometers at the Analyti-cal Laboratory of the Beijing Research Institute of Uranium Geology, Beijing, China. Operating conditions were 20 keV accelerating voltage, a 10 nA beam current (measured on the Faraday cup), and a 2-μm focused electron beam size. The Al-Kα, Si-Kα, Mg-Kα, Y-Lα, and As-Lα were measured with TAP crystal, Ti-Kα, Fe-Kα, Mn-Kα, Hf-Lα, Ta-Lα, Ba-Lα, Ce-Lα, La-Lα, Eu-Lα, Yb-Lα, Tb-Lα, Lu-Lα, Tm-Lα, Nd-Lβ, Gd-Lβ, Sm-Lβ , Pr-Lβ, Dy-Lβ, Er-Lβ, and Ho-Lβ with LiF crystal, and Nb-Lα, U-Mα, Ca-Kα, Pb-Mα, P-Kα, Th-Mα, S-Kα, and Zr-Lα with PETJ crystal, respectively. Average 99% confi-dence detection limits in parentheses are in elemental parts per million. The counting times on the analytical lines, as well as half of this time for background counts on both sides of the peak, were 10 seconds for each of the analyzed elements.

The standards used were as follows: albite for Al; zircon for Zr and Si; pyrope for Mg; yttrium Al garnet (synthetic) for Y; monazite for P, Ce, La, Pr, and Nd, metal uranium, haf-nium, tantalum, ytterbium, gadolinium, samarium, dyspro-sium, erbium, and holmium for U, Hf, Ta, Yb, Gd, Sm, Dy,



Er, and Ho, respectively; bustamite for Ca and Mn; galena for Pb; hematite for Fe; ThO2 (synthetic) for Th; benitoite for Ti; KNbO3 (synthetic) for Nb; arsenopyrite for As; barite for S; EuP5O14, TbP5O14, LuP5O14; and TmP5O14 for Eu, Tb, Lu, and Tm, respectively. The ZAF routine was applied for data correction. Detailed operating conditions and correction stan-dards are provided in Qiu et al. (2019). The analytical data are given in Appendix Table A2 and Appendix Figure A1.

In situ SHRIMP U-Th-Pb dating

Subsequent to the geochemical discrimination of monazite grains on polished thin sections by electron microprobe analy-sis (EPMA), in situ U-Th-Pb dating was conducted on mona-zite in the selected ore samples. Parts of polished thin sections containing monazite grains >10 μm across were drilled out in 2-mm-diameter plugs using a hollow microdrill and cast in 25-mm-diameter epoxy mounts. Before coating with ~40-nm pure gold for analysis by the SHRIMP, the sample mounts

were thoroughly cleaned along with the standard mount fol-lowing established protocols. This involves the use of petro-leum spirit (rinse and 5-min ultrasonic bath), isopropanol (rinse and 5-min ultrasonic bath), soap solution (rinse and 3-min ultrasonic bath), and deionized water (8–10 times in-cluding ultrasonic bath at least twice). Uranium-Th-Pb analy-ses of monazite were performed using the SHRIMP II facil-ity housed at the John de Laeter Centre, Curtin University, Perth, Western Australia. Optical and BSE images were used to guide placement of the primary ion beam during SHRIMP analyses. Analytical procedures and operational settings were similar to those described in detail by Fletcher et al. (2010) and Zi et al. (2019).

The SHRIMP U-Th-Pb data were reduced with the Squid-2 software (version 2.50.11.02.03) (Ludwig, 2012) using spot av-erage values for all ratios. Monazite French (206Pb/238U age = 514 Ma, 208Pb/232Th age = 504 Ma, U = 1,000 ppm) was used as the primary standard for calibrations of Pb/U and Pb/Th

Fig. 3. Photographs of underground exposures and hand specimens of representative gold ores from the Jiaojia (A, B), Lin-glong (C, D), and Rushan (E, F) gold deposits.

A B

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py

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15 cm15 cm

20 cm20 cm



ages and U concentrations. One-dimensional calibrations of 206Pb+/270[UO2]+ and 208Pb+/264[ThO2]+ were used for mona-zite 206Pb/238U and 208Pb/232Th, respectively (Fletcher et al., 2010). Corrections for U, Th, Pb, and REE matrix effects in monazite Pb/U and Pb/Th were carried out subsequently by applying established protocols (Fletcher et al., 2010). Mona-zite Z2908 (207Pb/206Pb age = 1796 Ma) was used to monitor the instrumental mass fractionation in 207Pb/206Pb. Six analy-ses on Z2908 collected during the session returned a weighted mean 207Pb/206Pb age of 1794 ± 8 Ma (mean square of weight-ed deviates [MSWD] = 0.57, 95% confidence level). Data plots were prepared using Isoplot-3 (Ludwig, 2012). Individ-ual analyses are presented with 1σ errors, whereas weighted mean dates are quoted with 95% confidence limits, unless otherwise specified. The 1σ external spot-to-spot error was propagated to the sample data. In addition, the 2σ error in the weighted mean 206Pb/238U date of the calibration standard was propagated in quadrature to the weighted mean dates of the unknowns. In situ SHRIMP U-Th-Pb data collected on monazite grains are summarized in Appendix Table A3.

In situ LA-ICP-MS U-Pb dating

To compare the potential advantage and disadvantage with perspectives of the occurrence and size of monazite grains

from the Jiaodong gold deposits, and the beam size and com-mon lead concentration collected by both LA-ICP-MS and SHRIMP methodologies, in situ U-Pb isotope analyses were carried out using the LA-ICP-MS facility at the Isotopic Lab-oratory, Tianjin Center, China Geological Survey. The mona-zite crystals that were large in diameter (generally >10 μm), clean on the surface, and regular in shape were selected and marked on the doubly polished thin sections by using a mi-croscope and electron microprobe. The marked thin sections were subsequently held in the independent designed sample bracket, through which the latitude-longitude coordinates of the selected crystals were collected. The thin sections were then removed for cleaning with a cotton ball dipped in alcohol (95%) and were put back in their designated locations when dry. Laser sampling was performed using a Neptune multiple-collector (MC)-ICP-MS (Thermo Fisher Ltd.) coupled with a NEW WAVE 193 nm-FX ArF Excimer laser-ablation system (ESI Ltd.). The MC-ICP-MS is a double focusing multicol-lector ICP-MS. The maximum mass dispersion is 17%. This machine has nine Faraday cups, including one fixed central channel and eight movable Faraday cups. The SEM is bound with the central channel and the four ion counters are bound with the L4 Faraday cup. The Excimer LA system pulse width is less than 4 ns with eight different spot sizes of 2, 10, 20, 35,

Fig. 4. Representative BSE images of hydrothermal monazite occurrences. Monazite crystal coexisting with pyrite in K-feld-spar altered granite (A), and intergrown with pyrite in disseminated quartz-sericite-pyrite–altered granite (B-C) at Jiaojia. Monazite crystal enclosed in quartz from quartz-pyrite vein at Linglong (D-F). Monazite crystal hosted along fracture in quartz at Rushan (G-I). Abbreviations: mon = monazite, py = pyrite, qtz = quartz.

A B

D

G

py

py

mon

qtz

K feldspar

py

mon

qtz

monqtz

pypy

pypy

pypy

monmon

monmonmonmon

qtzqtzqtzqtz

qtzqtz

K feldsparK-- feldspar

JiaojiaJiaojia JiaojiaJiaojia

LinglongLinglong

qtz

monmonmon

qtzqtz

RushanRushan

monmon

qtzqtzJiaojiaJiaojiaC

monmon

qtzqtz

LinglongLinglongE

monmon

qtzqtz

LinglongLinglongF

monmon

qtzqtz

RushanRushanH

monmon

qtzqtz

RushanRushanI

10 mμ10 mμ

10 mμ10 mμ

10 mμ10 mμ 15 mμ15 mμ

15 mμ15 mμ

20 mμ20 mμ

20 mμ20 mμ

20 mμ20 mμ20 mμ20 mμ



50, 75, 100, and 150 μm and the ablation frequency of the laser is 1 to 200 Hz. Detailed operating conditions of the la-ser ablation system and the MC-ICP-MS instrument and data reduction are as referred to by Geng et al. (2017) and Horst-wood et al. (2016).

Age data and concordia plots were reported at 1σ er-ror, whereas the uncertainties for weighted mean ages are given at 95% confidence level. The 207Pb/206Pb, 206Pb/238U, 207Pb/235U, and 208Pb/232Th ratios were calculated from mea-sured ion intensities using ICPMSDataCal 8.4 (Liu et al., 2010). Concordia diagrams and weighted mean U-Pb ages were processed using Isoplot version 4 software (Ludwig, 2012). Common-Pb corrections were made using the meth-od of Anderson (2002). All monazite analyses were conduct-ed with a beam diameter of 5 μm, a 5-Hz repetition rate, and energy density of 15 J/cm2. Reference standard material 44069 (SIMS U-Pb age: 424.9 ± 0.4 Ma; Aleinikoff et al., 2006) was analyzed after every five unknowns under iden-tical conditions. The error of LA-MC-ICP-MS analysis is 0.2%, and the error of age data is less than 1% consider-ing both standard reference error and systemic error. De-tailed operating conditions of the laser ablation system and the ICP-MS instrument and data reduction are provided in Qiu et al. (2019). In situ LA-ICP-MS U-Pb data collected on monazite grains are summarized in Appendix Table A4.

Results

Geochemical compositions of monazite

The monazite grains from the three deposits have consistent compositions with 28.52 to 33.70 wt % Ce2O3 and 28.96 to 32.49 wt % P2O5. Their light rare earth element (LREE) concentrations range from 50.44 to 56.88 wt %, and to-tal REE concentrations from 51.32 to 60.91 wt %. All the monazite grains from the three gold deposits show the same REE distribution patterns. They are typified by a weakly negative to slightly positive Ce anomaly varying from 0.81

to 1.03 and a distinct positive Eu anomaly ranging from 2.59 to 11.88 (Fig. 5).

SHRIMP geochronology of monazite

Fifteen analyses were collected from 11 monazite grains from the Jiaojia deposit. They have low to moderate U and Th con-centrations varying from 78 to 251 ppm and 949 to 73,051 ppm, respectively, with Th/U ratios between 7 and 373 (Ap-pendix Table A3). The monazite analyses show a relatively high percentage of common Pb with most analyses having f206 >5% (f206 denotes 204Pb-corrected common Pb fraction of 206Pb). Four spots show >20% of common 206Pb and are excluded. The remaining 11 analyses give a weighted mean age of 121.8 ± 3.6 Ma (n = 11, MSWD = 1.03) (Fig. 6A, B). Fifteen analyses were collected from six monazite grains from the Linglong deposit. Five spots show >20% common 206Pb and one spot records an anomalously low 206Pb*/238U value that decouples from its 208Pb*/232Th. Excluding these six anal-yses, the remaining nine analyses give a weighted mean age of 120.0 ± 4.6 Ma (n = 9, MSWD = 1.12) (Fig. 6C, D). They con-tain 60 to 213 ppm U and 4,882 to 108,174 ppm Th, with high Th/U ratios ranging from 23 to 1,143 (Appendix Table A3).

LA-ICP-MS geochronology of monazite

Eight monazite crystals were analyzed with 20 spots for the Ji-aojia gold deposit sample. Uranium and Th contents are 16 to 205 ppm and 1,413 to 35,339 ppm, respectively. The analyses show Th/U ratios from 11 to 1,187. The 20 analyses include 206Pb*/238U ages ranging from 111 ± 2 to 128 ± 5 Ma (Fig. 7A, B) and define a lower intercept age at 119.8 ± 2.1 Ma (n = 20, MSWD = 1.6). Twenty analyses were made on eight monazite crystals from the Linglong gold deposit. Uranium and Th contents are 5 to 317 ppm and 628 to 31,954 ppm, respectively. The Th/U ratios range from 14 to 1,240. The 20 analyses for 206Pb*/238U ages range from 116 ± 3 to 125 ± 6 Ma (Fig. 7C, D) and yield a lower intercept age at 119.1 ± 1.4 Ma (n = 20, MSWD = 0.66). Eighteen analyses were made

Fig. 5. Chondrite-normalized REE distribution pattern of hydrothermal monazite compositions in this study with comparison to that from peraluminous granitoid and metamorphic environments (from Williams et al., 2007; Y-axis not to scale).

Peralkalinegranitoid

Peralkalinegranitoid

MetamorphicMetamorphic

Smaller to negligibleEu anomaly afterplagioclase breakdown

Smaller to negligibleEu anomaly afterplagioclase breakdown

1,000

10,000

100,000

1,000,000

Sam

ple

Cho

ndri

te/

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

JiaojiaLinglongRushan



on eight monazite crystals from the Rushan gold deposit. The data indicate U concentrations of 73 to 2,068 ppm and high Th concentrations of 625 to 644,096 ppm, with Th/U ratios from 3 to >1,000. The 206Pb*/238U ages ranging from 110 ± 2 to 122 ± 3 Ma (Fig. 7E, F) yielded a lower intercept age at 114.2 ± 1.5 Ma (n = 18, MSWD = 2.2).

Discussion

Defining hydrothermal origin of monazite

Distinguishing with certainty whether monazite in a granit-oid-hosted ore deposit is hydrothermal or magmatic in ori-gin is difficult. However, crystal textures and occurrence of monazite, in combination with mineral geochemistry, can be used to confidently distinguish monazite of different origins (Vielreicher et al., 2003; Rasmussen and Muhling, 2007; Williams et al., 2007; Taylor et al., 2015; Zi et al., 2019). The ThO2 abundance and REE distribution patterns of monazite

are useful discriminators between hydrothermal and igne-ous monazite.

The textural relationships with other alteration phases of igneous minerals suggest the monazite grains in this study are hydrothermal in origin. Furthermore, they have Th concentrations (0.05–3.5 wt %) much lower than magmatic monazites (>5 wt %; e.g., Schandl and Gorton, 2004). The much lower Th concentrations of hydrothermal monazite in-dicate that the solubility of Th4+ is relatively low compared to that of LREE3+ in hydrothermal fluids responsible for monazite precipitation. This may result from the fact that thorium tends to be immobile in moderate temperature, aqueous-carbonic metamorphic fluids (Schandl and Gorton, 2004). Magmatic monazite when crystallizing from a melt is stoichiometrically and charge balanced by a combination of the cherelite and huttonite substitutions (Williams et al., 2007). It is relatively depleted in Eu, because Eu is pref-erentially incorporated into plagioclase when crystallizing

Fig. 6. Representative BSE images showing dated monazite grains, and their relationship with gold-bearing pyrite and quartz from Jiaojia and Linglong. Concordia diagram and 206Pb/238U weighed mean age of hydrothermal monazite analyzed by SHRIMP.

0.00

0.07

0.14

0.21

0.28

0.35

0.42

0.49

0.0

0.1

0.2

0.3

0.4

30 40 50 60 70

121.8±3.6 Man=11, MSWD=1.03

35 45 55 65 75

20

62

38

Pb/

Uw

eigh

ted

mea

nag

e2

06

23

8P

b/U

wei

ghte

dm

ean

age

Jiaojia

1

2

123±3 Ma123±3 Ma3

116±5 Ma116±5 Ma

112±9 Ma112±9 Ma

monmon

pypy

1

115±6 Ma115±6 Ma4

106±8 Ma106±8 Ma3117±13 Ma117±13 Ma

7125±6 Ma125±6 Ma

12124±4 Ma124±4 Ma

11124±5 Ma124±5 Ma

monmon

qtzqtz

20

72

06

Pb /

Pb

238 206U/ Pb

Linglong

20

72

06

Pb/

Pb

238 206U/ Pb

80

100

120

140

160

180

80

100

120

140

160

180

A

B120.0±4.6 Ma

n=9, MSWD=1.12



in equilibrium with magmatic monazite (Zhu and O’Nions, 1999; Kim et al., 2005). In contrast, the REE distribution patterns of monazite analyzed in this study show distinct Eu positive anomalies, suggesting a hydrothermal system that did not involve plagioclase crystallization. These petrologic, mineralogical, and chemical traits indicate that the mona-

zites analyzed in our study from altered rock at various Jia-odong gold deposits are hydrothermal in origin.

Analytical techniques applied to monazite geochronology

Traditional dating of monazite grains has long been performed by separation of grains from the host rocks for dissolution or

Fig. 7. Concordia diagrams and 206Pb/238U weighed mean ages of hydrothermal monazite analyzed by LA-ICP-MS.

98

102

106

110

114

118

122

126

130

90

100

110

120

130

140

95

105

115

125

135

145

B119.8±2.1 Man=20, MSWD=1.6

D

F

Jiaojia

Linglong

Rushan

A Jiaojia

C Linglong

RushanE

238 206U/ Pb

119.1±1.4 Man=20, MSWD=0.66

114.2±1.5 Man=18, MSWD=2.2

238 206U/ Pb

238 206U/ Pb

20

72

06

Pb/

Pb

20

72

06

Pb/

Pb

20

72

06

Pb/

Pb

102106110114118122126130134

0.04

0.06

0.08

0.10

46 50 54 58 62

105115125135145155

0.04

0.05

0.06

0.07

0.08

0.09

40 44 48 52 56 60 64

100110120130140150

0.04

0.05

0.06

0.07

0.08

42 46 50 54 58 62 66

20

62

38

Pb/

Uw

eigh

ted

mea

nag

e2

06

23

8P

b/U

wei

ghte

dm

ean

age

20

62

38

Pb/

Uw

eigh

ted

mea

nag

e



epoxy mounting and dating, but this would inevitably cause the loss of textural context and also allow potential mixing of mona-zites with different origins (Vielreicher et al., 2003; Rasmussen and Muhling, 2007; Williams et al., 2007; Qiu and Yang, 2011). These issues were avoided in the present study by applying in situ techniques, i.e., analyzing monazite grains in doubly pol-ished thin sections by SHRIMP and LA-ICP-MS.

Monazite grains analyzed by SHRIMP and LA-ICP-MS yielded identical results for the Jiaojia and Linglong deposits, mutually attesting to the robustness of both analytical methods (Figs. 6, 7). Unlike monazite crystallized from igneous sources, hydrothermal monazite in gold deposits can have relatively higher common Pb contents because the ore fluid can locally concentrate wall-rock Pb during fluid-rock interaction (e.g., Goldfarb and Groves, 2015). Use of 204Pb to correct SHRIMP U-Th-Pb results is an approach that increases the precision of the data relative to those data from LA-ICP-MS, for which such a correction cannot be carried out. Furthermore, using 204Pb-corrected SHRIMP results can increase the precision of the data when the f206 is <20%. Once the proportion of com-mon Pb is higher (e.g., the f206 is >20%), the SHRIMP results, however, can be abnormal and cannot provide a robust age (Taylor et al., 2015; Zi et al., 2019). A larger sampling volume in LA-ICP-MS compared to SHRIMP therefore can buffer the local high common Pb, and thus give an effective age of 114.7 ± 1.4 Ma for the Rushan monazite with the high common Pb (Fig. 7).

Implications for geodynamic controls on the genesis of the Jiaodong gold ores

The new geochronological results for the giant gold camps of Linglong and Jiaojia in western Jiaodong indicate a major gold

episode at 120 Ma. These results are also consistent with other recently published monazite ages from the Xiadian deposit to the south of the Linglong district (Ma et al., 2017) and from the Penglai-Qixia belt to the east (Feng et al., 2018; Li et al., 2018; Yang et al., 2018). Collectively, these data suggest that the immense gold-related hydrothermal event responsible for the accumulation of much of the >4,000 t Au in Jiaodong was extremely limited in duration, occurring over a time span of only a few million years. This is in contrast to conclusions based on previously published data, which suggested a much longer duration of 15 to 20 m.y. for the gold-forming hydrothermal event despite a similar median age at ca. 120 Ma (Fig. 8).

The new data reported in this paper include the first high-precision monazite age for gold in the Neoproterozoic Sulu terrane of the South China block on the easternmost part of the peninsula, an area that accounts for about 10% of the overall resource in the Jiaodong gold province. Conflicting 40Ar/39Ar ages for Rushan based on hydrothermal sericite in-clude those first suggested as ca. 109 to 108 Ma (Li et al., 2006) and more recently as ca. 120 Ma (Zhang et al., 2020). The latter is indeed consistent with the major gold event in western Jiaodong. In contrast, our 114.2 ± 1.5 Ma monazite date for Rushan suggests a discrete gold event occurred about 5 m.y. later than the deposits to the west in the North China block. Given the many questions described above regarding the existing argon geochronology, we believe the ca. 114 Ma age for Rushan is the most reliable age for the gold event in the South China block. Additional high-precision ages from a few other deposits in the Sulu terrane are, however, still needed to confirm this hypothesis.

These data collectively continue to support the opinion that the gold mineralization in Jiaodong occurred during the

Fig. 8. Comparison of LA-ICP-MS monazite U-Pb isotope ages, hydrothermal zircon ages, and sericite Ar-Ar ages in the Jiaodong gold province.

Jiaojia Linglong Rushan90

160

150

140

130

120

110

100

170

80

Age (Ma)

NW

Wth

rust

and

com

pres

sion

NW

norm

alan

dex

tens

ion

Tan-Lu fault

Linglong biotite granite

Number

51015

Guojialing granodiorite

OIB-like dike

Arc-like dike

U-Pb LA-ICP-MS/SHRIMP ZirconAr-Ar (Sericite)

U-Pb SHRIMP(Monazite)U-Pb LA-ICP-MS Monazite



extensional regime along eastern Asia and was particularly re-lated to large-scale plate reorganizations (e.g., Bierlein et al., 2006; Goldfarb et al., 2007; Sun et al., 2007; Li et al., 2019). The proposed relatively younger gold mineralization age at Rushan in eastern Jiaodong compared to those of the Lin-glong and Jiaojia deposits in western Jiaodong could relate in some manner to the eastward rollback of the Izanagi plate during the extension (Kusky et al., 2014; Geng et al., 2017; Wu et al., 2019; Fig. 9). However, the temporal restriction of the gold event to a very narrow part of the much longer period of extension, related magmatism, and slab rollback indicates that the gold event must have been triggered by a more specific process.

Two possible hydrologic regimes for the gold event were suggested by Goldfarb and Santosh (2014). The exceptional fluid migration episode at 120 Ma correlates with the record-ed onset of decreased spreading rates and plate velocities (Liu et al., 2017), which potentially would have enhanced fluid pressure cycling and fluid migration along a slow subduction megathrust above the downgoing and dehydrating Izanagi plate (e.g., Warren-Smith et al., 2019). Such fluid would mi-grate updip along an impermeable interface between the overriding crust and the subducting slab until intersecting fa-vorable structures in the former (e.g., Hyndman et al., 2015). A problem with this first scenario, however, would be that the slab began rolling back about 20 m.y. prior to the gold event, as defined by the onset of regional extension in eastern Asia (Wu et al., 2019). If this is correct, as is argued in most of the presently accepted geodynamic models, then any slab-derived fluid would have been lost to the developing mantle wedge significantly prior to mineralization.

The alternative fluid scenario would involve extensive ser-pentinization of the mantle wedge during the Late Jurassic Izanagi slab subduction and dehydration (Goldfarb and San-tosh, 2014). Such an event would broadly correlate with the period of Late Jurassic adakite-like magmatism over much of

the Jiaodong Peninsula, where Precambrian lower crust was also hydrated and consequently melted. Much of the water as well as the gold and sulfur also likely originally contained in the subducting slab were stored in the serpentinized mantle wedge for about 20 m.y., to be subsequently and dramatically released during a transient geodynamic event at 120 Ma. Our preferred scenario would be the development of a slab-gap during the earlier mentioned shifting Izanagi motion at rough-ly that time. In fact, Kusky et al. (2014) have hypothesized the opening of such a gap at ca. 120 Ma, during the ongoing extensive decratonization and crustal extension in the eastern North China block (Fig. 9). In this geodynamic setting, a large volume of water would be released into the roots of structures transecting the overlying lithosphere in a few million years (e.g., Kirby et al., 2014; Deng et al., 2019). Specifics of such a hypothesized gap are impossible to define because the entire crust of the Izanagi plate has been lost below eastern Asia such that all constraints on plate history are based on a variety of competing hypotheses (e.g., Seton et al., 2012). Neverthe-less, a gap along the spreading ridge between the Izanagi and Pacific, or even one caused by spreading of a small Mesozoic microplate from the hypothesized Izanagi plate, could have caused devolatilization of the fertilized wedge.

The voluminous gold-transporting fluid is consistently aque-ous-carbonic in composition (Pirajno et al., 1997; Fan et al., 2003, 2007; Kolb et al., 2015; Guo et al., 2017), similar to that of all orogenic gold deposits. Typically, however, very low CO2 fluxes were believed to be generated in the non-arc subduction environment. It is now recognized that a slab at shallow levels, such as below a delaminated thinned craton, would release sig-nificant amounts of CO2 into the overlying environment (e.g., Barry et al., 2019; Gorce et al., 2019), rather than solely recy-cling the carbon into the mantle. Furthermore, the dehydration of mafic crust and related sediments along the downgoing slab could add significant amounts of H2S to the wedge (Alt et al., 2012). Therefore, a relatively brief 120 Ma thermal event de-

Fig. 9. Model illustrating the geodynamics and timing of the easterly rollback of the Izanagi (paleo-Pacific) slab leading to dehydration of the previously fertilized mantle wedge and release of auriferous fluid. Auriferous fluid release was concen-trated at ca. 120 Ma (Jiaojia, Linglong) but continued for another 5 m.y. into eastern Jiaodong (Rushan).

EJapaneseArc

0

Dep

th(k

m)

100

120→115 Ma

Western Jiaodong Eastern Jiaodong

25

50

75Rollback

SerpentiniteSubmarinesediments

Younging Gold Mineralization

Crust

Asthenosphere Lithosphere

Jiaojia RushanLinglong

Melt rising

Ore-f orming fluid

Golddeposits

Subcontinental Lithospheric Mantle

Tan-lu FaultWulian-Yantan

Fault

Izanagi Plate



volatilizing the hydrated mantle wedge would potentially pro-duce voluminous fluid not significantly different in composition from other regional metamorphic fluids.

ConclusionsTextural and geochemical characteristics revealed that the monazite crystals in the major Jiaodong gold province depos-its at Linglong, Jiaojia, and Rushan are hydrothermal in ori-gin. The in situ dating methods using SHRIMP U-Th-Pb and LA-ICP-MS U-Pb on doubly polished thin sections provided the most robust temporal constraints on the gold mineraliza-tion in Jiaodong. We affirmed the validity of the LA-ICP-MS dating for hydrothermal monazite that may partly overcome the issue of high common Pb.

Our new robust geochronological data have improved our understanding of gold ore genesis in the Jiaodong province. The giant resource within the North China block was formed over only a few million years of time at ca. 120 Ma; previ-ous ages using less robust dating techniques, which may be 10 to 15 m.y. older or younger than the consistent monazite ages obtained in this and in previous studies, are erroneous or define relatively minor mineralization events. The postsub-duction opening of a slab gap at ca. 120 Ma is the most likely cause of serpentinite devolatilization in the mantle wedge and the release of a major volume of gold-transporting aqueous-carbonic fluid that was stored in the wedge. Although more high-quality geochronological data are required, initial mea-surements suggest that the small portion of the overall gold resource in the South China block within the eastern part of the Jiaodong Peninsula may be ~5 m.y. younger than that in the North China block.

AcknowledgmentsThe authors would like to thank Editor-in-Chief Larry Meinert, Associate Editor Massimo Chiaradia, and one anonymous re-viewer for providing constructive comments and help during review. This work was financially supported by the National Natural Science Foundation of China (41230311, 41572069, 41702069), the National Key Research Program of China (2016YFC0600107-4, 2016YFC0600307), the State Key Lab-oratory of Geological Processes and Mineral Resources at the China University of Geosciences (GPMR201812), and the 111 Project of Ministry of Science and Technology (BP0719021).

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Jun Deng is a professor at the China University of Geosciences (Beijing). He received his B.Sc. (1981) and M.Sc. (1989) degrees from the China University of Geosciences (Wuhan), and Ph.D. (1992) from Chinese Academy of Geological Sci-ences. In last 30 years, he has devoted himself to the genesis and resource prospects of gold deposits in Jiaodong. Since 2009, he has organized two National Key Basic Research Development Programs as chief scientist funded by Ministry of Sciences and Technology, China. These two programs contribute to the topic of “Accre-tionary and continent-collisional orogenesis and the associated mineralization in Tethyan regime, SW China.”


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