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Article

Geochronological Constraints on the Genesis of the Changshitougounao Gold Deposit, Qinling Orogen

by
Xian-Fa Xue
1,
Sheng-Xiang Lu
2,*,
Shou-Xu Wang
2,
Da-Hu Yuan
3,
Zheng-Wang Zeng
4,
Jin-Hong Qiu
1 and
Jie Wang
1,5,*
1
State Key Laboratory of Geological Processes and Mineral Resources, Frontiers Science Center for Deep-Time Digital Earth, School of Earth Sciences and Resources, China University of Geosciences, Beijing 100083, China
2
Shandong Gold Geology and Mineral Exploration Co., Ltd., Laizhou 261400, China
3
The Third Geological and Mineral Exploration Institute of Gansu Provincial Bureau of Geology and Mineral Resources, Lanzhou 730000, China
4
Northwest Gold Co., Ltd., Lanzhou 730050, China
5
Centre for Exploration Targeting, School of Earth Sciences, The University of Western Australia, 35 Stirling Hwy, Crawley, WA 6009, Australia
*
Authors to whom correspondence should be addressed.
Minerals 2025, 15(9), 903; https://doi.org/10.3390/min15090903
Submission received: 6 July 2025 / Revised: 14 August 2025 / Accepted: 16 August 2025 / Published: 26 August 2025
(This article belongs to the Special Issue Gold–Polymetallic Deposits in Convergent Margins)
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Abstract

The Western Qinling Orogenic Belt, China’s second-largest Au-metallogenic province, hosts numerous polymetallic deposits, with gold resources particularly concentrated in the northwestern Xiahe–Hezuo area. The Changshitougounao gold deposit, located south of the Xiahe Fault, comprises disseminated ores controlled by near E–W-trending faults and is primarily hosted in quartz diorite and the Lower Triassic Longwuhe Formation. Zircon LA–ICP–MS U–Pb dating of fresh quartz diorite yields an age of 241.8 ± 2.6 Ma. Two generations of monazite were identified: type I magmatic monazite and type II hydrothermal monazite. Type I monazite is intergrown with feldspar, quartz, and biotite, and in situ LA–ICP–MS U–Pb analysis gives an age of 239.2 ± 2.2 Ma. Type II monazite occurs as irregular granular aggregates associated with Au-bearing sulfides and hydrothermal sericite, with an in situ U–Pb age of 230 ± 3.5 Ma. Apatite, also coeval with Au-bearing sulfides and type II monazite, yields an LA–ICP–MS U–Pb age of 230.9 ± 2.5 Ma and 230.7 ± 3.0 Ma. Zircon and type I monazite thus constrain the emplacement of the ore-bearing quartz diorite to ca. 240 Ma, whereas hydrothermal type II monazite and apatite constrain the timing of mineralization to ca. 230 Ma. The ~10 Ma interval between magmatism and mineralization indicates that goldmineralization in the Changshitougounao deposit is decoupled from Early Triassic magmatic activity. Integrating previous studies of the West Qinling geodynamic evolution, we infer that the Changshitougounao deposit formed during collisional orogenesis, in response to the closure of the Paleo-Tethys Ocean. Consequently, the Changshitougounao gold deposit is best classified as an orogenic gold system. Pyrite–arsenopyrite and sericite alteration serve as effective exploration vectors, and the contact zone between quartz diorite veins and slate represents a favorable structural setting for ore prospecting.

1. Introduction

Accurately constraining the timing of orogenic gold mineralization is fundamental to understanding both deposit genesis and geodynamic evolution [1,2,3]. The West Qinling Orogenic Belt, situated between the North China and South China Blocks, hosts over 2280 t of gold, making it China’s second-largest gold province (Figure 1) [4,5]. The Xiahe–Hezuo area represents the largest gold-bearing metallogenic cluster in West Qinling, with more than 665 t of gold and numerous polymetallic deposits [6,7]. The host rocks comprise widespread Early–Middle Triassic granitoids and Devonian–Permian sedimentary rocks [8,9]. Zircon U–Pb geochronology indicates regional magmatic activity at ca. 250–235 Ma [10,11,12,13,14]. There are two predominant deposit types in the Xiahe–Hezuo area: orogenic gold (-antimony) deposits and magmatic–hydrothermal deposits [15,16,17]. Hydrothermal sericite, apatite, and monazite ages suggest that orogenic gold mineralization was concentrated between ca. 235 Ma and 210 Ma, exemplified by Zaozigou (106 t), Jiagantan (153 t), Yidinan (34 t), and Nanban (2.6 t) deposits [13,14,18,19,20]. In contrast, intrusion-related gold systems, such as the Ludousou and the Dewulu Cu–Au skarn, record emplacement ages of ca. 250–235 Ma [15,21,22]. The Changshitougounao deposit, whose orebodies are entirely concealed and located south of the Xiahe–Hezuo fault, makes precise determination of its mineralization timing crucial for understanding its genesis. This also provides a framework for constraining its origin and guiding future exploration in the Gannan area. In this study, we describe the geology of the Changshitougounao gold deposit and innovatively apply coeval U–Pb geochronology of magmatic zircon, hydrothermal monazite, and apatite to precisely constrain the timing of magmatic activity and gold mineralization.

2. Regional Geology

The Qinling Orogenic Belt, a principal segment of the Central China Orogenic Belt, extends > 1500 km E–W across central China (Figure 1) [23,24,25]. Its northern boundary is delineated by the Lingbao–Lushan–Wuyang Fault and Qilian Orogen, demarcating the North China Block [26,27]. The southern margin is defined by the Mianlue–Bashan–Xiangguang and Songpan–Ganzi Faults, separating it from the South China Block [2,28]. Three major sutures, Kuangping, Shandan, and Mianlue, subdivide the belt into the southern North China Block, the North Qinling Block, the South Qinling Block, and the northern South China Block [29]. The Kuangping Suture, located between the South China Block and the North Qinling Block, is characterized by extensive Paleo- to Mesoproterozoic ophiolitic mélanges, dominated by greenschist- and amphibolite-facies volcanic-arc rocks dated at ca. 1.45–0.95 Ga [27]. The Shangdan Suture to the south contains Paleozoic ophiolitic assemblages with subduction-related volcanic-sedimentary suites [30]. The Mianlue Suture, located between the South Qinling Block and the South China Block, comprises ophiolitic mélanges, ocean–island basalts, and island-arc volcanic sequences [31,32,33].
Bounded by the Huicheng Basin and Foping Anticline, the Qinling Belt is conventionally divided into the East and West Qinling Orogenic Belts [34,35]. The West Qinling Orogen preserves a record of polyphase tectonism associated with the Paleo-Tethys Ocean evolution, culminating in the Late Triassic North China–South China block collision, constituting the eastern Paleo-Tethys Oceans [36,37]. Devonian–Triassic sedimentary cover is widespread, whereas exposure of Precambrian basement is sparse [31]. Mesozoic magmatism was vigorous, especially during the Early to Middle Triassic, and gave rise to numerous orogenic and magmatic–hydrothermal gold deposits, making it China’s second largest gold-bearing district [5,17,24,38,39,40,41,42]. Situated at the northwestern margin of the West Qinling Orogen, the Xiahe–Hezuo area comprises Carboniferous–Triassic marine sedimentary sequences intruded by Early–Middle Triassic granitoids, with subsidiary Permian volcanics and Cretaceous volcaniclastic units [37]. NWW-trending structures, notably the Xiahe–Hezuo Fault and the Xinbao–Lishishan anticline, dominate the regional structural fabric. South of the Xiahe–Hezuo Fault, the area is subdivided into northeast and southwest domains, marked by porphyry–skarn gold deposits genetically linked to Triassic granitoids, and by vein–disseminated gold–antimony deposits, respectively [43,44].

3. Deposit Geology

The Changshitougounao gold deposit (102°34′15″–102°41′00″E, 35°04′30″–35°10′00″N) is situated near Damai Village, east of Xiahe County in Gansu Province. Systematic exploration, initiated in 2014 by the Gansu Provincial Bureau of Geology and Minerals Exploration and Development has defined resources > 1 t Au at 2.53 g/t. The Changshitougounao is a concealed deposit with no surface expression, and it remains at an early exploration stage without any underground workings [45,46]. Mineralization is hosted principally within Triassic quartz diorite intrusions and the Longwuhe Formation metasedimentary sequence (Figure 2). The Longwuhe Formation comprises predominantly silty and argillaceous slates interlayered with minor clastic limestone and fine sandstone. Structural control is exerted by both regionally extensive E–W-trending and secondary E–W-trending faults. The former serve as the principal ore conduits and dilatant zones, while the latter are subordinate fractures that localize mineralization. Quartz diorite dikes intrude along the E–W fracture corridors. Alteration assemblages are characteristic of mid- to low-temperature fluids and include silicification, pyritization, carbonatization, and arsenopyrite mineralization. Pyrite and arsenopyrite are the principal sulfide phases, with subordinate stibnite locally present. Gold occurs exclusively as invisible inclusions or lattice-bound forms within pyrite and arsenopyrite. And no native gold was observed in our petrographic analysis [45].

4. Samples and Analytical Methods

4.1. Sample Descriptions

Three quartz diorite samples were selected from drill holes Zk11701 and Zk11702 along exploration line 117: one fresh sample (24CSTGN01) and two mineralized samples (24CSTGN02 and 24CSTGN03). Zircon U–Pb dating was performed on 24CSTGN01 to constrain the crystallization age of the intrusive body. Hydrothermal monazite and apatite U–Pb dating was conducted on 24CSTGN02 and 24CSTGN03 to determine the timing of mineralization.
The fresh quartz diorite (sample 24CSTGN01) is gray-black and massive, with discernible quartz grains and minor coarse-grained dark minerals, including biotite and hornblende (Figure 3). Phenocrysts constitute ~50% of the rock volume, comprising plagioclase (~25%), quartz (~15%), biotite (~5%), and hornblende (~5%). Plagioclase and quartz phenocrysts typically range from 0.2 to 1.0 mm. Biotite and hornblende phenocrysts are generally 0.2–0.3 mm. Plagioclase and quartz occur as tabular grains, biotite as euhedral flakes, and hornblende as prismatic crystals. The fine-grained groundmass is cryptocrystalline, comprising plagioclase (15%–30%), quartz (5%–25%), and accessory zircon and apatite.
The two mineralized quartz diorite samples (24CSTGN02 and 24CSTGN03) are also gray-black but display pervasive alteration (Figure 4). Primary minerals include quartz, feldspar, sericite, pyrite, arsenopyrite, and minor stibnite. Plagioclase and biotite phenocrysts exhibit varying degrees of sericitization to fine-grained sericite. The groundmass consists of plagioclase, quartz, and subordinate K-feldspar, with accessory apatite, monazite, and sericite (Figure 5). Pyrite occurs both as euhedral grains and as disseminated aggregates, locally accompanied by intense sericitization. Detailed petrographic observations of monazite and apatite were carried out using both optical microscopy (Leica DM2700P, Leica Microsystems, Wetzlar, Germany) and scanning electron microscopy (SEM) (Thermo Fisher Scientific, Waltham, MA, USA) at China University of Geosciences, Beijing, to ensure that the dated grains accurately reflect the age of the gold deposit.

4.2. Analytical Methods

4.2.1. Zircon and Apatite LA–ICP–MS U–Pb Dating

The fresh quartz diorite and mineralized samples were first crushed to 40–60 mesh. Zircon and apatite crystals were separated using conventional heavy-liquid and magnetic techniques, then handpicked under a Leica M205C binocular microscope (Leica Microsystems, Wetzlar, Germany) at the Langfang Regional Geological Survey, Hebei Province. Selected grains were mounted in epoxy, polished to ~50% thickness to expose internal features, and cleaned in a 5% HNO3 ultrasonic bath. Before U–Pb analysis, mounts were carbon-coated for cathodoluminescence (CL) imaging. Zircon CL micrographs were acquired with a JXA-880 electron microscope (JEOL Ltd., Tokyo, Japan) (20 kV, 20 nA) at the Langfang Regional Geological Survey, Hebei Province. Apatite CL images were captured on a Tescan GAIA 3 SEM (TESCAN ORSAY HOLDING, a.s., Brno, Czech Republic) at the Beijing Research Institute of Uranium Geology. All grains were meticulously examined to document internal zoning, inclusions, and fractures.
Zircon LA–ICP–MS U–Pb age dating was performed using a Thermo Fisher Neptune multicollector ICP-MS (Thermo Fisher Scientific, Waltham, MA, USA) coupled with an ESI New Wave 193 nm FX ArF excimer laser ablation system (Elemental Scientific Lasers, Bozeman, MT, USA) at Tianjin Center, China Geological Survey. The laser beam spot diameter was set to 30 μm with an 8 Hz repetition rate. The zircon standard GJ-1 was used for U–Pb age calibration, and NIST SRM 610 glass was used as an external standard for determining U, Th, and Pb concentrations in zircon. Apatite LA–ICP–MS U–Pb age determinations were carried out using a laser ablationmulticollector ICP-MS system consisting of a New Wave 193-FX ArF excimer laser coupled to a Thermo Fisher Neptune MC–ICP–MS at Tianjin Center, China Geological Survey. The laser spot size was 40 μm. NIST SRM 610 glass was used as the external standard for elemental concentrations, and Otter Lake monazite was used as the apatite U–Pb age standard. Isotopic ratios of zircon and apatite were calculated using ICPMSDataCal 11.8 [47], and data processing methods were used with Isoplot 3.0 [48].

4.2.2. Monazite LA–ICP–MS U–Pb Dating

Monazite grains were first identified in doubly polished thin sections using optical microscopy and SEM at China University of Geosciences, Beijing, then targeted for in situ U–Pb analysis. Geochronological measurements were conducted at Yanduzhongshi Geological Analysis Laboratories Ltd. Analyses were performed on an Analytik Jena PQMS quadrupole ICP-MS coupled to a NWR193 193 nm ArF excimer laser, employing 30 µm spot sizes at ~4 J/cm2 laser fluence. Common-Pb corrections followed the 207Pb-based are detailed in the references [49,50]. NIST SRM 610 glass was used as an external standard for the determination of U, Th, and Pb concentrations. Monazite 44069 was used as the external standard for monazite U–Pb dating analyses. Concordia diagrams U–Pb ages were processed using Isoplot 3.0.

5. Results

5.1. Zircon U–Pb Geochronology

LA–ICP–MS U–Pb analyses of the fresh quartz diorite (sample 24CSTGN01) is shown in Supplementary Table S1. Cathodoluminescence (CL) imaging (Figure 6A) reveals that most grains are euhedral with well-developed oscillatory zoning. Grain lengths range from 100 to 200 µm, with aspect ratios of 2:1 to 3:1 and Th/U ratios above 0.28, consistent with magmatic zircon [51]. Nineteen grains were analyzed, of which seventeen yielded concordant ages. The weighted mean 206Pb/238U age is 241.8 ± 2.6 Ma (MSWD = 1.6; n = 17; Supplementary Table S1, Figure 6B).

5.2. Monazite U–Pb Geochronology

Two distinct types of monazites (Type I and Type II) have been identified based on textural and compositional criteria. Type I monazite predominantly occurs within biotite (Figure 5A,B). It typically forms euhedral to subhedral single crystals. LA–ICP–MS analyses reveal uniformly high Th abundances, ranging from 4340 to 73,000 ppm (mean: 21,027 ppm), with Th/U ratios constrained between 24.1 and 968.2. In situ U–Pb dating of this monazite type, summarized in Supplementary Table S2 and displayed on a Tera–Wasserburg concordia diagram, yielded a lower intercept age of 239.2. ± 2.2 Ma (MSWD = 0.34, n = 18) (Figure 7A).
Type II monazite is characteristically anhedral, with abundant dissolution cavities, and commonly forms irregular aggregates of fine-grained anhedral crystals (Figure 5C–F). This type exhibits highly variable Th concentrations (884–42,700 ppm; mean = 18,229 ppm) and a broad range of Th/U ratios (0.51–159.3). In situ U–Pb dating defines a lower intercept age of 231.0 ± 3.5 Ma (MSWD = 0.9, n = 22; Supplementary Table S2; Figure 7B).

5.3. Apatite U–Pb Geochronology

Apatite separates from samples 24CSTGN02 and 24CSTGN03 occur as semi-euhedral to anhedral grains within or adjacent to pyrite and arsenopyrite. CL images reveal two types of luminescence: one appears black with greenish rims, and the other is uniformly green. Despite these differences, both types yield consistent LA–ICP–MS lower intercept ages of 230.9 ± 2.5 Ma (MSWD = 1.6, n = 28; Supplementary Table S3; Figure 8) and 230.7 ± 3.0 Ma (MSWD = 3.0, n = 42; Supplementary Table S3; Figure 8), indicating consistent ages.

6. Discussion

6.1. Origin of Monazite and Apatite

Monazite and apatite are ubiquitous accessory silicate minerals that can form via magmatic, metamorphic, and hydrothermal processes [52,53,54]. Type I monazite occurs as euhedral grains intergrown with quartz and magmatic biotite, consistent with a magmatic origin (Figure 5A,B) [55]. In contrast, Type II monazite forms irregular aggregates of multiple anhedral to subhedral micro-grains, a habit distinct from magmatic monazite (Figure 5C–F). Petrographic observations show that Type II monazite is intimately associated with pyrite, arsenopyrite, and sericite, indicating coeval crystallization with sulfide mineralization from a common hydrothermal fluid [21,41,42,56,57,58]. Monazite has a relatively high closure temperature of approximately 700–750 °C, making it a robust geochronometer that is generally resistant to resetting during low- to medium-grade metamorphism [59]. Therefore, the low- to medium-grade metamorphism that occurred in the Xiahe–Hezuo district during north-directed subduction and collision of the Paleo-Tethys Ocean (~250–230 Ma) would not have reset the U–Pb isotopic system in monazite [42,55,60,61]. Additionally, apatite occurs mainly at the margins of or within sulfide phases, and cathodoluminescence images show evidence of hydrothermal dissolution and reprecipitation, indicating alteration by mineralizing hydrothermal fluids (Figure 5E–H).

6.2. Magmatism Timing

The ore-hosting intrusion of the Changshitougounao gold deposit is a quartz diorite. LA–ICP–MS U–Pb dating of magmatic zircon from the fresh quartz diorite yields an age of 241.8 ± 2.6 Ma, while magmatic monazite yields 239.2 ± 2.2 Ma. These ages overlap within analytical uncertainty and indicate a crystallization age of ca. 240 Ma for the host intrusion.
Regional studies document widespread Early–Middle Triassic magmatism in the Xiahe–Hezuo area (ca. 250–235 Ma; Figure 9) [17,19,38,62]. Specifically, the Ayishan intrusion crystallized at 242–238 Ma, the Dewulu complex at 247–238 Ma, the Tongren intrusion at 242–238 Ma, the Meiwu intrusion at 251–243 Ma, and the host rock at Zaozigou, Ludousou, Zaorendao, and Yidinan similarly crystallized at ca. 235–250 Ma [3,22,36,63,64,65,66]. In close agreement with these regional data, zircon and magmatic monazite from the fresh quartz diorite of the Changshitougounao gold deposit define ages of ca. 240 Ma, confirming that the Changshitougounao gold deposit formed during the Early Triassic magmatic episode in the West Qinling orogen.

6.3. Mineralization Timing

The in situ LA–ICP–MS U–Pb ages of hydrothermal monazite (231.5 ± 3.5 Ma) and apatite (230.9 ± 2.5 Ma, 230.7 ± 3.0 Ma) constrain gold mineralization at the Changshitougounao gold deposit to ca. 230 Ma. This age is consistent with regional orogenic gold mineralization in the Xiahe–Hezuo district, which is concentrated between 235 Ma and 210 Ma, as exemplified by the Zaozigou deposit (ca. 211 Ma, hydrothermal monazite in situ LA–ICP–MS U–Pb), and the Yidinan deposit (232 Ma, hydrothermal monazite in situ LA–ICP–MS U–Pb) [21,67]. In contrast, regional magmatic–hydrothermal deposits formed earlier, between 250 Ma and 235 Ma, including the Laodou deposit (249.1 Ma and 235 Ma, hydrothermal sericite 40Ar/39Ar), Au–Cu skarn deposits adjacent to the Dewulu intrusion (ca. 240 Ma, hydrothermal sericite 40Ar/39Ar), and the Xiekeng–Jiangligou–Shuangpengxi polymetallic deposit (ca. 240 Ma, molybdenite Re–Os) [2,15,19,22,65,68,74,75]. Thus, the ca. 230 Ma mineralization age at Changshitougounao aligns with the regional orogenic gold event. These data bracket mineralization in the district coeval with, or slightly younger than, Early Triassic magmatism.

6.4. Genetic Classification of the Changshitougounao Gold Deposit

The Xiahe–Hezuo polymetallic belt, located at the western margin of the West Qinling Orogenic Belt, contains the region’s largest polymetallic mineral resources. Deposits here are chiefly classified as either orogenic or magmatic–hydrothermal. Orogenic gold deposits, such as Zaozigou (106 t), Yidinan (34 t), Nanban (2.6 t), and Wanken (4 t), are typically hosted in Triassic metasedimentary successions and Early–Middle Triassic granitoids and are controlled by secondary regional fault sets [7,76]. Host-rock alteration is dominated by intense silicification, sericitization, pyritization, arsenopyritization, and carbonatization. Orebodies exhibit disseminated and vein-hosted textures, with pyrite, arsenopyrite, stibnite, and sphalerite as the principal sulfides [19,21,76,77]. Hydrothermal minerals dating of these orogenic systems yields mineralization ages of 235–210 Ma (Figure 9). By contrast, magmatic–hydrothermal deposits, for example, the Xiekeng–Jiangligou–Shuangpengxi Cu–Au–Fe–Mo skarn deposit, the Laodou intrusion-related gold deposit, Gangcha gold deposit and the Dewulu Au–Cu skarns deposits, are hosted entirely within granitoid intrusions and formed synchronously with magmatism [19,22,68,69,74,78,79]. Both the quartz diorite host and the gold mineralization date of the Laodou deposit, to ~249 Ma [22]. Likewise, the Dewulu intrusion and its surrounding skarn-hosted Au–Cu deposits formed at ca. 239 Ma [15,75]. These systems feature mineral assemblages of magnetite–siderite, pyrite, chalcopyrite, bornite, magnetite, chalcocite, arsenopyrite, and native gold, with supergene goethite, azurite, and malachite. Host-rock alteration displays potassic alteration, chloritization, silicification, sericitization, and carbonatization [68,74].
The Changshitougounao gold deposit differs markedly from magmatic–hydrothermal deposits (Supplementary Table S4). Mineralization is concentrated at the contact between quartz diorite and Triassic slate. Alteration is dominated by intense pyritization, arsenopyritization, silicification, sericitization, and carbonatization. Ore minerals include pyrite, arsenopyrite, apatite, and monazite, with minor stibnite. The orebodies display strong structural control by shear zones and lack alteration characteristics typical of magmatic–hydrothermal deposits. Hydrothermal monazite and apatite yield in situ LA–ICP–MS U–Pb ages that are ~10 Ma younger than the host quartz diorite emplacement, indicating that gold mineralization is not directly linked to magmatic intrusion. These characteristics, such as alteration assemblage, mineralogy, structural control, and timing, align with the orogenic gold model of Goldfarb et al. [5]. Previous geochemical and U–Pb zircon data indicate three major Indosinian plutonic pulses in the West Qinling Orogen at ca. 250–235 Ma, 228–215 Ma, and 215–185 Ma, corresponding to subduction-related magmatism, syn-collision granite emplacement, and post-collision magmatic activity, respectively [17,35,40,60]. By coupling these regional emplacement phases with the ~230 Ma mineralization age at Changshitougounao, we interpret the Changshitougounao gold deposit as having formed during collisional orogenesis associated with closure of the Paleo-Tethys Ocean. The deposit is best classified as an orogenic gold system. Pyritization, arsenopyritization, and sericitization are key hydrothermal alteration vectors for exploration. The most favorable mineralization site is the contact between granitoid intrusions and Triassic slate.

7. Conclusions

(1)
Zircon U–Pb ages from fresh quartz diorite and coeval Type I magmatic monazite, constrain the emplacement of the ore-hosting intrusion to ca. 240 Ma. In contrast, hydrothermal apatite and Type II monazite yield U–Pb ages of ca. 230 Ma, indicating gold mineralization occurred 10 Ma after intrusion and suggesting a limited genetic link between magmatism and mineralization.
(2)
Mineralization is structurally controlled by secondary regional faults at the contact between the quartz diorite and Triassic slate. Hydrothermal alteration is dominated by silicification, pyritization, arsenopyritization, and sericitization. These alteration assemblages, combined with shear-zone control, distinguish the Changshitougounao gold deposit from nearby magmatic–hydrothermal systems and align it with classical orogenic gold deposits.
(3)
The Changshitougounao gold deposit formed during collisional orogenesis, associated with closure of the Paleo-Tethys Ocean. Sericitization, pyritization, and arsenopyritization are identified as key exploration vectors. The contact between Early–Middle Triassic granitoids and underlying slate represents the most prospective horizon.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/min15090903/s1, Table S1. LA-ICP-MS zircon U-Pb age of the Changshitougounao gold deposit (24CSTGN01); Table S2. In-situ LA-ICP-MS U-Pb data of two types (magmatic and hydrothermal) monazite grains (24CSTGN01 and 24CSTGN02); Table S3. LA-ICP-MS U-Pb apatite data for mineralized quartz diorite (24CSTGN02 and 24CSTGN03); Table S4. Comparison of typical Orogenic and Magmatic Deposits in the Western Qinling.

Author Contributions

Conceived the ideas, X.-F.X., J.W. and S.-X.L.; map compilation, J.-H.Q. and S.-X.W.; data curation, formal analysis, and investigation, X.-F.X., J.-H.Q., Z.-W.Z. and D.-H.Y.; writing—original draft, X.-F.X. and S.-X.L. All authors have read and agreed to the published version of the manuscript.

Funding

This study was financially supported by the National Natural Science Foundation of China (42303067), the Shandong Gold Group Collaborative Research Grant (23B1014), projects of Ministry of Natural Resources, a new round of Mineral Exploration Breakthrough Strategic Action Science and Technology Support Project (ZKKJ202410), and the Frontiers Science Center for Deep-time Digital Earth (2652023001), and the Fundamental Research Funds for the Central Universities, China (2-9-2024-008).

Data Availability Statement

The data set is presented directly in the present study.

Acknowledgments

We are grateful to Hao-Cheng Yu for their field guidance and constructive discussions. We are grateful to Jia-Hui Zhou for the assistance with the figures. We also deeply thank the anonymous reviewers and editors for their helpful comments and suggestions.

Conflicts of Interest

Authors Sheng-Xiang Lu and Shou-Xu Wang was employed by the Shandong Gold Geology and Mineral Exploration Co., Ltd. Author Zheng-Wang Zeng was employed by the Northwest Gold Co., Ltd. The remaining authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

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Figure 1. Simplified geological map of the West Qinling Orogenic Belt (A) and simplified geological map and mineral deposit distribution of the Xiahe–Hezuo district (B) (modified after [21]).
Figure 1. Simplified geological map of the West Qinling Orogenic Belt (A) and simplified geological map and mineral deposit distribution of the Xiahe–Hezuo district (B) (modified after [21]).
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Figure 2. Simplified geological map of the Changshitougounao gold deposit (A) and schematic cross-section along exploration profile A–A′ (B).
Figure 2. Simplified geological map of the Changshitougounao gold deposit (A) and schematic cross-section along exploration profile A–A′ (B).
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Figure 3. Hand specimen of quartz diorite (A) and photomicrographs showing petrographic features (B–D). Pl = plagioclase, Qz = quartz, Bt = biotite, and Hbl = hornblende.
Figure 3. Hand specimen of quartz diorite (A) and photomicrographs showing petrographic features (B–D). Pl = plagioclase, Qz = quartz, Bt = biotite, and Hbl = hornblende.
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Figure 4. Hand specimens and petrographic characteristics of mineralized quartz diorite. Hand specimens showing silicification, sulfidation, and sericitization (A,B); photomicrographs exhibiting sericitization and carbonatization (C,D); and pyrite–arsenopyrite–stibnite assemblage (E,F). Ser = sericite, Cal = calcite, Py = pyrite, Apy = arsenopyrite, and Stb = stibnite.
Figure 4. Hand specimens and petrographic characteristics of mineralized quartz diorite. Hand specimens showing silicification, sulfidation, and sericitization (A,B); photomicrographs exhibiting sericitization and carbonatization (C,D); and pyrite–arsenopyrite–stibnite assemblage (E,F). Ser = sericite, Cal = calcite, Py = pyrite, Apy = arsenopyrite, and Stb = stibnite.
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Figure 5. Photomicrographs showing the texture and mode of occurrence of type I (A,B) and type II (C–F) monazite, and apatite grains (G,H). The yellow circles highlight biotite grain boundaries. Mon = monazite), Ap = apatite.
Figure 5. Photomicrographs showing the texture and mode of occurrence of type I (A,B) and type II (C–F) monazite, and apatite grains (G,H). The yellow circles highlight biotite grain boundaries. Mon = monazite), Ap = apatite.
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Figure 6. Representative zircon cathodoluminescence images (A) and zircon LA–ICP–MS U–Pb concordia diagrams of fresh quartz diorite (B,C).
Figure 6. Representative zircon cathodoluminescence images (A) and zircon LA–ICP–MS U–Pb concordia diagrams of fresh quartz diorite (B,C).
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Figure 7. In situ LA–ICP–MS U–Pb Tera–Wasserburg concordia diagrams of type I (A) and type II (B) monazite grains.
Figure 7. In situ LA–ICP–MS U–Pb Tera–Wasserburg concordia diagrams of type I (A) and type II (B) monazite grains.
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Figure 8. LA–ICP–MS U–Pb Tera–Wasserburg concordia diagrams of apatite grains. Representative cathodoluminescence images with identified analytical spot and U–Pb age (Ma) value are also shown (A,B). Representative cathodoluminescence images of apatite grains with identified analytical spot are also shown. Red box circle: U-Pb beam.
Figure 8. LA–ICP–MS U–Pb Tera–Wasserburg concordia diagrams of apatite grains. Representative cathodoluminescence images with identified analytical spot and U–Pb age (Ma) value are also shown (A,B). Representative cathodoluminescence images of apatite grains with identified analytical spot are also shown. Red box circle: U-Pb beam.
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Figure 9. Magmatic activity and mineralization ages in the Xiahe–Hezuo district. Previous data are from [11,13,14,15,19,21,22,41,42,65,67,68,69,70,71,72,73].
Figure 9. Magmatic activity and mineralization ages in the Xiahe–Hezuo district. Previous data are from [11,13,14,15,19,21,22,41,42,65,67,68,69,70,71,72,73].
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Xue, X.-F.; Lu, S.-X.; Wang, S.-X.; Yuan, D.-H.; Zeng, Z.-W.; Qiu, J.-H.; Wang, J. Geochronological Constraints on the Genesis of the Changshitougounao Gold Deposit, Qinling Orogen. Minerals 2025, 15, 903. https://doi.org/10.3390/min15090903

AMA Style

Xue X-F, Lu S-X, Wang S-X, Yuan D-H, Zeng Z-W, Qiu J-H, Wang J. Geochronological Constraints on the Genesis of the Changshitougounao Gold Deposit, Qinling Orogen. Minerals. 2025; 15(9):903. https://doi.org/10.3390/min15090903

Chicago/Turabian Style

Xue, Xian-Fa, Sheng-Xiang Lu, Shou-Xu Wang, Da-Hu Yuan, Zheng-Wang Zeng, Jin-Hong Qiu, and Jie Wang. 2025. "Geochronological Constraints on the Genesis of the Changshitougounao Gold Deposit, Qinling Orogen" Minerals 15, no. 9: 903. https://doi.org/10.3390/min15090903

APA Style

Xue, X.-F., Lu, S.-X., Wang, S.-X., Yuan, D.-H., Zeng, Z.-W., Qiu, J.-H., & Wang, J. (2025). Geochronological Constraints on the Genesis of the Changshitougounao Gold Deposit, Qinling Orogen. Minerals, 15(9), 903. https://doi.org/10.3390/min15090903

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