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Article

Molybdenite Re-Os Isotopic Ages of Two Late Mesozoic Giant Mo Deposits in the Eastern Qinling Orogenic Belt, Central China

by
Yuanshuo Zhang
1,2,3,
Li Yang
4,
Herong Gui
2,*,
Dejin Wang
1,
Mengqiu He
1 and
Jun He
3,*
1
School of Resources and Environment, Anqing Normal University, Anqing 246011, China
2
School of Resources and Civil Engineering, Suzhou University, Suzhou 234000, China
3
School of Earth and Space Sciences, University of Science and Technology, Hefei 230026, China
4
Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China
*
Authors to whom correspondence should be addressed.
Minerals 2025, 15(8), 800; https://doi.org/10.3390/min15080800
Submission received: 14 June 2025 / Revised: 27 July 2025 / Accepted: 27 July 2025 / Published: 30 July 2025
(This article belongs to the Section Mineral Deposits)
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Abstract

Precise Re-Os isotopic ages of the Jinduicheng and Donggou Mo deposits in the East Qinling orogenic belt can shed light on the controversies about multiple-stage pulses of mineralization and further elucidate the genesis and metallogenic process of the deposits. In this study, we propose two major events of Mo mineralization in this orogenic belt occurring during the Late Mesozoic: the early stage of 156–130 Ma and late stage of 122–114 Ma. Results of molybdenite Re-Os isotopic analysis reveal that the Jinduicheng deposit formed at 139.2 ± 2.9 Ma, while the Donggou deposit exhibited two-stage mineralization at 115.4 ± 1.6 Ma and 111.9 ± 1.3 Ma. These isotopic ages align with the spatiotemporal evolution of coeval ore-barren granites exposed in eastern Qinling, pointing to a close genetic relationship between the magmatism and mineralization that was controlled by the same tectonic activity, likely in a post-collisional setting. This highlights the multiple-stage Mo mineralization and provides evidence for further understanding the geodynamics and metallogenic process in the eastern Qinling orogenic belt.

1. Introduction

More than 95% of molybdenum reserves and production in the world are related porphyry deposits, ranging from porphyry Cu (Mo ± Au) deposits to pure porphyry Mo deposits. The origin of high ore grades and tectonic settings of the deposits have long been debated. Recognized tectonic settings mainly include rift-related ones associated with highly evolved rhyolite magmas and arc-related (or subduction-related) ones linked to calc-alkaline magmas [1,2]. Some researchers suggest that arc-related mineralization belts with thickened crusts, such as the Colorado metallogenic belt, experienced multiple pulses of Mo mineralization and large-scale Mo anomalies [1]. Nevertheless, recent studies highlight that syn- to post-collisional environments are also significant for porphyry deposits. For instance, the Gangdise porphyry copper deposit is related to a post-collisional setting [3], while the East Qinling orogenic belt (EQOB) hosts molybdenum deposits in a post-orogenic extensional environment [4]. The sources of molybdenum also remain controversial: one interpretation favors from the lower crust or the ancient continental lithospheric mantle [1,5]; another proposes a two-stage enrichment process involving surface weathering and sedimentation followed by magma processes related to plate subduction or melting of the deep burial crust [6].
The Qinling–Dabie orogenic belt hosts the world’s most important molybdenum ore belt. Over 92% of the molybdenum reserves are associated with porphyry, and porphyry–skarn deposits are related to Late Mesozoic granite plutons, especially the EQOB, being the most significant Mo repository. Previous studies [7] proposed two episodes of Mo mineralization in the EQOB in the Early Mesozoic (~230–220 Ma) and Late Mesozoic (~160–110 Ma). Molybdenite Re-Os dating further reveals two stages of Mo mineralization in Late Mesozoic and ore-bearing granite porphyries of ~148–138 Ma and ~130–112 Ma, consistent with the spatiotemporal evolution of ore-barren granites emplaced at ~158–130 Ma and ~120–100 Ma in the EQOB [8]. A close genetic relationship between the Mo deposits and coeval ore-barren granites has been recognized on the basis of these observations. Although extensive studies on the Mo deposits in the Qinling–Dabie orogenic belt have been performed, controversies concerning pulses and ages of mineralization still remain and hinder our understanding on the genesis of the world-class Mo ore cluster in the EQOB [9]. Therefore, more chronological data of Mo mineralization are crucial to genetic links between the granitic magmatism and porphyry mineralization. In this study, we focus on two giant Mo deposits (Jinduicheng and Donggou) in the EQOB to further constrain mineralization ages and improve understanding of the genesis and process of Mo mineralization.

2. Geological Background and Petrography

The Qinling orogenic belt, suturing the North and South China cratons and extending several thousand kilometers east–westwards in Central China, links the Dabie orogen in the east and the Kunlun orogen in the west. This orogenic belt exhibits multiple-stage tectonic evolution between the Neoproterozoic and the Mesozoic. It contains four tectonic units, i.e., from north to south, the southern margin of the North China Craton, North Qinling, South Qinling, and the northern margin of South China [7,10]. The southern margin of the North China Craton consists of Archean to Paleoproterozoic crystalline basement (e.g., ~2.5 Ga Taihua Group), Paleoproterozoic volcanic rocks (e.g., ~1.80 Ga Xiong’er Group), and Neoproterozoic to Phanerozoic sedimentary rocks. The Taihua Group is dominated by tonalite–trondhjemite–granodiorite gneiss, graphite-bearing gneiss, amphibolite, marble, quartzite, and banded iron-formation and underwent greenschist- to upper-granulite-facies metamorphism [10,11]. The Xiong’er Group comprises andesite and basaltic andesite with minor dacite and rhyolite and unconformably overlies the Taihua Group [11,12].
In the Qinling orogenic belt, magmatic stages in the Neoproterozoic, Paleozoic, Early Mesozoic, and Late Mesozoic periods accompanied the tectonic evolution. Late Mesozoic granitoid rocks were widely distributed in this orogenic belt, especially within the southern margin of the North China Craton. Two major magmatic stages of 158–130 Ma and 120–100 Ma can be recognized from these granitoid rocks [8]. They are composed mainly of granite, monzogranite, granodiorite, and granite porphyries. These granitoid rocks are the most important in the Qinling orogenic belt metal mineralization in Central China [13,14]. Many Mo or Mo-W polymetallic deposits are closely related to granite, such as the Jinduicheng, Nannihu, Shangfanggou, and Donggou deposits. Occasionally, vein-type Zn-Pb-Cu-Ag-Au deposit surrounding the porphyry Mo deposit forms well-defined ore clusters, for instance, the Sanyuangou Pb-Zn-Ag vein-type deposit near the Donggou porphyry Mo deposit [9].
The Jinduicheng Mo deposit is located at the western part of the Mo-(Au-Ag) polymetallic mineralization belt in the EQOB (Figure 1b) and has a proven reserve of almost one million tons of molybdenum metal [15]. The exposed rock units in the Jinduicheng ore district are mainly composed of gneisses of the Taihua Group, volcanic rocks of the Xiong’er Group, and clastic and carbonate rocks of the Mesoproterozoic Guandaokou Group. Nearly vertical faults with the WNW and NNE directions developed in the mining area. The intersection of these faults controls the distribution of granite porphyry and Mo deposits (Figure 2a; Figure 3a,b). Magmatic rocks are widely exposed, and different mineralization types can be observed in the ore district, including porphyry Mo deposit (e.g., the Jinduicheng, Balipo, and Shijiawan deposits) and carbonate-vein Mo deposit (e.g., the Huanglongpu deposit). The Late Mesozoic Laoniushan granite is exposed as massif pluton in the northwest of the ore district, while many granite porphyries form bodies, which are closely to Mo mineralization (e.g., Jinduicheng, Shijiawan, and Balipo deposits). The Jinduicheng granite porphyry with an area of ~0.07 km2 extends in the northwestward direction to Mo mineralization and crosses into the Xiong’er Group region. The porphyry rocks are light red to brick red in color with obvious spotted structures. The phenocrysts are mainly quartz and potassium feldspar with a particle size of 3–5 mm, while particles in the matrix are 0.1–0.5 mm in size and composed of potassium feldspar (20–40 vol.%), quartz (25–35 vol.%), plagioclase (5–15 vol.%), sericite (5–10 vol.%), and minor biotite. The accessory minerals include magnetite, apatite, zircon, pyrite, and hematite (Figure 3c–f).
The Jinduicheng Mo ores within the rock mass of the granite porphyry and in the contact zones. The surface length of the ore body is ~1600 m and extends in the NW-NE direction. It displays porphyritic, scaly, and radial structures and is composed mainly of porphyry-type (ca. 25%) and andesite-type (ca. 70%) ores with minor quartzite-type Mo ores [7]. The ore minerals are mainly molybdenite and pyrite with small amounts of chalcopyrite, magnetite, sphalerite, and galena. The vein minerals are quartz, potassium feldspar, plagioclase, biotite, and sericite, with secondary fluorite, chlorite, and calcite (Figure 3b–d). The surrounding rocks of the deposit are mainly composed of silicified and propylitized basaltic andesite and exhibit typical features of the porphyry Mo ores. They underwent regular alteration from the porphyry body to the surrounding rocks, namely, potassium alteration, sericite alteration, silicification, propylitic alteration, and carbonate alteration [20].
The Donggou Mo deposit at the eastern part of the EQOB (Figure 1b) has a proven reserve of several hundred thousand tons of molybdenum metal [17]. This Mo deposit located in the center of the ore district and its periphery contain many Pb-Zn deposits, for instance, the Sanyuangou and Laodaizhanggou deposits. The exposed rocks in the Donggou ore district are volcanic rocks of the Xiong’er Group. Fault structures in the NE and NWW-EW directions are widely developed, and the NE trending faults control the distribution of mineralized rocks and Mo deposits in the ore district [20]. Late Mesozoic granite plutons are exposed widely in this region, such as the Taishanmiao granite and the Donggou granite porphyry. The Taishanmiao granite, located in southwest of the Donggou deposit, consists of medium- to coarse-grained syenogranite and porphyritic syenogranite [4,13,21]. The Donggou Mo ores are mainly located on the inner and outer contact zones of the granite porphyry. The Donggou granite porphyry, with an exposure area of ~0.01 km2, is brick red in color with spotted structures. It contains phenocrysts composed mainly of quartz, plagioclase, and feldspar. Quartz phenocrysts show the development of erosion structures. The matrix in a fine-grained structure is mainly composed of quartz, potassium feldspar, plagioclase, and minor biotite. The accessory minerals include molybdenite, magnetite, hematite, and zircon (Figure 4).
In the Donggou ore deposit, the ore occurs mainly as scaly veins, disseminations, and fine veinlets. The metal minerals are mainly molybdenite and minor pyrite, chalcopyrite, and minerals quartz, potassium feldspar, and plagioclase, with secondary biotite, chlorite, epidote, sericite, and fluorite. Hydrothermal alteration occurred in the Donggou ore deposit, and the types are silicification, potassic alteration, and biotization, followed by sericitization, chloritization, and carbonation (Figure 4). Silicification and potassic alteration are manifested in two forms: fine vein infiltration and intergranular metasomatism, both closely related to Mo mineralization. On the basis of field and petrographic observations, four stages can be recognized in the deposit, i.e., Stage I: quartz–K-feldspar, with very little Mo ore; Stage II: molybdenite vein-K-feldspar–quartz, the first and main Mo mineralization; Stage III: molybdenite veins–quartz, the second Mo mineralization; and Stage IV: quartz–carbonate-fluorite, without Mo ore.

3. Analytical Technique and Results

Molybdenite grains of the ore samples were separated in the Keda Rock Mineral Sorting Technology Service Co., Ltd., in Langfang City, Hebei Province. The grains were examined under a microscope, and only the pure ones without any oxidation or contamination of other minerals were chosen for analytical purposes. Molybdenite Re-Os isotopic analysis was performed at the Re-Os Isotope Chronology Laboratory of the National Geological Experiment Center in Beijing. A TJA X-series ICP-MS (inductively coupled plasma mass spectrometer) produced by the TJA Company was used for isotopic measurement. Uncertainties in Re and Os contents derived from the errors of sample and diluent weighing, calibration of diluents, correction of mass fractionation in isotopic measurements, and precision of measured isotopic ratios, with a 95% confidence level. The uncertainty of model ages includes the uncertainty of the decay constant (1.02%) with a confidence level of 95%. Details for the analytical procedures for the Re-Os isotopic technique used in this study are available elsewhere [22,23]. Fourteen molybdenite samples were collected from the Jinduicheng and Donggou deposits for the Re-Os isotopic analysis in this study. The analytical results for the Re-Os isotopic composition are given in Table 1.
Jinduicheng deposit: Three molybdenite samples from granite porphyry rocks (samples JDC151-2, JDC151-4, and JDC151-6) and four from andesite rocks (samples JDC150-1, JDC150-2, JDC150-4, and JDC150-5) were analyzed. The analytical results show that Re contents of molybdenite samples range from 20 ppm to 59 ppm. A positive correlation between Re and 187Os contents can be seen, and the contribution of initial 187Os is negligible in all the samples. When using the 187Re decay constant (λ) of 1.666 × 10−11/a [23], an isochron age of 139.2 ± 2.9 Ma (MSWD value of 1.2) can be obtained when using the ISOPLOT 4.15 software (Figure 5) [24]. Model ages of seven molybdenite samples range from 141 Ma to 137 Ma, giving a weighted average value of 139.2 ± 0.8 Ma with a MSWD value 0.79 (Figure 5).
Donggou deposit: One molybdenite sample from granite porphyry rock (sample DG0907) and six (samples DG0904, RY0710, RY0711-a, RY0712-a-1, RY0712-a-2, and RY0712-b) from andesite rocks were collected for the analysis. According to field observation of ore veins, two samples (RY0711-a, RY0712-b) derived from the veins of the late stage and the other five from veins of the early stage. All the molybdenite samples have relatively low Re contents from 3.07 ppm to 9.79 ppm. The analytical results show that the five molybdenite samples from the early-stage veins yield Re-Os model ages ranging from 114.6 ± 1.6 Ma to 115.9 ± 1.6 Ma with a weighted average value of 115.1 ± 0.7 Ma. When the ISOPLOT 4.15 software is used, these samples yield a Re-Os isochron age of 115.4 ± 1.6 Ma (MSWD value of 0.85; Figure 6). An initial 187Os/188Os value of −0.01 ± 0.07 obtained from the isochron indicates negligible common (or initial) osmium during the crystallization of molybdenite. The two samples from the late-stage veins give younger Re-Os model ages of 111.7 ± 1.7 Ma and 112.2 ± 1.7 Ma, respectively, and an average value of 111.9 ± 1.3 Ma (Figure 6).

4. Discussion

4.1. Mo Mineralization Stages

The Re-Os isotopic system of molybdenite is remarkably robust and can remain stable even in high-grade and contact metamorphic processes owing to its high closure temperature [25,26]. Therefore, the molybdenite Re-Os isotopic system can usually provide reliable dating results and has commonly been employed to study mineralization. In this study, molybdenite samples from the Jinduicheng and Donggou Mo deposits exhibited high-precision Re-Os isotopic ages of 139.2 ± 2.9 Ma and 115.4 ± 1.6 Ma, respectively. Molybdenite Re-Os model ages of the Donggou deposit indicate two stages of Mo mineralization at ~115 Ma and ~112 Ma.
K-Ar and Rb-Sr isotopic ages of 132 Ma to 124 Ma were reported for the Jinduicheng Mo deposit in previous studies [20] and references therein. Nevertheless, the K-Ar and Rb-Sr isotopic systems are susceptible to late hydrothermal activities, resulting in high uncertainty of dating. Two pulses of Mo mineralization of 141–138 Ma and 129 Ma were recognized on the basis of molybdenite Re-Os isotopic ages of the Jinduicheng deposit [27,28], but the young age (129 ± 7 Ma) is of significant uncertainty. In combination with molybdenite Re-Os isotopic ages of ~139 Ma obtained in this study, we propose that the Jinduicheng deposit formed at ca. 140 Ma during early Cretaceous [27,28].
Several Re-Os isotopic ages have been obtained for the Donggou Mo deposit, for instance, from 116.5 ± 1.7 Ma to 115.5 ± 1.7 Ma [29] and from 115.1 ± 2.0 Ma to 114.1 ± 1.4 Ma [17]. Four genetic stages were previously recognized by the authors of [9], who noted that molybdenite ores are concentrated in the first two stages, whereas later stages are essentially barren. On the basis of petrological observations and isotope dating, combined with the data presented herein, we distinguish five mineralization stages: Stage I: quartz–K-feldspar, with very little Mo ore; Stage II: molybdenite vein-K-feldspar–quartz, the first and main Mo mineralization; Stage III: molybdenite veins–quartz, the second Mo mineralization; Stage IV: quartz–polymetallic sulfide veins; and Stage Ⅴ: quartz–calcite veins. Previous Re–Os dating yielded 117.5 ± 0.8 Ma for Stage III quartz–molybdenite veins and 116.4 ± 0.6 Ma for Stage IV quartz–polymetallic sulfide veins [9]. In this study, molybdenite from Stage II gives ~115 Ma, whereas Stage III veins yield ~112 Ma. Collectively, these ages indicate that the Donggou porphyry Mo deposit formed mainly between 118 Ma and 112 Ma.

4.2. Implications for the Mineralization and Geodynamics

Previous molybdenite Re-Os isotopic dating studies have revealed three stages of Mo mineralization in the Qinling orogenic belt, namely, 233–220 Ma, 148–138 Ma, and 130–110 Ma [7]. The different mineralization types mainly include porphyry, porphyry–skarn, and hydrothermal vein ores. The Early Mesozoic mineralization of ~233–220 Ma, mainly hydrothermal veins, is represented by quartz–vein Mo deposits, e.g., the Qianfanling deposit [30] and carbonatite vein Mo deposits, e.g., the Xigou, Huanglongpu, and Dahu deposits [27,31,32,33]. The Late Mesozoic Mo mineralization of 148–110 Ma mainly comprises porphyry and porphyry–skarn deposits, e.g., the Jinduicheng, Nannihu, and Donggou deposits [9,17,28]. As shown in the age histograms (Figure 7a–g), the Late Mesozoic molybdenite deposits in the EQOB are mainly distributed in the northern margin of the North Qinling terrane and the southern margin of the North China Craton (Figure 1b). The Re-Os isotope ages of molybdenite in Leimengou, Nannihu, Donggou, Jinduicheng (the southern margin of the North China Craton), Qiushuwan, Nantai, and Yuchiling (the North Qinling terrane) ore district are consistent with the zircon U-Pb ages of granitic magmatic activities (granitic magmatism and porphyry mineralization) within the error range (Figure 7a–g). In addition, the Re-Os isotopic ages reported in the previous studies are distributed in two groups of 156–130 Ma and 122–114 Ma with two age peaks at 147.5 Ma and 117.5 Ma, indicating two Mo mineralization events during the Late Mesozoic (Figure 7h). The Re-Os dating results suggest that the Jinduicheng and Donggou deposits belong to the first and second Mo mineralization stages, respectively. These two mineralization events are temporally consistent with the ore-barren granite plutons and ore-bearing granite porphyries in the EQOB, which formed in 158–130 Ma and 120–100 Ma [4,8,13]. This implies that simultaneous mineralization and magmatism might be controlled by the same tectonic activity.
The genesis of the Late Mesozoic porphyry Mo deposits in the EQOB has been debated in recent decades. The genetic relationship between the Late Mesozoic magmatism (represented by granite porphyry and ore-barren granite batholith) and mineralization is crucial to the source and mechanism of the Mo deposits. Geochemical characteristics of the granites point to an origin from a mixture of the ancient basement rocks and the juvenile crust or mantle material [16,34]. Two main opinions can be summarized from previous studies: one holds that there is a genetic link among the barren granite batholith, granite porphyry, and Mo deposits [2,13,33,35,36]; the other holds that magmatism and ore-forming processes were produced by two independent geological systems [37]. Many researchers proposed that the granite porphyry belongs to a highly evolved part of the granite batholith, and Mo mineralization might have occurred through the differentiation of the magma and fluid–magma interaction in the late magmatic stage [2,33,35,36]. However, it is also argued that the Donggou porphyry deposit is a product of rapid localization and consolidation of a high-temperature magma, while the adjacent batholith (Taishanmiao granite) resulted from a low-temperature magma [37]. The small-volume magma of the Donggou porphyry could not provide sufficient ore-forming material to form a super-large deposit and similar characteristics in geochemistry between the Donggou porphyry, and the Taishanmiao granite can be rooted from a similar magma source [37].
According to tectonic setting and characteristics of mineralization and related granite, porphyry Mo deposits are generally divided into three major types, i.e., the back-arc rift-related type, forming in the back-arc extension stage induced by oceanic plate subduction and related to highly evolved rhyolite-alkaline magma [1,2,38]; continental arc-related type, forming in the background of a continental margin arc and related to calc-alkaline magma [1,39]; and collisional orogen type, developing in syn- to post-collisional settings [38]. It has been proposed that the Qinling orogenic belt entered a post-collisional setting during the Late Mesozoic; therefore, the Mo deposits belong to the collisional type. The collision-type Mo deposits in the EQOB, whose ore-forming magmas were derived mainly from the lower–middle continental crust and produced CO2-rich fluids, which host distinctive CO2–daughter-mineral-bearing fluid inclusions, potassic–carbonate–fluorite-dominated alteration, and only weak phyllic and propylitic overprints, differ markedly from continental-arc and back-arc rift-type Mo deposits [38].
Minerals 15 00800 g007
Figure 7. Ages of the Late Mesozoic granite plutons, granite porphyries, and Mo deposits in the EQOB (a–g) and histogram of Re-Os isotopic ages for the Late Mesozoic Mo deposits in the EQOB (h). Data sources: [9,15,17,18,28,29,31,32,33,40,41,42,43,44] and this study. The dashed line separates Mo deposit, granite porphyry, and granite batholith.
Figure 7. Ages of the Late Mesozoic granite plutons, granite porphyries, and Mo deposits in the EQOB (a–g) and histogram of Re-Os isotopic ages for the Late Mesozoic Mo deposits in the EQOB (h). Data sources: [9,15,17,18,28,29,31,32,33,40,41,42,43,44] and this study. The dashed line separates Mo deposit, granite porphyry, and granite batholith.
Minerals 15 00800 g007
The North Qinling terrane mainly developed Late Jurassic Mo deposits (~150–145 Ma; Figure 7e–g), while two stages of Mo mineralization can be recognized along the southern margin of the North China Craton (Figure 7a–d). For instance, the Yechangping porphyry Mo deposit in the Donggou ore district formed at ~145 Ma (Re-Os isotopic age), representing the early mineralization stage [42], and the Zhuyuangou and Donggou deposits formed at ~120–110 Ma, belonging to the products of the late stage (Figure 7c) [9,45], this paper. As shown in the age histograms (Figure 7h), the Late Mesozoic Mo deposits in the EQOB can be subdivided into two mineralization pulses, namely, the early one of ~156–130 Ma and the late one of ~120–110 Ma. Previous studies have shown that the EQOB underwent a tectonic regime transition from post-collisional compression to extension during the Late Mesozoic, with ca. 130 Ma being the tectonic transition period [46,47,48]. The crust in the orogenic belt was thicker than 40 km, and partial melting took place in the garnet stable zone prior to ~130 Ma, and subsequently the crustal thickness decreased to ca. 30 km. The evidence of molybdenite Re-Os isotopic dating also points to a transition of the mineralization occurring at ~130–122 Ma in the EQOB (Figure 7h) [49]. In summary, the magmatic activities that formed the Late Mesozoic granitoid rocks are temporally consistent with Mo mineralization, indicating a genetic connection between magmatism and mineralization, both of which formed in post-collision environments (Figure 7a–g).

5. Conclusions

The porphyry Mo deposits in the eastern Qinling orogenic belt record the multiple- pulse mineralization during the Late Mesozoic. Molybdenite Re-Os isotopic dating gives ~139 Ma for the Jinduicheng Mo deposit, indicating early mineralization in the Early Cretaceous. Two different molybdenite veins of the Donggou Mo deposit yield Re-Os isotopic ages of ~115 Ma and ~112 Ma, likely representing early (molybdenite-quartz–K-feldspar) and late (molybdenite-quartz) mineralization.
When summarizing molybdenite Re-Os isotopic ages previously reported in the literature, two major stages of the porphyry Mo mineralization at ~156–130 Ma and ~120–110 Ma can be discriminated in the eastern Qinling orogenic belt. These mineralization events are coeval and even spatially related to the ore-barren granites widespread in the orogenic belt, suggesting a genetic connection between mineralization and magmatism during the Late Mesozoic orogenic collapse.

Author Contributions

Conceptualization and writing—original draft preparation, Y.Z. and L.Y.; methodology and investigation, D.W. and M.H.; supervision and writing—review and editing, J.H. and Y.Z.; funding acquisition, H.G. All authors have read and agreed to the published version of the manuscript.

Funding

This study was financially supported by the Postdoctoral Research Startup Grant of Suzhou University (Anhui Provincial Coal Mine Exploration Engineering Technology Research Center), grant 2022BSH004.

Data Availability Statement

The authors confirm that the data supporting the findings of this study are available within the article.

Acknowledgments

We thank X.-Y. Zhu for assistance in the fieldwork.

Conflicts of Interest

The authors declare no conflicts of interest.

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Minerals 15 00800 g001
Figure 1. (a) Tectonic sketch of China; (b) geological sketch of the Qinling orogen: the North Qinling terrane and the southern margin of the North China Craton in the Qinling orogen (after [16,17,18,19]).
Figure 1. (a) Tectonic sketch of China; (b) geological sketch of the Qinling orogen: the North Qinling terrane and the southern margin of the North China Craton in the Qinling orogen (after [16,17,18,19]).
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Figure 2. Geological sketch of porphyry Mo deposit and Late Mesozoic granite in the (a) Jinduicheng and (b) Donggou deposits (after [7,17]).
Figure 2. Geological sketch of porphyry Mo deposit and Late Mesozoic granite in the (a) Jinduicheng and (b) Donggou deposits (after [7,17]).
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Figure 3. Photographs of ores from the Jinduicheng deposit: (a) field photograph of the Jinduicheng deposit; (b) ores in andesite; (c,d) ores in granitic porphyry showing relationship of multiple-stage veins; (e,f) microphotographs showing alteration of granitic porphyry. Mineral abbreviations: Kfs: K-feldspar; Mo: molybdenite; Py: pyrite; Qtz: quartz; Pl: plagioclase; Mus: Muscovite. Dashed lines represent later-stage cross-cutting veins.
Figure 3. Photographs of ores from the Jinduicheng deposit: (a) field photograph of the Jinduicheng deposit; (b) ores in andesite; (c,d) ores in granitic porphyry showing relationship of multiple-stage veins; (e,f) microphotographs showing alteration of granitic porphyry. Mineral abbreviations: Kfs: K-feldspar; Mo: molybdenite; Py: pyrite; Qtz: quartz; Pl: plagioclase; Mus: Muscovite. Dashed lines represent later-stage cross-cutting veins.
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Figure 4. Different types of molybdenite occurrences in the Donggou Mo deposit: (a) early-stage ore-barren quartz vein, crosscut by later pyrite vein; (b) porphyry-type quartz–molybdenite vein within porphyry (molybdenite in scaly form); (c) quartz–molybdenite vein within andesite (molybdenite in massive form); (d) quartz–K-feldspar–molybdenite vein in andesite (molybdenite in massive form); (e) quartz–molybdenite vein within andesite (molybdenite distributing along vein wall, crosscutting early ore-barren quartz vein); (f) first-stage coarse scaly molybdenite veins (RY0712a-1), crosscut by second-stage thin film-like molybdenite along vein wall (RY0712b). Mineral abbreviations and dashed lines are as in Figure 3.
Figure 4. Different types of molybdenite occurrences in the Donggou Mo deposit: (a) early-stage ore-barren quartz vein, crosscut by later pyrite vein; (b) porphyry-type quartz–molybdenite vein within porphyry (molybdenite in scaly form); (c) quartz–molybdenite vein within andesite (molybdenite in massive form); (d) quartz–K-feldspar–molybdenite vein in andesite (molybdenite in massive form); (e) quartz–molybdenite vein within andesite (molybdenite distributing along vein wall, crosscutting early ore-barren quartz vein); (f) first-stage coarse scaly molybdenite veins (RY0712a-1), crosscut by second-stage thin film-like molybdenite along vein wall (RY0712b). Mineral abbreviations and dashed lines are as in Figure 3.
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Figure 5. Molybdenite Re-Os isochron age (a) and Os model age (b) of the Jinduicheng Mo deposit.
Figure 5. Molybdenite Re-Os isochron age (a) and Os model age (b) of the Jinduicheng Mo deposit.
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Figure 6. Molybdenite Re-Os isochron age (a) and Os model age (b) of the Donggou Mo deposit. The solid line represents the isochron age of the early-stage veins, while the dashed line represents the late-stage veins.
Figure 6. Molybdenite Re-Os isochron age (a) and Os model age (b) of the Donggou Mo deposit. The solid line represents the isochron age of the early-stage veins, while the dashed line represents the late-stage veins.
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Table 1. Molybdenite Re-Os isotopic data of the Jinduicheng and Donggou porphyry Mo deposits.
Table 1. Molybdenite Re-Os isotopic data of the Jinduicheng and Donggou porphyry Mo deposits.
Sample No.Weight (mg)Re ± 2σ (ppm)187Re ± 2σ (ppm)187Os ± 2σ (ppb)Model Age ± 2σ (Ma)
Jinduicheng
JDC150-1100.858.97 ± 1.0837.06 ± 0.6886.43 ± 0.70139.8 ± 3.0
JDC150-2100.446.67 ± 0.7429.34 ± 0.4667.12 ± 0.55137.2 ± 2.7
JDC150-4100.229.25 ± 0.2918.38 ± 0.1843.11 ± 0.35140.6 ± 2.1
JDC150-5100.223.52 ± 0.1814.78 ± 0.1134.45 ± 0.31139.8 ± 2.0
JDC151-4100.820.29 ± 0.1512.75 ± 0.0929.52 ± 0.24138.8 ± 1.9
JDC151-250.0525.25 ± 0.2515.87 ± 0.1636.80 ± 0.31139.0 ± 2.2
JDC151-650.1822.60 ± 0.2114.21 ± 0.1332.91 ± 0.31138.9 ± 2.1
Donggou
RY0711-a100.59.79 ± 0.096.16 ± 0.0611.47 ± 0.10111.7 ± 1.7
RY0712-b112.23.11 ± 0.021.96 ± 0.013.66 ± 0.04112.2 ± 1.7
DG0904100.68.83 ± 0.085.55 ± 0.0510.66 ± 0.09115.3 ± 1.7
DG090785.606.79 ± 0.064.27 ± 0.048.16 ± 0.07114.6 ± 1.7
RY0710101.05.22 ± 0.043.28 ± 0.036.33 ± 0.05115.9 ± 1.6
RY0712-a-177.103.15 ± 0.031.98 ± 0.023.81 ± 0.03115.3 ± 1.6
RY0712-a-2202.63.07 ± 0.021.93 ± 0.023.69 ± 0.03114.6 ± 1.6
Model age (t) = 1/λ × ln(1 + 187Os/187Re), where λ(187Re) = 1.666 × 10−11 a−1 [23].
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Zhang, Y.; Yang, L.; Gui, H.; Wang, D.; He, M.; He, J. Molybdenite Re-Os Isotopic Ages of Two Late Mesozoic Giant Mo Deposits in the Eastern Qinling Orogenic Belt, Central China. Minerals 2025, 15, 800. https://doi.org/10.3390/min15080800

AMA Style

Zhang Y, Yang L, Gui H, Wang D, He M, He J. Molybdenite Re-Os Isotopic Ages of Two Late Mesozoic Giant Mo Deposits in the Eastern Qinling Orogenic Belt, Central China. Minerals. 2025; 15(8):800. https://doi.org/10.3390/min15080800

Chicago/Turabian Style

Zhang, Yuanshuo, Li Yang, Herong Gui, Dejin Wang, Mengqiu He, and Jun He. 2025. "Molybdenite Re-Os Isotopic Ages of Two Late Mesozoic Giant Mo Deposits in the Eastern Qinling Orogenic Belt, Central China" Minerals 15, no. 8: 800. https://doi.org/10.3390/min15080800

APA Style

Zhang, Y., Yang, L., Gui, H., Wang, D., He, M., & He, J. (2025). Molybdenite Re-Os Isotopic Ages of Two Late Mesozoic Giant Mo Deposits in the Eastern Qinling Orogenic Belt, Central China. Minerals, 15(8), 800. https://doi.org/10.3390/min15080800

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