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Article

Metallogenic Age and Tectonic Setting of the Haigou Gold Deposit in Southeast Jilin Province, NE China: Constraints from Magmatic Chronology and Geochemistry

by
Zhongjie Yang
1,
Yuandong Zhao
1,*,
Cangjiang Zhang
1,*,
Chuantao Ren
1,
Qun Yang
2 and
Long Zhang
1
1
Mudanjiang Natural Resources Comprehensive Survey Center, China Geological Survey, Changchun 130000, China
2
College of Earth Sciences, Jilin University, Changchun 130061, China
*
Authors to whom correspondence should be addressed.
Minerals 2025, 15(6), 582; https://doi.org/10.3390/min15060582
Submission received: 2 April 2025 / Revised: 22 May 2025 / Accepted: 24 May 2025 / Published: 29 May 2025
(This article belongs to the Special Issue Genesis and Metallogeny of Non-ferrous and Precious Metal Deposits, 2nd Edition)
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Abstract

:
Haigou deposit, located in Dunhua City, southeast Jilin Province, NE China, is a large-scale gold deposit. The gold ore body is categorized into two types: quartz-vein type and altered rock type, with the quartz-vein type being predominant. The vein gold ore body primarily occurs within the monzonite granite and monzonite rock mass in the Haigou area and is controlled by fault structures trending northeast, northwest, and near north-south. In order to constrain the age and tectonic setting of quartz vein-type gold mineralization, we conducted a detailed underground investigation and collected samples of monzonite granite and pyroxene diorite porphyrite veins related to quartz-vein-type gold mineralization for LA-ICP-MS zircon U-Pb dating and whole-rock main trace element data testing to confirm that monzonite granite is closely related to gold mineralization. Pyroxene diorite porphyry and gold mineralization were found in parallel veins. The zircon U-Pb weighted mean ages of monzonite and pyroxene diorite porphyrite veins are 317.1 ± 3.5 Ma and 308.8 ± 3.0 Ma, respectively, indicating that gold mineralization in monzonite, pyroxene diorite porphyrite veins, and quartz veins occurred in the Late Carboniferous. The monzonite granite and pyroxene diorite porphyrite veins associated with quartz vein-type gold mineralization have high SiO2, high K, and high Al2O3 and are all metaluminous high-potassium calc-alkaline rock series. Both of them are relatively enriched in light rare earth elements (LREE) and macroionic lithophile elements (LILE: Rb, Ba, K, etc.), but deficient in heavy rare earth elements (HREE) and high field strength elements (HFSE: Nb, Ta, P, Ti, etc.), the monzonitic granite Eu is a weak positive anomaly (δEu = 1.15–1.46), the pyroxene diorite porphyre dyke Eu is a weak positive anomaly (δEu = 1.09–1.13), and the Nb and Ta are negative anomalies. The Th/Nb values are 0.28–0.73 and 1.48–2.05, and La/Nb are 2.61–4.74 and 4.59–5.43, respectively, suggesting that diagenetic mineralization is the product of subduction in an active continental margin environment. In recent years, scholarly research on Sr, Nd, and Pb isotopes in Haigou rock masses has indicated that the magmatic source region in the Haigou mining areas is complex. It is neither a singular crustal source nor a mantle source but rather a mixed crust-mantle source, primarily resulting from the partial melting of lower crustal materials, with additional contributions from mantle-derived materials. In summary, the metallogenic characteristics, chronology data, geochemical characteristics, and regional tectonic interpretation indicate that at least one phase of magmatic-hydrothermal gold mineralization was established in the Late Carboniferous as a result of the subduction of the Paleo-Asian ocean plate at the northern margin of the North China Craton.

1. Introduction

Southeast Jilin Province, NE China, located at the intersection of the eastern segments of the northern margin of the North China Craton and the southern margin of the Jiamusi massif (Figure 1A), contains the world-renowned Jiapiguo-Haigou gold metallogenic belt [1,2,3,4]. During the Archean Eon, this area was part of a granitoid-greenstone belt. Subsequently, from the late Paleozoic to the early Mesozoic, it was part of the Paleo-Asian Ocean and Paleo-Pacific tectonic domains. This resulted in intense tectonic-magmatic activity in the region, providing excellent conditions for gold mineralization. More than 20 large, medium, and small gold deposits have been discovered, including Haigou, Jiapigou, Songjianghe, Bajiazi, and Banmiaozi, among others (Figure 1B). Their formation in both space and time is related to the widespread Mesozoic intrusive bodies [5,6,7,8,9,10]. However, gold deposits related to Paleozoic magmatism are relatively few and have been studied less. In recent years, many workers have conducted research on most gold deposits in this area. This has improved our knowledge of gold mineralization in Northeast China, provided a new direction for the exploration of gold deposits in this area, and contributed to the study of the evolution and mineralization of the Paleo-Asian Ocean and Paleo-Pacific tectonic domains.
The Haigou gold deposit is located on the southeast margin of the Jiapigou-Haigou gold metallogenic belt (Figure 1B). It is one of the important large-scale quartz vein gold deposits in China, with a cumulative production of more than 20 t of gold. Previous studies have mainly examined petrology, mineralogy, deposit geology, deposit geochemistry, structural geology, and isotope chronology, and a series of important research results have been achieved, such as ore characteristics [11,12], surrounding rock alteration [13,14], ore-forming material sources [15,16], diagenetic and ore-forming chronology [17,18,19,20], ore-forming fluid characteristics and sources [21,22,23,24], ore-controlling structure [13,25,26,27,28], ore-forming model [29], and ore-forming prediction [30,31]. However, the genesis, metallogenic age, and metallogenic geological setting of the Haigou gold deposit are still not well understood. (1) In terms of diagenetic and metallogenic chronology, 40Ar/39Ar isotope dating has been carried out on fluid inclusions, altered rock sericite, molybdenite, and pyrite in gold-bearing quartz veins, and vein rocks cutting through gold orebodies. Re-Os isotope dating has been carried out on sulfide and U-Pb isotope dating on zircon, suggesting that the main metallogenic periods of the Haigou gold deposit are 170–160 Ma [4,20] and 135–128 Ma [6,32]. Although there is much data on the chronology of mineralization, the exact metallogenic age remains controversial. (2) In terms of ore-forming material sources and ore-forming fluid characteristics, some scholars believe that the ore-forming materials of the Haigou gold deposit are mainly derived from the Mesoproterozoic greenschist facies metamorphic rock series of the Serohe Group [15,29], and the ore-forming fluids are derived from magmatic-hydrothermal and paleo-atmospheric precipitation [16,22,26,29,32]. However, the Haigou gold deposit contains different types of rock masses and dike rocks. These mainly include the ocean channel complex (monzonitic-monzonitic granite), gabbro diorite, granodiorite, biotite monzonitic granite and its “same source” diorite porphyrite, syenite diorite, lamprogreenite, and other dike rocks [33], but the relationship with gold mineralization is not clear and needs further study. (3) In terms of metallogenic tectonic setting, some scholars believe that the gold-bearing quartz veins of the Haigou gold deposit are controlled by NE-NNE fault structures, and the mineralization is dominated by filling. However, there are still different opinions on whether these ore-controlling fault structures were formed during the continental rift, rift trough, or post-orogenic extension after the final closure of the Paleo-Asian Ocean or during subduction of the paleo-Asian plate at the northern margin of the Boreland [34,35,36,37,38].
Based on previous work, this paper systematically investigates the geology of the Haigou gold deposit, as well as the geochronology and geochemistry of the diorite and diopside diorite veins intimately associated with its mineralization. This research offers a theoretical foundation for a deeper comprehension of the mineralization process of deposits, enabling the determination of their mineralization age and geological context. Additionally, it is of significant importance to study and explore of similar deposits in the region.

2. Geological Background and Deposit Geology

2.1. Geological Background

The southeastern region of Jilin Province is located at the intersection of the eastern segment of the northern margin of the North China Craton and the eastern segment of the southern margin of the Jiamusi Massif. This area has undergone two different stages of tectonic evolution [39,40,41]. The Paleozoic tectonic evolution was mainly controlled by the gradual subduction of the Paleo-Asiatic plate at the northern margin of the North China Craton, while the Mesozoic to Cenozoic tectonic evolution was mainly controlled by the oblique subduction of the Paleo-Pacific plate relative to Eurasia [8,9,10,42,43,44,45]. Under the superimposed transformation of the ancient Asian Ocean and the Pacific Rim tectonic domains, the NE Dunhua-Mishan fault zone developed on the west side of the region, the NE Ji’an-Songjianghe fault developed on the east side, and the NW Furhe fault and Qingchaguan-Jinyinbie fault were displaced (Figure 1B). The Precambrian in the region experienced multiple periods of metamorphism and magmatic activity, and strong tectonic and magmatic emplacement occurred in the Phanerozoic, especially in the Mesozoic, and related gold mineralization developed [46,47,48,49,50,51,52]. The metamorphic rock strata of the Proterozoic Ji’an group, the Seluohe group, the sedimentary strata of the Qingbaikou system, and the volcano-sedimentary strata of the Mesozoic and Cenozoic are mainly found, and the Paleozoic strata are generally missing [6,31]. The intrusive rocks are mainly late Paleozoic granitic rocks, Mesozoic granitic rocks, and diorite rocks, and a large number of intermediate-acidic dike rocks have also been developed. Volcanic rocks can only be found in local areas, mostly Mesozoic and Cenozoic andesite and basalt. [9,53,54,55,56,57]. Secondary fault structures are also well developed in the region, which can be divided into two large-scale fault tectonic systems in the NW-EW and NE-NNE directions, and each fault tectonic system is composed of several faults in the same distribution direction [58,59]. The unique tectonic environment and frequent tectonic-magma-hydrothermal activities in this research area led to the formation of more than 20 large and medium-sized gold deposits, such as Haigou, Jiapigou, Songjianghe, Bajiazi, and Banmiaozi.

2.2. Deposit Geology

The Haigou gold deposit is located at the southeast end of the Jiapigou-Haigou gold belt in southeast Jilin Province, at the intersection of the NE Ji’an-Songjiang fault and the NW Jinyin-Haigou fault, and is controlled by the NE-NNE fault, so it is a prospective quartz vein-type gold deposit [59]. The Seluohe group Mesoproterozoic metamorphic rock series is mainly exposed in mining areas. There are four groups of NE-NEE, NW, near SN, and EW faults, among which NE-NEE faults are the most important ore-controlling structures in the Haigou Gold mine area. Magmatic rocks in the area are well developed, mainly exposed to the gully complex and a series of associated dike rocks, followed by the Yanshanian Huangnihe biotite monzogranite and Dahaigou pyroxene diorite in the northwest and southeast, respectively (Figure 2A). Previous studies have suggested that the complex rock mass of Haigou produces the form of rock strain, which is mainly formed by the successive emplacement of monzonite and monzonite granite, both of which appear as concentric circles in the plane [21,60]. Most gold veins are found in this complex rock mass, which is closely related to the mineralization of the Haigou gold deposit. Through this underground survey, it was found that monzonite granite is closely related to the gold ore body, and there is strong potassization, silicification, sericitization, and pyritization. The local gold grade is generally about 0.5 g/t, up to 3 g/t (Table 1, Figure 3A,B), and gold ore bodies occur in it. At the same time, pyroxene diorite porphyrite veins parallel to the gold ore body were found in the bottom plate, and these veins showed gold-related alteration (Table 1, Figure 3C,D). Through this field investigation and in combination with previous research results, it is believed that the monzonitic granite and pyroxene diorite porphyrite veins are closely related to the gold mineralization of Haigou in terms of space and genesis.
More than 50 gold orebodies have been found in the Haigou gold mine, mainly in monzonitic granite and a small amount in the metamorphic rock series of the Selohe Group (Figure 2A). The ore bodies are mostly regular single veins and are lentil-shaped with different sizes. The ore types are mainly gold-bearing quartz veins and altered rock types. The ore minerals included natural gold, pyrite, galena, and small amounts of sphalerite, chalcopyrite, and pyrrhotite (Figure 4A–C). The gangue minerals are quartz, calcite, plagioclase, sericite, and chlorite. In addition to natural gold, the main gold-bearing minerals are galena, pyrite, quartz, and gold telluride (Figure 4D–I). Natural gold is mostly micro-fissure gold and intergranular gold, and a small amount is encapsulated gold, which is irregularly distributed in the grains of various sulfide ore minerals and gangue minerals, with a fine particle size of 0.001–0.1 mm, and most of it is 0.01–0.03 mm. The ore mainly comprises hemiidiomorphic-heteromorphic grains with metasomatic, inclusive, and cataclastic textures (Figure 4D–I). The ore is dominated by veins, mesh, sparse disseminated structure, star point structure, and block structure (Figure 4A–C).
Taking 28# gold vein as an example, this vein is the largest and most industrially valuable gold-bearing quartz vein in the mining area, with proven gold reserves of 29,676 kg, accounting for more than 80% of the proven gold reserves of the entire gold mine, with a maximum gold grade of 115.0 g/t and an average grade of 8.04 g/t. The lode is generally NE trending, with dips of 310~320° and 45~85°. It gradually steepens with depth. The orebody tapers in both the strike and dip directions and the strike control length exceeds 2400 m [4,7,8,56]. Surrounding rock alteration mainly includes silicification, potassic feldspathization, albitization, pyritization, sericite, and carbonitization, among which potassic and silicitization are the most significant, and silicitization and sericite are most closely related to gold mineralization.

3. Sample and Analytical Methods

3.1. LA-ICP-MS Zircon U–Pb Dating

The selection of zircon single minerals, target preparation, acquisition of zircon reflected light and transmitted light phase images, cathodoluminescence (CL) imaging, and LA-ICP-MS zircon U-Pb isotope analysis were conducted at the Key Laboratory of Northeast Asia Mineral Resources Evaluation under the Ministry of Natural Resources, located in Changchun City, Jilin Province. All samples were collected from fresh, unaltered rock specimens (~5 kg) for the zircon separation. Initially, the samples underwent conventional processing methods, including crushing, washing, sieving, and natural drying. Subsequently, magnetic separation and heavy liquid separation techniques were employed to extract over 100 zircon grains from each monzonite granite (HG-TW1) and pyroxene diorite porphyry vein (HG-TW2) sample obtained from the Haigou mining area. Under a binocular microscope, these grains were meticulously selected based on their clean surfaces, well-defined crystal morphologies, transparencies, and minimal inclusions or fractures. The selected zircon grains were embedded in an epoxy resin base and polished to approximately half of their original thickness to expose the crystal core for target preparation. Microscopic images of the zircon grains were captured under both reflected and transmitted light conditions. Cathodoluminescence (CL) images of the zircon grains were subsequently acquired using a JEOL scanning electron microscope to examine their internal structures and determine the optimal spot positions for zircon U-Pb isotope analysis, which was ultimately used for age determination. The spots were positioned as close as possible to the zircon growth zones to avoid inclusions and fractures (Figure 5).
Zircon U-Pb isotope age determination was performed using an Agilent 7500A quadrupole inductively coupled plasma mass spectrometer (ICP-MS) from the United States in conjunction with a COMPExPro 193 nm ArF excimer laser. The beam spot diameter was set to 32 μm. For every six sample measurements, one standard zircon 91500 and one NIST610 were analyzed as external standards. Age calculations were corrected for isotope ratio fractionation using standard zircon 91500 as an external reference. Element concentration calculations utilized NIST610 as the external standard and silicon (Si) as the internal standard [61]. Errors in the isotope ratios and ages are reported at the 2σ confidence level. The detailed experimental procedure can be found in the relevant literature [62,63,64]. Correlation processing of the zircon isotope data was conducted using the Glitter 4.0 software. A common lead correction was performed using Anderson’s method [65], while Isoplot 3.0 was used to calculate the weighted average age of the zircons [66] and plot the zircon U-Pb age concordia curve (Figure 6).

3.2. Major and Trace Element Concentrations

Sample processing, as well as the analysis and testing of major, trace, and rare earth elements in rocks, were completed by the Laboratory of the Mudanjiang Natural Resources Comprehensive Survey Center, China Geological Survey. Sample collection involved selecting fresh, unaltered rock samples. Sample processing involved first removing the weathered surface, followed by cleaning, crushing, grinding, and reducing the ground powder to below 200 mesh. Finally, whole-rock major, trace, and rare earth element analyses were conducted. The laboratory employs an X-ray fluorescence spectrometer to determine the major elements, with a relative standard deviation (RSD) of 2%–5%. Trace elements and rare earth elements (REEs) were analyzed using an inductively coupled plasma mass spectrometer (ICP-MS). The precision of the analysis is determined by the element content: when the content exceeds 10 × 10−6, the precision is better than 5%; for contents below 10 × 10−6, the precision is better than 10%. The detailed experimental operation process and method were described by Qi and Zhou [67].

4. Analytical Results

4.1. Zircon U–Pb Age

The LA-ICP-MS zircon U–Pb ages for monzonitic granite (HG-TW1) and pyroxene diorite porphyrite (HG-TW2) are listed in Table 2 and shown in Figure 5. All zircon grains from the monzonitic granite and pyroxene diorite porphyrite samples were euhedral–subhedral in shape and transparent and mostly displayed oscillatory growth zoning in CL images (Figure 5) and high Th/U ratios (0.16–1.21 > 0.1), indicating a magmatic origin [68,69,70].
For sample HG-TW1, the 206Pb/238U ages of 22 analytical spots yield 206Pb/238U ages range from 310 ± 7 Ma to 324 ± 8 Ma, with a weighted mean age of 317.1 ± 3.5 Ma (MSWD = 0.12, N = 22; Figure 6). Except for three analytical spots showing 206Pb/238U ages of 1992 ± 39 Ma, 2124 ± 48 Ma, and 282 ± 7 Ma, the 206Pb/238U ages of 24 analytical spots from sample HG-TW2 vary from 302 ± 8 Ma to 313 ± 7 Ma, with the Concordia U–Pb age and weighted mean age of 309.2 ± 1.5 Ma and 308.8 ± 3.0 Ma (MSWD = 0.10, N = 24; Figure 6), respectively. Two older zircons (1992 ± 39 Ma and 2124 ± 48 Ma) from sample HG-TW2, combined with CL images of zircons, are interpreted as inherited or captured zircons entrained by the magma.

4.2. Major and Trace Element

The whole-rock major and trace element concentrations of the monzonitic granite (HG-TW1) and pyroxene diorite porphyrite (HG-TW2) from the Haigou deposit are presented in Table 3. The monzonitic granite has high SiO2 (70.47–71.01 wt. %) and Na2O + K2O (9.74–10.17 wt.%) and contains Al2O3 content of 14.56–15.02 wt.%, TFe2O3 content of 1.08–1.93 wt.%, CaO content of 1.35–1.89 wt.%, TiO2 content of 0.11–0.15 wt.%, and MgO content of 0.17–0.33 wt.%, with Mg# [Mg# = 100 × Mg2+/(Mg2+ + TFe2+)] values varying from 9 to 19. Compared with monzonitic granite, pyroxene diorite porphyrite has relatively lower SiO2 ratios, ranging from 52.90 to 54.09 wt.%, Na2O + K2O varying from 4.55 to 5.28 wt.%, but relatively higher Al2O3 (14.54–15.30 wt.%), TFe2O3 (7.29–7.75 wt.%), CaO (6.63–8.32 wt.%), TiO2 (0.56–0.60 wt.%) and similar MgO (8.13–9.27 wt.%), with higher Mg# values ranging from 49 to 51. Their A/CNK ratios vary from 0.88 to 0.91 and range from 0.69 to 0.81, and A/NK ratios vary from 1.03 to 1.09 and range from 1.98 to 2.33, respectively, indicative of metaluminous rocks. In the w(SiO2) % vs. w(Na2O + K2O) % diagram (Figure 7A), monzonitic granites are divided into alkaline series and pyroxene diorite porphyrite samples are divided into subalkaline series, mainly located in the granite and gabbro diorite regions, respectively. This is consistent with the characteristics identified under a microscope. On the A/CNK vs. A/NK diagram (Figure 7B), they all fall into the metaluminous region, and in the SiO2 vs. K2O diagrams (Figure 7C), they all fall into the high-K calc-alkaline series field.
In the chondrite-normalized rare earth element (REE) patterns (Table 3, Figure 8A), the monzonitic granite and pyroxene diorite porphyrite samples from the Haigou deposit have different degrees of enrichment in light rare-earth elements (LREEs) relative to heavy rare-earth elements (HREEs). The monzonitic granite samples [LREE/HREE = 14.64–19.51, (La/Yb)N = 28.80–44.14] are more fractionated than the pyroxene diorite porphyrite samples [LREE/HREE = 7.43–8.18, (La/Yb)N = 9.67–11.21]. The monzonitic granite has obviously positive Eu anomalies (δEu = 1.15–1.46), while the pyroxene diorite porphyrite shows slightly positive Eu anomalies (δEu = 1.09–1.13). The weak positive Eu anomaly of monzonitic granite (HG-TW1) may be related to the fact that plagioclase was not completely separated during the formation of the magma or that plagioclase remained in the source area during the partial melting process. These processes affect the distribution of Eu in the magma, thereby forming a positive Eu anomaly. The weak positive Eu anomaly of the pyroxene diorite porphyritic (HG-TW2) may have led to the enrichment of Eu in the remaining magma relative to other rare earth elements during the magmatic evolution process due to the crystallization and separation of plagioclase. In the primitive mantle-normalized geochemical patterns (Table 3, Figure 8B), the monzonitic granite and pyroxene diorite porphyrite samples are enriched in large-ion lithophile elements (LILEs; e.g., Rb, Ba, and K) with obvious negative Ta, Nb, P, and Ti anomalies. The monzonitic granite, relative to the pyroxene diorite porphyrite, displays more intense depletion in high-field-strength elements (HFSEs; e.g., Zr, Hf, P, and Ti) and more enrichment in Sr, Nd, and Sm.

5. Discussion

5.1. Age of Magmatic Hydrothermal Events and Gold-Bearing Quartz Veins Mineralization

Previous studies on the metallogenic ages of the Haigou region have reached the following conclusions: The ore-forming ages of the Haigou gold deposit with quartz fluid inclusion dating by laser probe 40Ar/39Ar are 170 ± 20Ma and 172 ± 16 Ma, suggesting that the main ore-forming stage of the Haigou gold deposit occurred in the late Early Jurassic [4,20]. The U-Pb age of the vein rocks almost parallel to the veins is determined to be 132–128 Ma [6,32], and the metallogenic time of the Jiapigou-Haigou gold metallogenic belt is 102 ± 2 Ma, suggesting that the gold ore age in this area is Mesozoic [18]. Previous studies have proposed that gold mineralization in the Haigou gold deposit occurred during the Yanshanian period based on the spatial interpenetration relationships between different dike rocks and quartz vein ore bodies. The primary geological evidence includes diorite porphyry veins and gold-bearing quartz veins located in the same tectonic fractures, often produced in parallel, with local occurrences of quartz veins cutting through the diorite porphyry. Additionally, the diorite porphyry in these areas has undergone alteration and gold mineralization, suggesting that its formation occurred slightly earlier than that of the gold-bearing quartz veins. Pyroxene diorite porphyry, which cuts through the Haigou rock body and gold-bearing quartz veins, represents a late-stage dike; thus, its formation time should be later than the mineralization period.
This study conducted LA-ICP-MS dating analyses on typical magmatic zircon crystals from two-mica granite samples and pyroxene diorite porphyry vein samples in the Haigou gold district. The calculated weighted average U-Pb ages of the zircons are 317.1 ± 3.5 Ma and 308.8 ± 3.0 Ma. These results indicate that medium-acidic magmatic-hydrothermal events occurred in this region during the Late Carboniferous. The zircon U-Pb dating results from two grains in the pyroxene diorite porphyry veins yielded ages of 1992 ± 39 Ma and 2124 ± 48 Ma, which are consistent with the ages of the regional Paleoproterozoic metamorphic rock series, indicating that these Paleoproterozoic rocks likely underlay the area at the time of emplacement. The age of the monzogranite sample (317.1 ± 3.5 Ma) was significantly older than that of the pyroxene diorite porphyry vein sample (308.8 ± 3.0 Ma). Zhai et al. (2019) [57] proposed that the formation of molybdenite in the Haigou gold district may be related to hydrothermal activity during the early stages of mineralization based on mineralogical characteristics and established mineralization-stage sequences. They inferred that molybdenite formation occurred either slightly earlier than or contemporaneously with gold mineralization. Systematic sampling of pyrite samples closely associated with gold mineralization was also conducted, suggesting that pyrite in gold-bearing quartz veins formed largely synchronously with gold deposition. High-precision Re-Os dating was performed on molybdenite and pyrite from ore-bearing quartz veins [58]. The results yielded a molybdenite model age of (306.9 ± 6.7) Ma, a pyrite model age of (297 ± 20) Ma, and isochron ages of 311.2 ± 4.8 Ma for molybdenite and 320 ± 11 Ma for pyrite [58]. Most quartz vein-type gold bodies in the Haigou gold deposit are hosted within monzogranite bodies. Intensive alteration of the monzogranite adjacent to gold-bearing quartz veins was observed, with localized gold grades reaching up to 0.5 g/t (maximum 3 g/t). Pyroxene diorite porphyry veins intrude into the monzogranite and occur below the gold-bearing quartz veins, forming parallel structures. The spatial and genetic relationships among monzonitic granite, pyroxene diorite porphyry veins, and gold-bearing quartz veins support this conclusion.
In summary, the monzogranite and pyroxene diorite porphyry veins exhibit close spatial, temporal, and genetic associations with gold mineralization. This suggests that gold mineralization in the Haigou gold district occurred during the Late Carboniferous (317–309 Ma), with a mineralization duration of approximately 8 Ma. The findings suggest that a distinct gold-forming episode occurred during the Haixi period in this region, dominated by magmatic rocks such as monzogranite and pyroxene diorite porphyry veins. It was also mentioned earlier that some scholars have obtained the age of mineralization in the Mesozoic Era in this mining area. Therefore, this work cannot deny that gold mineralization had a reactivation and enrichment effect during the Late Yanshan period. Previous achievements can limit the mineralization time of this period to a lower limit, which should not be later than 135 Ma.

5.2. Tectonic Setting and Associated Mineralization

The geochemical characteristics of the monzogranite associated with gold-bearing quartz veins are as follows: it exhibits high SiO2 (silica), K (potassium), and Al2O3 (alumina) contents, coupled with low MgO (magnesium oxide) and CaO (calcium oxide) levels, classifying it as a metaluminous high-K calc-alkaline rock (Figure 7C). The rock shows enrichment in light rare earth elements (LREE) and large ion lithophile elements (LILE) (e.g., Rb, Ba, K), while heavy rare earth elements (HREE) and high-field-strength elements (HFSE) (e.g., Nb, Ta, P, Ti) are relatively depleted. The depletion of P and Ti may be attributed to the significant fractional crystallization of apatite, sphene, and ilmenite during magma evolution, which is consistent with the relative enrichment of Sr. The negative anomalies of Nb and Ta in the rock suggest a mantle-derived origin associated with subduction zones [75] or crustal contamination of magma [76,77]. In the SiO2 vs. Ce (Figure 9A) and SiO2 vs. Zr (Figure 9B) discrimination diagrams, the monzogranite plots fall within the I-type granite field, indicating that it formed primarily by the partial melting of unweathered crustal igneous rocks. However, the possibility of a mantle-derived magma contribution to the Haigou pluton cannot be entirely excluded. In recent years, several scholars have conducted specialized studies in this field and reported Sr, Nd, and Pb isotope analysis results for monzonite granites derived from this paper, suggesting that the Haigou rock mass exhibits a Type I enrichment mantle evolution trend. The magma source region is complex and likely not derived from a single crustal or mantle source but rather from a crust-mantle mixed origin. Proterozoic crustal material is inferred to be the primary source, while the magma may represent the product of partial melting of lower crustal material with significant contributions from mantle components [7]. From the tectonic environment discriminant diagrams, the monzogranite samples plot near the boundary between syn-collisional granite and volcanic arc granite on the Yb vs. Ta diagram (Figure 9C). On the (Yb + Ta) vs. Rb diagram (Figure 9D), all the tested samples fall within the volcanic-arc granite field, indicating that the monzogranite is predominantly volcanic-arc derived. On the Ta/Yb vs. Th/Yb diagram (Figure 9E), the monzogranite samples are concentrated near the active continental margin (continental arc) region. Monzonite granite is characterized by large ion lithophile (LILE) enrichment and high field strength (HFSE) deficit and has an obvious Ta-Nb-Sr-P-Ti deficit, with a subduction background similar to that of the active continental margin. This suggests that the tectonic background of mineralization in the Haigou gold deposit is that of an active continental margin. In addition, a large amount of chronological data, geochemical characteristics, and regional tectonic evolution indicate that the area was in an active continental margin arc environment during the Late Carboniferous, which was related to the subduction of the Lower Paleo-Asian Ocean plate of the North China Craton to the south. Consequently, we propose that the monzogranite and its associated gold mineralization formed during the Late Carboniferous (~317 Ma).
The geochemical characteristics of pyroxene diorite porphyry veins, which occur parallel to gold-bearing quartz veins within the same tectonic fault zone, indicate the following: This rock type is distinguished by relative enrichment of light rare earth elements (LREE) compared to heavy rare earth elements (HREE), a weak positive europium anomaly as reflected in δEu values, and relatively high ratios of Nb/Ta and Zr/Hf (15–17 and 25–29, respectively). These features suggest that the magma source exhibits properties consistent with those of mantle-derived magma. In the discriminant diagram of Ta/Yb vs. Th/Yb (Figure 9E), the pyroxene diorite porphyrite vein samples fall in the island arc basalt region near the active continental margin (continental arc) region. In the discrimination diagram of Ta/Hf vs. Th/Hf (Figure 9F), pyroxene diorite porphyry vein samples fall in the continental island arc and volcanic arc basalt area of the plate convergence margin, which further indicates that the tectonic background of gold mineralization of the Haigou gold deposit is an active continental margin, which was formed in the subduction collision environment of the ancient Asian Ocean. This is related to the subduction of the lower PaleoAsian Ocean plate of the North China Craton to the south. Chronologically, gold mineralization occurred during dike rock activity (308 Ma ± 3 Ma). The relationship between pyroxene diorite porphyrite veins and gold-bearing quartz veins: the strong alteration of pyroxene diorite porphyrite veins and local gold mineralization to form a gold ore body suggests that pyroxene diorite porphyrite magmatism was a source of ore-forming fluids.
Therefore, the late Carboniferous monzonitic granite and pyroxene diorite porphyrite veins of the Haigou gold deposit are directly or indirectly related to gold mineralization. The frequent activities of monzonitic granite and pyroxene diorite porphyrite veins not only provide heat sources for gold mineralization but also bring a large number of deep-source fluids and some ore-forming materials for gold mineralization. The diagenetic age of the Haigou gold deposit can represent the ore-forming age.

5.3. Genesis and Metallogenic Significance of Ore Deposit

Located at the intersection between the Central Asian Orogenic Belt and the eastern segments of the NCC, southeast Jilin Province has successively experienced the evolution and transition of the Paleo-Asian Ocean and Paleo-Pacific Ocean metallogenic domains [1,2,3,4,5,30,31,32,33,34]. During the Carboniferous, sustained subduction of the Lower Paleo-Asian Ocean plate in the North China Craton formed a large number of crust and mantle-derived granites and basic dike rocks, which were accompanied by gold and polymetallic mineralization. Recent studies have shown that this region experienced a transition from the closure of the Paleo-Asian Ocean collision to post-collision extension during the Triassic period. A large number of Mesozoic polymetallic deposits have been discovered, including porphyry copper-molybdenum deposits (such as Guokuidingzi) and magmatic copper-nickel sulfide deposits (such as Hongqiling). In the Early and Middle Jurassic, the regional tectonic setting changed to the subduction of the paleo-Pacific plate under Eurasia, forming mesothermal hydrothermal quartz vein-type gold deposits (such as Erdaodianzi), volcanic rock-type gold deposits (such as Guanma) and crushed alteration type gold deposits (such as Houliushuhezi), however, Paleozoic deposits are almost unknown. The late Paleozoic gold-polymetallic deposits newly discovered in central and eastern Jilin Province in recent years, including the polymetallic mineralization processes of Xiaohongshilazi Pb Zn, Hongtaiping and Dongfeng Nanshan Cu Pb Zn, were formed in an active continental margin environment during the subduction of the Paleo-Asian Ocean and developed along the Suolun-Xilamulun-Changchun-Yanji suture zone [3]. The discovery of these deposits not only contributes to the study of Paleozoic mineralization in this area but also provides theoretical support for the search for similar gold polymetallic deposits and the study of the evolution and mineralization of the Northeast Paleo-Asian Ocean.
At present, gold-bearing quartz vein-type gold mineralization generally occurs in Carboniferous island-arc-type granite, and no Paleozoic gold-bearing quartz vein-type gold deposit has been found in the eastern part of Heilongjiang Province and Jilin Province, which may be due to the local extension or rift structure under the subduction of the Paleozoic Paleo-Asian oceanic plate in this area. The Late Carboniferous island-arc granite is the main ore-bearing body of gold-bearing quartz vein-type gold mineralization in this area, and its gold background anomaly value is very high, indicating that the island-arc granite formed by the subduction of the Paleo-Asian Ocean under the active continental margin background of the Late Carboniferous can be used as an important prospecting indicator of gold-bearing quartz vein-type gold deposits in this area. Therefore, the deep edge of the Haigou gold deposit and its periphery are important areas for further exploration of Late Carboniferous magmatic-hydrothermal gold deposits related to the evolution of the Paleo-Asian Ocean. At the same time, Panshi and Yongji in the middle of Jilin Province and Longjing and Kaishantun in the east of Jilin Province belong to the same regional metallogenic geological background as the Haigou mining area and also have metallogenic potential for gold, copper, lead, and zinc.

6. Conclusions

(1)
Quartz vein-type gold mineralization is closely related to the central monzonite granite of the Haigou complex and the pyroxene diorite porphyrite veins of the same tectonic period. Quartz vein-type gold mineralization occurs mostly in monzonite granite, and pyroxene diorite porphyrite veins occur mostly in unified tectonic fractures. Pyroxene diorite porphyrite veins are consistent with quartz vein-type gold mineralization and are located parallel to the quartz vein-type gold mineralization footwall. The ages of monzonitic granite and pyroxene diorite porphyrite veins are 317.1 ± 3.5 Ma and 308.8 ± 3.0 Ma, respectively, which are spatially, temporally, and genetically related to quartz vein-type gold mineralization, suggesting that gold mineralization occurred in the Late Carboniferous Epoch.
(2)
Monzonitic granite, closely related to quartz vein-type gold mineralization, exhibits a trend of type I enrichment mantle evolution, and the magma source area is complex, possibly a crust-mantle mixed source. The Proterozoic shell source material is the main source, which may be the product of partial melting of the lower crust material and may have more mantle material added. Monzonitic magmatism not only provides a heat source for gold mineralization but may also transport deep fluids with gold.
(3)
The geochemical characteristics of monzonitic granite and pyroxene diorite porphyrite dike rocks show that they are metaluminous high-potassium calc-alkaline rocks, both of which are enriched in light rare earth elements (LREE) and large ion-lithophile elements (LILE), and deficient in heavy rare earth elements (HREE) and high field strength elements (HFSE). This suggests that they formed in an active continental margin arc environment caused by the subduction of the Paleo-Asiatic plate during the Late Carboniferous.
(4)
The metallogenic dynamic background of the Haigou gold deposit is the mantle upsurge under the continuous subduction of the lower Paleo-Asian Ocean plate in the late Paleozoic North China Craton, and the fragmentation and reduction of the mantle lithosphere led to strong tectonic, magmatic, and hydrothermal activities, which resulted in the formation of a large number of crust and mantle-derived granites and basic dyke rocks, accompanied by gold and polymetallic mineralization.
(5)
Late Carboniferous monzonite granite and pyroxene diorite porphyrite veins are closely related to magmatic-hydrothermal quartz vein gold mineralization and are important prospecting indicators of similar gold-bearing quartz vein gold deposits in this area.

Author Contributions

Conceptualization: Z.Y., Y.Z., and C.Z.; field investigation: Z.Y., Q.Y., and L.Z.; experimental analysis: Z.Y., Y.Z., and C.Z.; software: C.R.; validation: Z.Y.; resources: Z.Y. and C.Z.; data curation: Z.Y.; writing-original draft preparation: Z.Y. and Q.Y.; writing-review and editing: Z.Y.; visualization: L.Z.; funding acquisition: Z.Y. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the funding project of the Northeast Geological S&T Innovation Center of the China Geological Survey (NO. QCJJ2023-15, NO. QCJJ2022-14), and the Dynamic Evaluation Project of Gold Resource Potential in Eastern Jilin-Heilongjiang Area (DD20230373).

Data Availability Statement

The data presented in this study are available on request from the corresponding author.

Acknowledgments

We thank the leaders and geologists of the Haigou ore district for their support of our fieldwork.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 1. (A) Simplified tectonic map of NE China (modified from Wu et al. [1]); (B) regional geological map of southeast Jilin Province (modified from Fan [7]).
Figure 1. (A) Simplified tectonic map of NE China (modified from Wu et al. [1]); (B) regional geological map of southeast Jilin Province (modified from Fan [7]).
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Figure 2. (A) Regional geological sketch map of the Haigou gold deposit (modified from Qiu [8]); (B) Profile map of exploration line from the Haigou gold deposit (modified from Qiu [8]).
Figure 2. (A) Regional geological sketch map of the Haigou gold deposit (modified from Qiu [8]); (B) Profile map of exploration line from the Haigou gold deposit (modified from Qiu [8]).
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Figure 3. Photomicrographs of the magmatic rock of the Haigou gold deposit. Instructions: (A,B) Monzonitic granite (HG-TW1; A field hand specimen; B under cross-polarized light); (C,D) Pyroxene diorite porphyrite vein (HG-TW1; C field hand specimen; D under cross-polarized light. Abbreviations: Px: pyroxene; Pl: plagioclase; kfs: K-feldspar; Bt: Biotite; Qz: quartz.
Figure 3. Photomicrographs of the magmatic rock of the Haigou gold deposit. Instructions: (A,B) Monzonitic granite (HG-TW1; A field hand specimen; B under cross-polarized light); (C,D) Pyroxene diorite porphyrite vein (HG-TW1; C field hand specimen; D under cross-polarized light. Abbreviations: Px: pyroxene; Pl: plagioclase; kfs: K-feldspar; Bt: Biotite; Qz: quartz.
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Figure 4. Representative photographs showing the texture and structure of the orebodies in the Haigou gold deposit. (A) Lumpy pyrite quartz vein, Medium coarse-grained idiomorphic pyrite; (B) Lumpy pyrite quartz vein, Fine-grained hemidiomorphic-heteromorphic pyrite; (C) Molybdenite quartz veins, Thin film molybdenite; (D) Gold-bearing pyrite quartz veins (reflected light); (E) Gold ore (reflected light); (F) Pyrite fossil quartz vein type ore with idiomorphic to semi-idiomorphic vein structure (reflected light); (G) Early galena by pyrite coating during the major stage of the vein-type mineralization(reflected light); (H) Pyrite replaced by galena during the major stage of the vein-type mineralization (reflected light); (I) Symbiosis of pyrrhotite, pyrite and chalcopyrite in vein-type mineralization(reflected light). Abbreviations: Gl: gold; Py: pyrite; Ccp: Chalcopyrite; Sp: sphalerite; Gn: galena; Po: pyrrhotite; Qtz: quartz.
Figure 4. Representative photographs showing the texture and structure of the orebodies in the Haigou gold deposit. (A) Lumpy pyrite quartz vein, Medium coarse-grained idiomorphic pyrite; (B) Lumpy pyrite quartz vein, Fine-grained hemidiomorphic-heteromorphic pyrite; (C) Molybdenite quartz veins, Thin film molybdenite; (D) Gold-bearing pyrite quartz veins (reflected light); (E) Gold ore (reflected light); (F) Pyrite fossil quartz vein type ore with idiomorphic to semi-idiomorphic vein structure (reflected light); (G) Early galena by pyrite coating during the major stage of the vein-type mineralization(reflected light); (H) Pyrite replaced by galena during the major stage of the vein-type mineralization (reflected light); (I) Symbiosis of pyrrhotite, pyrite and chalcopyrite in vein-type mineralization(reflected light). Abbreviations: Gl: gold; Py: pyrite; Ccp: Chalcopyrite; Sp: sphalerite; Gn: galena; Po: pyrrhotite; Qtz: quartz.
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Figure 5. Cathodoluminescence (CL) images of representative zircon grains from monzonite granites (HG-TW1) and pyroxene diorite porphyry veins (HG-TW2) in the Haigou deposit are shown. The red circle highlights the spot for U-Pb dating analysis.
Figure 5. Cathodoluminescence (CL) images of representative zircon grains from monzonite granites (HG-TW1) and pyroxene diorite porphyry veins (HG-TW2) in the Haigou deposit are shown. The red circle highlights the spot for U-Pb dating analysis.
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Figure 6. LA-ICP-MS zircon U–Pb concordia and weighted mean age diagrams for the monzonitic granite (HG-TW1) and pyroxene diorite porphyrite (HG-TW2) from the Haigou deposit.
Figure 6. LA-ICP-MS zircon U–Pb concordia and weighted mean age diagrams for the monzonitic granite (HG-TW1) and pyroxene diorite porphyrite (HG-TW2) from the Haigou deposit.
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Figure 7. (A) w(SiO2) % vs. w(Na2O + K2O) % diagram (modified from Middlemost E A K [71]); (B) A/CNK vs. A/NK diagram (modified from Maniar P D and Piccoli P M [72]); (C) w(SiO2) % vs. w(K2O) % diagram (modified from Peccerillo and Taylor [73]).
Figure 7. (A) w(SiO2) % vs. w(Na2O + K2O) % diagram (modified from Middlemost E A K [71]); (B) A/CNK vs. A/NK diagram (modified from Maniar P D and Piccoli P M [72]); (C) w(SiO2) % vs. w(K2O) % diagram (modified from Peccerillo and Taylor [73]).
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Figure 8. (A) Chondrite-normalized rare earth element (REE) patterns and (B) primitive mantle-normalized geochemical patterns for the rhyolite and dacite from the Haigou deposit. Chondrite and primitive mantle values are from Boynton [74] and Sun and McDinough [75], respectively.
Figure 8. (A) Chondrite-normalized rare earth element (REE) patterns and (B) primitive mantle-normalized geochemical patterns for the rhyolite and dacite from the Haigou deposit. Chondrite and primitive mantle values are from Boynton [74] and Sun and McDinough [75], respectively.
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Figure 9. (A) SiO2 vs. Ce diagram (modified from Collins et al. [78]); (B) SiO2 vs. Zr diagram (modified from Collins et al. [78]); (C) Yb vs. Ta diagram (modified from Pearce et al. [79]); (D) Yb + Ta vs. Rb diagram (modified from Pearce et al. [79]); (E) Ta/Yb vs. Th/Yb diagram (modified from Pearce et al. [80]); (F) Ta/Hf vs. Th/Hf (modified from Wang et al. [81]).
Figure 9. (A) SiO2 vs. Ce diagram (modified from Collins et al. [78]); (B) SiO2 vs. Zr diagram (modified from Collins et al. [78]); (C) Yb vs. Ta diagram (modified from Pearce et al. [79]); (D) Yb + Ta vs. Rb diagram (modified from Pearce et al. [79]); (E) Ta/Yb vs. Th/Yb diagram (modified from Pearce et al. [80]); (F) Ta/Hf vs. Th/Hf (modified from Wang et al. [81]).
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Table 1. Characteristics of the volcanic rocks in the Haigou ore district.
Table 1. Characteristics of the volcanic rocks in the Haigou ore district.
Sample No.LithologyLocationTexture/StructureMineral Composition
HG-TW1monzonite granite8 middle section of Xiaohaigou mining areaMedium-fine grain granitic texture/
Massive structure		The mineral composition is mainly composed of plagioclase, potassium feldspar, quartz, biotite, and hornblende. Plagioclase, idiomorphic to semi-idiomorphic structure, with a particle size of 2–4 mm and a content of 30%; Potassium feldspar, idiomorphic to semi-idiomorphic structure, particle size in 2–4 mm, the content accounts for 35%; Quartz, heteromorphic granular structure, particle size in 1–3 mm, the content accounts for 25%; Biotite, sheet structure, slice diameter in 1–3 mm, content accounted for 8%; Hornblende, semi-idiomorphic plate columnar structure, particle size in 1–3 mm, content accounts for 2%; The local feldspar shows obvious kaolin alteration, and the amphibole shows biotite alteration.
HG-TW2pyroxene diorite porphyrite veins8 middle section of Xiaohaigou mining areaPorphyritic texture massive structurePhenocrysts account for 20% of the rock and consist of plagioclase (1–3 mm, partly altered to kaolinite).
Matrix is primarily microscopy cryptocrystalline texture and is dominated by plagioclase (0.1–0.3 mm) and minor amphibole (~0.2 mm)
Table 2. LA-ICP-MS zircon U–Pb dating data of monzonitic granite and pyroxene diorite porphyrite in the Haigou deposit.
Table 2. LA-ICP-MS zircon U–Pb dating data of monzonitic granite and pyroxene diorite porphyrite in the Haigou deposit.
Sample No.Element Content (ppm)Th/UIsotope Ratio (± 2σ)Age (Ma ± 2σ)
232Th238U207Pb/206Pb207Pb/235U206Pb/238U207Pb/206Pb207Pb/235U206Pb/238U
Ratios2σRatios2σRatios2σAge2σAge2σAge2σ
HG-TW1 Monzonitic granite
HG-TW1-1141 906 0.16 0.052410.001910.364350.013420.050420.001230343315103177
HG-TW1-2147 159 0.92 0.054350.005070.378410.034410.050490.001713861443262531810
HG-TW1-395 141 0.67 0.052180.005250.362250.035560.050350.001762931583142731711
HG-TW1-4112 203 0.55 0.053530.003470.371660.02370.050350.0014335193321183179
HG-TW1-5127 198 0.64 0.052430.00220.36840.015480.050960.0012530453318113208
HG-TW1-6154 217 0.71 0.053330.007020.364590.046520.049580.00213432103163531213
HG-TW1-7156 200 0.78 0.052570.003720.36610.025410.050510.00148310105317193189
HG-TW1-8205 202 1.01 0.053480.001910.380090.013860.051540.0012434942327103248
HG-TW1-9120 184 0.65 0.052740.002080.366290.014670.050370.0012331849317113178
HG-TW1-10131 167 0.78 0.053350.002350.371530.016330.050510.0012534456321123188
HG-TW1-11141 221 0.64 0.053380.001850.371540.013220.050490.0012134540321103187
HG-TW1-1292 153 0.60 0.053680.002150.370120.014970.050010.0012335849320113158
HG-TW1-13305 269 1.13 0.053010.002270.360580.015520.049340.0012232954313123107
HG-TW1-1465 103 0.63 0.052950.003460.368180.023640.050440.0014232795318183179
HG-TW1-15131 203 0.64 0.053260.002620.373230.018280.050830.001334065322143208
HG-TW1-1676 127 0.60 0.053190.007250.367810.048650.050150.002163372183183631513
HG-TW1-17165 370 0.45 0.052450.004470.362140.030150.050080.00163051313142231510
HG-TW1-18211 203 1.04 0.052380.002240.365880.015660.050670.0012530254317123198
HG-TW1-1978 129 0.61 0.052350.004070.362780.027550.050260.00153301118314213169
HG-TW1-20178 188 0.95 0.052820.002190.365370.015240.050170.0012332152316113168
HG-TW1-21134 192 0.70 0.0520.0020.358780.013960.050040.0012128547311103157
HG-TW1-22134 207 0.65 0.053670.002230.375660.01570.050770.0012535752324123198
HG-TW2 Pyroxene diorite porphyrite
HG-TW2-1249 617 0.40 0.052880.003460.359760.023050.049330.0013832495312173108
HG-TW2-2194 352 0.55 0.053770.002210.364530.015240.049160.0012336151316113098
HG-TW2-3166 317 0.52 0.053170.004380.354770.028580.048380.00153336125308213059
HG-TW2-4202 343 0.59 0.052590.002280.356180.015620.049110.0012331156309123098
HG-TW2-593 226 0.41 0.053810.003890.363420.025790.048980.00146363106315193089
HG-TW2-6102 271 0.38 0.054750.004360.371610.028970.049220.00153402119321213109
HG-TW2-7267 431 0.62 0.053450.001950.363090.013590.049270.001234843315103107
HG-TW2-8235 535 0.44 0.056440.002510.348140.015470.044750.0011447055303122827
HG-TW2-9161 414 0.39 0.052040.001850.354460.012920.04940.0011928742308103117
HG-TW2-10307 431 0.71 0.053920.003520.3570.022930.048020.0013736894310173028
HG-TW2-11538 1160 0.46 0.05240.002350.354360.015980.049050.0012430358308123098
HG-TW2-12404 651 0.62 0.052920.001850.358810.01270.049180.001163254131193097
HG-TW2-13333 685 0.49 0.053030.001490.358040.010420.048960.001113303131183087
HG-TW2-14173 418 0.41 0.05250.001580.359730.011130.049690.001143073331283137
HG-TW2-15245 385 0.64 0.053630.003050.356960.020080.048280.001335679310153048
HG-TW2-16152 302 0.50 0.052870.003560.357870.023630.04910.0014132398311183099
HG-TW2-17224 461 0.48 0.052990.002580.360650.017480.049360.0012632865313133118
HG-TW2-18131 285 0.46 0.052750.002020.356550.013840.049030.0011931847310103097
HG-TW2-19172 142 1.21 0.1640.00359.085550.212470.401530.009082285102220746212448
HG-TW2-20493 604 0.82 0.053130.001990.356020.013530.04860.0011733445309103067
HG-TW2-21196 363 0.54 0.052770.00180.358680.012520.04930.001173194031193107
HG-TW2-22247 502 0.49 0.052630.001930.356010.013240.049070.0011731344309103097
HG-TW2-23188 486 0.39 0.053090.002010.360470.013820.049250.0011833346313103107
HG-TW2-24214 410 0.52 0.052310.002520.356850.01710.049480.0012529964310133118
HG-TW2-25208 426 0.49 0.053150.001750.358770.012040.048950.001143353831193087
HG-TW2-26248 455 0.54 0.052830.002290.357490.015460.049080.0012132255310123097
HG-TW2-27241 475 0.51 0.161360.003318.105050.182360.36390.00805243665221927199239
Table 3. Whole-rock major and trace element data of biotite monzonitic granite and pyroxene diorite porphyrite in the Haigou deposit.
Table 3. Whole-rock major and trace element data of biotite monzonitic granite and pyroxene diorite porphyrite in the Haigou deposit.
Sample No.HG-TY1HG-TY2HG-TY3HG-TY4HG-TY5HG-TY6HG-TY7HG-TY8HG-TY9HG-TY10
Monzonitic GranitePyroxene Diorite Porphyrite
Major element (wt. %)
SiO270.66 70.47 70.52 70.98 71.01 53.80 54.09 53.48 52.90 53.45
TiO20.11 0.15 0.13 0.14 0.11 0.58 0.56 0.59 0.58 0.60
Al2O314.98 15.02 14.81 14.56 14.72 14.84 14.54 14.71 14.99 15.30
TFe2O31.17 1.08 1.71 1.93 1.33 7.29 7.39 7.49 7.75 7.75
MnO0.03 0.03 0.03 0.02 0.04 0.14 0.14 0.15 0.14 0.14
MgO0.33 0.29 0.19 0.21 0.17 8.13 8.46 8.63 9.27 8.99
CaO1.53 1.89 1.35 1.49 1.35 8.32 8.31 7.15 7.95 6.63
Na2O5.76 5.65 5.68 5.54 5.74 2.69 2.66 3.02 2.64 3.04
K2O3.98 4.11 4.15 4.19 4.43 2.20 1.89 2.26 1.94 1.97
P2O50.06 0.05 0.04 0.03 0.03 0.14 0.14 0.14 0.14 0.15
LOl1.32 1.21 1.33 0.85 1.01 1.46 1.38 2.02 1.28 1.51
Total99.93 99.95 99.94 99.94 99.94 99.59 99.55 99.63 99.57 99.52
Na2O+K2O9.74 9.76 9.83 9.73 10.17 4.89 4.55 5.28 4.58 5.01
Na2O/K2O1.45 1.37 1.37 1.32 1.30 1.22 1.40 1.33 1.36 1.55
A/CNK0.91 0.88 0.91 0.89 0.89 0.69 0.69 0.73 0.73 0.81
A/NK1.09 1.09 1.07 1.07 1.03 2.18 2.27 1.98 2.33 2.14
Mg#19.47 18.71 8.70 8.53 9.87 48.86 49.52 49.70 50.64 49.87
σ3.43 3.47 3.51 3.38 3.69 2.21 1.87 2.66 2.12 2.40
Trace element (ppm)
Li10.65 7.67 9.61 13.99 11.02 13.78 14.88 18.70 13.22 20.49
Be2.39 2.14 2.39 3.66 2.50 1.43 1.46 1.58 1.42 1.72
Sc4.27 4.76 4.80 6.13 5.02 16.83 17.70 16.61 16.63 19.45
V50.74 62.72 68.93 86.11 72.87 127.80 131.90 136.12 125.64 149.63
Cr16.55 14.66 14.27 17.56 14.32 399.61 422.81 371.57 394.77 453.94
Co7.36 9.27 8.99 9.42 7.68 38.16 42.02 37.73 38.77 45.57
Ni7.72 6.48 5.71 5.93 6.54 221.52 241.79 190.56 223.76 234.77
Cu8.90 8.66 7.96 9.91 7.00 17.60 12.05 27.45 10.36 27.63
Zn52.68 53.45 56.29 67.53 56.73 67.51 70.48 90.88 68.07 96.83
Ga15.43 16.34 17.41 24.37 17.26 14.91 15.13 15.69 14.55 17.53
Ge0.93 0.90 0.97 1.41 0.99 1.09 1.13 1.25 1.10 1.36
Rb60.17 50.52 61.40 83.10 63.99 43.89 40.01 83.00 44.49 95.22
Sr2033.46 2635.50 2396.04 2623.93 1847.74 874.28 877.77 710.25 700.03 700.12
Y16.79 22.44 26.90 34.07 20.68 12.71 12.93 12.98 11.85 13.93
Zr20.38 22.74 44.31 30.96 24.61 124.70 131.10 134.57 123.47 153.21
Nb17.23 27.40 32.58 39.22 29.52 3.90 3.14 3.28 2.67 3.50
Mo0.16 0.24 0.25 0.31 0.18 0.32 0.26 0.93 2.70 0.83
Cd0.06 0.08 0.07 0.08 0.05 0.08 0.09 0.09 0.10 0.09
In0.02 0.03 0.03 0.04 0.03 0.04 0.04 0.04 0.03 0.04
Cs1.64 1.34 1.57 2.50 1.90 2.64 2.38 5.53 3.57 6.59
Ba4052.74 5692.39 5662.47 4370.57 4518.53 934.81 846.77 1093.28 754.99 1031.28
La78.97 86.36 91.19 186.02 77.14 17.87 17.01 16.62 14.52 17.09
Ce114.82 131.85 140.33 269.07 123.57 32.96 31.91 31.31 27.72 32.76
Pr12.41 14.29 16.07 27.96 14.41 4.28 4.17 4.06 3.70 4.30
Nd41.56 49.15 55.59 89.91 50.13 16.82 16.70 16.59 14.82 17.54
Sm5.75 7.00 7.95 11.76 7.35 3.07 3.08 2.98 2.72 3.21
Eu2.75 3.16 3.46 4.54 3.03 1.09 1.07 1.05 0.96 1.16
Gd5.77 7.07 7.92 12.28 7.19 2.85 2.89 2.85 2.67 3.08
Tb0.73 0.96 1.12 1.58 0.96 0.47 0.46 0.45 0.42 0.50
Dy3.48 4.66 5.60 7.31 4.64 2.63 2.52 2.55 2.41 2.80
Ho0.63 0.84 0.98 1.30 0.83 0.49 0.48 0.49 0.45 0.54
Er1.79 2.36 2.80 3.68 2.33 1.33 1.32 1.33 1.27 1.49
Tm0.26 0.35 0.41 0.53 0.34 0.20 0.20 0.21 0.19 0.22
Yb1.46 1.95 2.27 3.02 1.90 1.14 1.19 1.14 1.08 1.26
Lu0.25 0.32 0.40 0.51 0.32 0.20 0.20 0.20 0.19 0.22
Hf1.07 1.23 1.43 1.68 1.38 4.44 4.48 5.30 4.83 6.06
Ta1.18 1.83 2.18 2.62 1.97 0.23 0.19 0.20 0.17 0.21
Pb33.01 28.20 39.50 58.09 42.11 11.89 11.03 14.40 10.39 14.90
Th8.76 11.61 10.47 28.67 8.29 5.78 6.06 5.75 5.48 6.25
U1.30 1.40 1.84 2.59 1.53 1.73 1.73 1.85 1.60 1.95
ΣREE270.63 310.32 336.07 619.48 294.12 85.40 83.20 81.83 73.13 86.18
LREE256.26 291.81 314.59 589.27 275.64 76.10 73.95 72.61 64.45 76.07
HREE14.38 18.50 21.49 30.21 18.49 9.30 9.26 9.22 8.68 10.11
LREE/HREE17.83 15.77 14.64 19.51 14.91 8.18 7.99 7.87 7.43 7.53
δEu1.46 1.38 1.33 1.15 1.27 1.13 1.10 1.10 1.09 1.13
δCe0.90 0.92 0.90 0.91 0.91 0.92 0.93 0.93 0.93 0.94
(La/Yb)N38.78 31.71 28.80 44.14 29.19 11.21 10.27 10.41 9.67 9.71
Th/Nb0.51 0.42 0.32 0.28 0.28 1.48 1.93 1.75 2.05 1.79
LOI = loss on ignition; Mg#= 100 × (MgO/40.31)/(MgO/40.31 + 0.8998 × Fe2O3T/71.84); σ = ((K2O+Na2O) × (K2O+Na2O))/(SiO2-43); δEu = 2 × w(Eu)N/[w(Sm)N + w(Gd)N]= 2 × (Eu/0.0735)/((Sm/0.195)+ (Gd/0.259)); δCe = 2 × w(Ce)N/[w(La)N + w(Pr)N]= 2 × (Ce/0.808)/((La/0.310) + (Pr/0.122)); (La/Yb)N = (La/0.31)/(Yb/0.209).
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Yang, Z.; Zhao, Y.; Zhang, C.; Ren, C.; Yang, Q.; Zhang, L. Metallogenic Age and Tectonic Setting of the Haigou Gold Deposit in Southeast Jilin Province, NE China: Constraints from Magmatic Chronology and Geochemistry. Minerals 2025, 15, 582. https://doi.org/10.3390/min15060582

AMA Style

Yang Z, Zhao Y, Zhang C, Ren C, Yang Q, Zhang L. Metallogenic Age and Tectonic Setting of the Haigou Gold Deposit in Southeast Jilin Province, NE China: Constraints from Magmatic Chronology and Geochemistry. Minerals. 2025; 15(6):582. https://doi.org/10.3390/min15060582

Chicago/Turabian Style

Yang, Zhongjie, Yuandong Zhao, Cangjiang Zhang, Chuantao Ren, Qun Yang, and Long Zhang. 2025. "Metallogenic Age and Tectonic Setting of the Haigou Gold Deposit in Southeast Jilin Province, NE China: Constraints from Magmatic Chronology and Geochemistry" Minerals 15, no. 6: 582. https://doi.org/10.3390/min15060582

APA Style

Yang, Z., Zhao, Y., Zhang, C., Ren, C., Yang, Q., & Zhang, L. (2025). Metallogenic Age and Tectonic Setting of the Haigou Gold Deposit in Southeast Jilin Province, NE China: Constraints from Magmatic Chronology and Geochemistry. Minerals, 15(6), 582. https://doi.org/10.3390/min15060582

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