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Article

Overprinting Mineralization in the Huoluotai Porphyry Cu (Mo) Deposit, NE China: Evidence from K-Feldspar Ar-Ar Geochronology and S-Pb Isotopes

by
Yonggang Sun
1,2,
Zhongjie Yang
3,*,
Mingliang Wang
1,
Chengcheng Xie
1,
Xusheng Chen
4 and
Fanbo Meng
4
1
School of Resources and Civil Engineering, Suzhou University, Suzhou 234000, China
2
CAS Key Laboratory of Crust-Mantle Materials and Environments, School of Earth and Space Sciences, University of Science and Technology of China, Hefei 230026, China
3
Mudanjiang Natural Resources Comprehensive Survey Center, China Geological Survey, Mudanjiang 157000, China
4
Qiqihaer Institute of Geological Exploration, Qiqihar 161006, China
*
Author to whom correspondence should be addressed.
Minerals 2024, 14(9), 859; https://doi.org/10.3390/min14090859
Submission received: 25 July 2024 / Revised: 16 August 2024 / Accepted: 22 August 2024 / Published: 24 August 2024
(This article belongs to the Special Issue Genesis and Metallogeny of Non-ferrous and Precious Metal Deposits, 2nd Edition)
Browse Figures
Versions Notes

Abstract

:
The Great Xing’an Range (GXR) is a significant belt of polymetallic deposits located in the eastern segment of the Central Asian Orogenic Belt. The recently found Huoluotai porphyry Cu (Mo) deposit is situated in the northern GXR region in northeastern (NE) China. The deposit has been studied extensively using field geology and geochronological methods, which have identified two distinct mineralization events. These events include an early occurrence of porphyry-type Cu (Mo) mineralization and a later occurrence of vein-type Cu mineralization. Prior geochronology investigations have determined an approximate age of 147 Ma for the early porphyry-type Cu (Mo) mineralization. 40Ar/39Ar dating of K-feldspar of the altered Cu-mineralized quartz diorite porphyry veins for the overprinting vein-type Cu mineralization provides plateau ages of 123.1 ± 1.5 Ma, 122.3 ± 2.8 Ma, and 122.2 ± 0.4 Ma. Sulfide S-Pb isotope compositions of the two mineralization events suggest that both have a magmatic source. The origin of ore-forming metals displays the features of a crust–mantle mixing origin. The regional extensional tectonic setting in NE China during the Early Cretaceous was caused by large-scale lithosphere delamination and upwelling of the asthenospheric mantle. These processes were triggered by the rollback of the Paleo-Pacific Plate. The tectonic event in question resulted in the lithospheric thinning, significant magmatic activity, and mineralization in NE China.

1. Introduction

Polymetallic vein mineralization often occurs in close proximity to, next to, or overlapping with mineralized porphyry systems [1,2]. Multiple studies have shown a genetic connection between these veins containing base metals and porphyry Cu (Mo) mineralization [1,3,4]. Hence, the strong spatial–temporal–genetic correlation between the porphyry and the accompanying polymetallic vein mineralization offers a solid foundation for the exploration of these two types of deposits. Meanwhile, the porphyry system is a complex system involving magmatic and hydrothermal processes, and the duration covers the emplacement of upper crust magma and related thermal events, and tectonic and geodynamic processes [5]. Therefore, studying the time limit of porphyry system mineralization has become the most important task to clarify the genetic model and guide mineral exploration [1,6]. In addition, the rapid improvements in the technique and accuracy of the radioisotope dating (U-Pb, Re-Os, Ar-Ar) method, as well as its wide application in the study of ore deposits, provide the possibility for us to determine the time limit of magma-hydrothermal mineralization. Subsequently, the ore deposits of porphyry systems are classified systematically [6,7].
The Central Asian Orogenic Belt (CAOB) is the world’s largest and most complex accretionary orogenic belt, the eastern part of which is the northeastern (NE) China (Figure 1A) [8]. The Great Xing’an Range (GXR) is a significant polymetallic metallogenic belt located in the western region of NE China (Figure 1B). It is known for hosting numerous important porphyry deposits, such as Duobaoshan, Wunugetushan, and Chalukou (Figure 1C). The Huoluotai porphyry Cu (Mo) deposit is situated in the Erguna Block, which is located in the northern part of the GXR. Prior research mostly examined the geological attributes [9] and the age and geochemical composition of intrusions [9,10,11]. Based on the aforementioned studies, the Huoluotai Cu (Mo) deposit is classified as a porphyry deposit. Through thorough field mapping and core logging, we have discovered that the Huoluotai Cu (Mo) exhibits two distinct types of Cu mineralization. The granodiorite porphyry mass is the primary rock responsible for the formation of veinlet-disseminated Cu (Mo) mineralization. This rock is regarded to be a representative example of a porphyry mineralization system based on the studies mentioned above. The primary rock responsible for the formation of disseminated/veined Cu mineralization is a quartz diorite porphyry vein, which shows vein-type mineralization. This research addresses the question of whether the porphyry Cu (Mo) mineralization and vein-type mineralization are the product of a single magmatic-hydrothermal event or independent events. Furthermore, there is little information on the origin of ore-forming metals for the vein-type Cu mineralization in the Huoluotai Cu (Mo) deposit. However, S-Pb isotope testing has been shown to be an effective method for identifying the origin of ore-forming metals [12,13,14,15,16].
In order to address the aforementioned problem, this work presents a comprehensive analysis of hydrothermal K-feldspar 40Ar/39Ar dating and S-Pb isotope composition of sulfides in the Huoluotai Cu (Mo) deposit. The objective is to determine the precise ages of the overprinting Cu mineralization and understand the origin of the ore-forming metals responsible for this mineralization. The combination of our findings with previously reported molybdenite Re-Os isotope data establishes the age boundaries for the two mineralization events in the Huoluotai Cu (Mo) deposit. This finding will provide valuable guidance for mineral exploration in the GXR.

2. Regional Geology

NE China comprises a collection of micro-landmasses, namely the Erguna, Xing’an, Songnen, Jiamusi, and Khanka blocks, arranged from west to east (Figure 1B). In the Paleozoic period, NE China was influenced by the closing of the Paleo-Asian Ocean. This resulted in the merging of many micro-landmasses, such as the Songnen, Xing’an, and Erguna blocks [18,19]. In the Mesozoic period, NE China experienced the overlapping and transformation of the Mongol–Okhotsk and Paleo-Pacific tectonic regions [18,20]. The GXR consists of the Erguna and Xing’an blocks, as well as the northern part of the Songnen Block (Figure 1B) [21]. The Erguna Block is situated between the Tayuan–Xiguitu and Mongol–Okhotsk suture zones (Figure 1B). It is an old micro-landmass with a Precambrian metamorphic crystalline basement [22]. The basement mostly consists of Precambrian metamorphic supracrustal rocks (including the Xinghuadukou, Ergunahe, and Jiageda Groups; [23,24,25]), and a small amount of Neoproterozoic granitic rocks that may be associated with the convergence/breakup of the Rodinia supercontinent (927~737 Ma; [18,26]). Fault structures in the Erguna Block are extremely developed, among which the NE-SW trending Erguna River Fault and the Derbugan Fault are the most famous, and they are also important ore-forming and ore-controlling structures of the giant metallogenic belt of precious metals and non-ferrous metals in the GXR [13]. The early Paleozoic granites in the Erguna Block are found in the Tahe and Mohe regions (Figure 1C). The Tahe granites are mostly composed of calc-alkaline and high-K calc-alkaline series, while the Mohe granites are classified as high-K calc-alkaline series [18,27,28,29,30]. The Erguna Block has significant Mesozoic magmatic activity and is characterized by abundant Mesozoic volcanic rocks and granites, which could be attributed to the impact of the Mongol–Okhotsk and Paleo-Pacific tectonic regions [20].

3. Ore Deposit Geology

The Huoluotai porphyry Cu (Mo) deposit is situated about 50 km to the southwest of Mohe City in Heilongjiang Province (Figure 1C). The NNW-striking Huoluotai River Fault is distributed in the northeastern part of the Huoluotai ore district (Figure 2A). There are multiple periods of magmatic rocks in the district (Figure 2). These rocks, listed in order of their formation age from earliest to latest, include medium- to fine-grained monzogranite (Early Jurassic; about 180 Ma), granodiorite porphyry (Late Jurassic; about 149 Ma), diorite porphyry (Late Jurassic–Early Cretaceous; about 146 Ma), and granite porphyry dikes (Early Cretaceous; about 142 Ma) (Figure 2) [15]. The granodiorite porphyry is recognized as the primary rock that contains the Cu (Mo) mineralization and is strongly linked to the hydrothermal alteration associated with the deposit (Figure 2B).
The Huoluotai ore district has two distinct types of Cu mineralization. Initially, the early formation of porphyry Cu (Mo) mineralization occurs in granodiorite porphyry. Furthermore, there is a subsequent occurrence of vein-type Cu mineralization in the quartz diorite porphyry. The alteration in porphyry Cu (Mo) mineralization in the Huoluotai Cu (Mo) deposit may be categorized, in chronological order, as potassic, chlorite–epidote, and phyllic alteration. The zones of alteration, progressing from the center to the margin, are the potassic alteration zone and the phyllic alteration zone (Figure 2B). Porphyry Cu (Mo) mineralization is found in the form of stockworks, veinlets, and disseminations within the potassic and phyllic alteration zones around the granodiorite porphyry (Figure 2B). Recent drilling has shown the presence of vein-type Cu mineralization in many quartz diorite porphyry dikes. The quartz diorite porphyry dikes, which were responsible for the vein-type Cu mineralization, intruded into the granodiorite porphyry (Figure 3A–C). The hydrothermal K-feldspar was extensively observed inside or in close proximity to the quartz diorite porphyry (Figure 3A–C), with localized overprinting by epidotization and carbonatization. Pyrite and chalcopyrite are the primary minerals found in the disseminated/veined mineralization (Figure 3D–G). The quartz diorite porphyry has an ash black color and a porphyritic texture (Figure 3C,H). The composition of the rock is characterized by the presence of 20%–25% phenocrysts and 75%–80% microgranular matrix. The phenocrysts are mostly formed of plagioclase (15%–20%), with smaller amounts of quartz, hornblende, and biotite (5%–10%). The matrix has a mineral composition that closely resembles that of the phenocrysts (Figure 3H).

4. Sampling and Analytical Methods

4.1. Sampling

Three K-feldspar samples (HLT-ZK18-3-1, HLT-ZK18-3-2, and HLT-ZK16-3-1) used for 40Ar/39Ar dating were collected from the K-feldspar of the altered Cu-mineralized quartz diorite porphyry dikes (Figure 3A–C). Four samples of sulfide were selected for analysis of S isotopes, whereas three samples of sulfide were chosen for analysis of Pb isotopes.

4.2. Analytical Methods

4.2.1. K-Feldspar 40Ar/39Ar Geochronology

Following crushing and cleaning procedures, all K-feldspar grains underwent meticulous handpicking under a binocular microscope. The 40Ar/39Ar dating analysis was performed using a multi-collector Thermo Fisher Scientific ARGUS VI mass spectrometer (Thermo Fisher Scientific, Bremen, Germany) at the Noble Gas Laboratory, School of Earth Sciences, University of Melbourne, Australia, achieving measurements with uncertainties < 0.1%. A comprehensive description of the analytical methods used for ARGUS VI systems is outlined by [31]. Plateau ages for the 40Ar/39Ar age spectra were determined using ISOPLOT 3.00 [32]. 40Ar/39Ar isotopic data are presented in Supplementary Material Tables S1 and S2.

4.2.2. Sulfur Isotope Analyses

Four sulfide samples underwent S isotope analysis at the Center of Analytical Laboratory in the Beijing Research Institute of Uranium Geology (ALBRIUG), China National Nuclear Corporation (Beijing, China). Samples, each over 99% pure, were mixed with cuprous oxide, ground to 200 mesh, and heated at 980 °C under a 2 × 10−2 Pa vacuum to generate SO2. This gas was frozen in vacuum for collection. Sulfur isotopes were analyzed using a Delta V Plus mass spectrometer (Thermo Fisher Scientific, Bremen, Germany), with results expressed in standard notation as deviations in parts per thousand (‰) from the sulfur isotope composition of the Vienna Cañon Diablo Troilite (V-CDT) standards, achieving precisions > 0.2‰. The sulfide reference materials were the GBW-04414 and GBW-04415 Ag sulfide standards, with δ34SV–CDT values of −0.07‰ ± 0.13‰ and 22.15‰ ± 0.14‰, respectively, determined in this study.

4.2.3. Pb Isotope Analyses

Three sulfide samples underwent Pb isotope analysis at ALBRIUG. Powder sulfide samples weighing 30–100 mg were dissolved in Teflon bombs using an ultrapure HF + HNO3 mixture, then dried. The residue was re-dissolved in an HBr + HNO3 mixture and processed through an AG 1-X8 anionic resin column for purification. Approximately 100 ng of Pb was applied onto single rhenium filaments using the silica gel method and analyzed with an ISOPROBE-T thermal ionization mass spectrometer (GV Instruments, Manchester, UK), achieving precision > 0.09%. The measured Pb isotope ratios were corrected for instrumental mass fractionation by comparing them with repeated analyses of the standard sample (NBS-981).

5. Results

5.1. 40Ar/39Ar Age of Hydrothermal K-Feldspar

The hydrothermal K-feldspar 40Ar/39Ar age spectra and inverse isochron diagrams are shown in Figure 4. Three K-feldspar samples (sample HLT-ZK18-3-1, HLT-ZK18-3-2, and HLT-ZK16-3-1) yield plateau ages of 123.1 ± 1.5 Ma, 122.3 ± 2.8 Ma, and 122.2 ± 0.4 Ma, respectively.

5.2. Sulfur Isotopes

The S isotope data of four sulfide samples from the Huoluotai Cu (Mo) deposit are provided in Table 1 and shown in Figure 5. The δ34SV–CDT values of four sulfides vary from 0.4‰ to 1.4‰, with an average of 0.9‰ (Table 1; Figure 5).

5.3. Pb Isotopes

The Pb isotope data of three sulfide samples from the Huoluotai Cu (Mo) deposit are provided in Table 2 and shown in Figure 6. The Pb isotope compositions of three sulfides show a narrow range of variance in 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb, varying from 18.1058 to 18.1068, 15.5120 to 15.5252, and 38.2265 to 38.3889, respectively.

6. Discussion

6.1. Two Mineralization Events in the Huoluotai Cu(Mo) Deposit

A previous study on the Huoluotai porphyry Cu (Mo) deposit obtained a Re-Os isochron age of 146.9 ± 2.3 Ma for six molybdenite samples, with a weighted average age of 146.8 ± 0.9 Ma [11]. The precise molybdenite Re-Os age constrains the porphyry mineralization age to be about 147 Ma. Zircon U-Pb dating for the ore-bearing granodiorite porphyry from the Huoluotai Cu (Mo) deposit has yielded a weighted mean age of 148.9 ± 0.9 Ma [11]. The molybdenite Re-Os age is in agreement with the age of the ore-bearing granodiorite porphyry (about 149 Ma). This suggests that the porphyry mineralization was most likely triggered by the granodiorite porphyry. In addition, we obtained 40Ar/39Ar plateau ages (123.1 ± 1.5 Ma, 122.3 ± 2.8 Ma, and 122.2 ± 0.4 Ma) for three hydrothermal K-feldspar samples of the altered Cu-mineralized quartz diorite porphyry veins; thus, the K-feldspar 40Ar/39Ar age indicates the overprinting mineralization age. Furthermore, the disseminated/veined Cu mineralizations are observed in the quartz diorite porphyry veins. As a consequence, the evidence above suggests a close spatial and temporal connection between the quartz diorite porphyry veins and the overprinting vein-type Cu mineralization. The geologically constrained geochronological data suggest that the deposit was the product of two independent hydrothermal events separated by up to >20 Ma.
In summary, we suggest that porphyry mineralization in the Huoluotai deposit was formed in the late Late Jurassic (similar to the Fukeshan and Xiaokelehe porphyry deposits), while vein-type mineralization occurred in the Early Cretaceous (similar to the Baoxinggou and Sandaowanzi Au deposits). The results can effectively guide mineral exploration in the GXR polymetallic metallogenic belt.

6.2. Origin of Ore-Forming Metals

The S isotope compositions of the porphyry and vein-type mineralization are similar (Figure 5); both fall within the range of sulfur produced from the magmatic source and are comparable to the sulfur values originating from the mantle source (Figure 5) [34]. The Pb isotope compositions of the porphyry and vein-type mineralization in the Huoluotai Cu (Mo) deposit vary within a narrow range, suggesting that they share a common Pb source. In the 206Pb/204Pb vs. 207Pb/204Pb diagram (Figure 6A), the Pb isotope data for the sulfide samples from the porphyry and vein-type mineralization are graphed in proximity to the mid-ocean ridge basalt (MORB) area, between the evolution curves representing mantle and orogen. In the 206Pb/204Pb vs. 208Pb/204Pb diagram (Figure 6B), the Pb isotope data are exhibited within the range of the orogen and upper crust evolution curves, which are close to the mantle evolution curve. This indicates that the data exhibit the features of a crust–mantle mixing origin.

6.3. Late Early Cretaceous Tectonic Setting and Mineralization Events

Late Early Cretaceous A-type granite/rhyolite [37,38], metamorphic core complex [39,40], and many bimodal magmatic rock assemblages [20,41] are widely developed in NE China. Therefore, NE China was in an extensional setting in the late Early Cretaceous [42,43,44]. However, the geodynamic mechanism of extensional settings remains controversial. There are mainly three viewpoints: (1) Lithospheric extension caused by the closure of the Mongol–Okhotsk Ocean [45,46]. (2) Large-scale lithosphere delamination caused by the westward subduction of the Paleo-Pacific Plate [43,47,48]. (3) The combined effects of the closure of the Mongol–Okhotsk Ocean and the subduction of the Paleo-Pacific Plate [18,49,50]. If the rocks in the GXR from the late Early Cretaceous are considered products of the post-orogenic effects following the closure of the Mongol–Okhotsk Ocean, it is difficult to explain why these rocks are oriented NNE, clearly differing from the orientation of the Mongol–Okhotsk suture zone (Figure 7). Furthermore, the influence of the Mongol-Okhotsk regime ceased during the early Early Cretaceous [51]. Late Early Cretaceous magmatic rocks (133~106 Ma) are widely distributed across NE China (Figure 7), which is difficult to explain by the thickened crustal collapse caused by the closure of the Mongol–Okhotsk Ocean. A suite of late Early Cretaceous calc-alkaline volcanic rocks was formed in the eastern part of the Jilin and Heilongjiang provinces, NE China [52], reflecting the subduction of the Paleo-Pacific Plate [48]. Therefore, the formation of the late Early Cretaceous magmatic rocks in NE China should be more closely linked to the subduction of the Paleo-Pacific Plate.
The westward subduction of the Paleo-Pacific Plate formed a Jurassic arc magmatic belt approximately 1000 to 1500 km wide (extending from the trench westward into the continental interior) across NE China and the North China Craton, likely resulting from the flat subduction of the Paleo-Pacific Plate during the Jurassic [42,53,54,55]. The pattern of progressively younger magmatic activity peaks from NW to SE in NE China during the Early Cretaceous clearly supports the rollback of the Paleo-Pacific Plate [37,56,57]. The rollback of the Paleo-Pacific Plate likely occurred after about 140 Ma [4,37], possibly related to a shift in the subduction direction of the plate around about 140 Ma to NNW [58,59]. The unique subduction process of the Paleo-Pacific Plate exacerbated lithospheric instability, resulting in large-scale lithosphere delamination and asthenospheric mantle upwelling, which triggered lithospheric thinning [60], extensive magmatic activity, and mineralization [58,61,62]. Late Early Cretaceous mineralization events (133~106 Ma) in the GXR can occur through various mechanisms, including the replacement of original mineral systems or hydrothermal modification, as exemplified by the Huoluotai Cu (Mo) deposit. Additionally, new deposit formations can arise, such as porphyry deposits like Yili, Xing’a, and Taipinggou, epithermal and orogenic Au deposits like Shabaosi, Baoxinggou, and Sandaowanzi, or skarn Pb-Zn deposits like Luoguhe (Figure 1C). The formation of these deposits is closely associated with the temporal and spatial distribution of late Early Cretaceous magmatic rocks in NE China [4,62].

7. Conclusions

(1)
Two mineralization events were identified in the Huoluotai deposit: (a) the early porphyry-type Cu (Mo) mineralization with the potassic alteration zone and the phyllic alteration zone from the center to the margin, and (b) the late vein-type Cu mineralization.
(2)
Our results, combined with previous molybdenite Re-Os and zircon U-Pb age data, reveal that mineralization in the Huoluotai deposit comprises two magmatic-hydrothermal events. The porphyry Cu (Mo) mineralization was formed in the late Late Jurassic and was spatially–temporally associated with the granodiorite porphyry (148.9 ± 0.9 Ma), while the vein-type Cu mineralization occurred in the Early Cretaceous (about 122 Ma) and was associated with the quartz diorite porphyry.
(3)
Sulfide S-Pb isotope compositions of the two mineralization events suggest that both have a magmatic source. The origin of ore-forming metals displays the features of a crust–mantle mixing origin.
(4)
Late Early Cretaceous mineralization events (133~106 Ma) in the GXR were formed under an extensional setting, which were associated with large-scale lithosphere delamination and the upwelling of the asthenospheric mantle triggered by the rollback of the Paleo-Pacific Plate.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/min14090859/s1, Table S1: 40Ar/39Ar data of two hydrothermal K-feldspar samples from the Huoluotai porphyry Cu (Mo) deposit. Table S2: 40Ar/39Ar data of a hydrothermal K-feldspar sample from the Huoluotai porphyry Cu (Mo) deposit.

Author Contributions

Conceptualization, Y.S., Z.Y. and M.W.; software, Y.S., C.X. and X.C.; investigation, Y.S., Z.Y. and X.C.; data curation, Y.S., Z.Y. and C.X.; funding acquisition, Y.S., Z.Y. and M.W.; project administration, Y.S., Z.Y. and F.M.; writing—original draft preparation, Y.S., Z.Y. and C.X.; and writing—review and editing, Y.S., Z.Y. and M.W. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the National Natural Science Foundation of China (42202070, 42073059, 42372108), Outstanding Youth Project of Anhui Education Department (2022AH020084), Doctoral/post-doctoral Scientific Research Start-Up Fund Project of Suzhou University (2022BSK009, 2023BSH001), Natural Science Foundation of Jilin Province (20230101089JC), China Postdoctoral Science Foundation (2022M721305), and Natural Science Research Project of Anhui Educational Committee (Program Name: Genesis and gold enrichment process of the Hekou lode gold deposit in Wuhe area, Bengbu, Anhui Province).

Data Availability Statement

The data presented in this study are available in the article or Supplementary Material.

Conflicts of Interest

The authors declare no conflicts of interest.

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Figure 1. (A) Location of the CAOB. (B) Geological map of NE China [4]. (C) Geological map of the northern part of the GXR [17].
Figure 1. (A) Location of the CAOB. (B) Geological map of NE China [4]. (C) Geological map of the northern part of the GXR [17].
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Figure 2. (A) Geological map of the Huoluotai Cu (Mo) deposit [15]. (B) Geological section of the Huoluotai Cu (Mo) deposit [15].
Figure 2. (A) Geological map of the Huoluotai Cu (Mo) deposit [15]. (B) Geological section of the Huoluotai Cu (Mo) deposit [15].
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Figure 3. Photographs and photomicrographs of vein-type Cu mineralization and hydrothermal alteration characteristics in the Huoluotai porphyry Cu (Mo) deposit: (A–C) hydrothermal K-feldspar was extensively formed inside or in close proximity to the quartz diorite porphyry dike; (D–G) veined/disseminated chalcopyrite in the quartz diorite porphyry; (H) a photomicrograph of the quartz diorite porphyry. Abbreviations: Kfs—K-feldspar; Pl—plagioclase; Ccp—chalcopyrite; Py—pyrite.
Figure 3. Photographs and photomicrographs of vein-type Cu mineralization and hydrothermal alteration characteristics in the Huoluotai porphyry Cu (Mo) deposit: (A–C) hydrothermal K-feldspar was extensively formed inside or in close proximity to the quartz diorite porphyry dike; (D–G) veined/disseminated chalcopyrite in the quartz diorite porphyry; (H) a photomicrograph of the quartz diorite porphyry. Abbreviations: Kfs—K-feldspar; Pl—plagioclase; Ccp—chalcopyrite; Py—pyrite.
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Figure 4. 40Ar/39Ar age spectra diagrams for three hydrothermal K-feldspar samples from the Huoluotai porphyry Cu (Mo) deposit. (A) 40Ar/39Ar age spectra diagram for a hydrothermal K-feldspar sample (HLT-ZK18-3-1); (B) 40Ar/39Ar age spectra diagram for a hydrothermal K-feldspar sample (HLT-ZK18-3-2); (C) 40Ar/39Ar age spectra diagram for a hydrothermal K-feldspar sample (HLT-ZK16-3-1).
Figure 4. 40Ar/39Ar age spectra diagrams for three hydrothermal K-feldspar samples from the Huoluotai porphyry Cu (Mo) deposit. (A) 40Ar/39Ar age spectra diagram for a hydrothermal K-feldspar sample (HLT-ZK18-3-1); (B) 40Ar/39Ar age spectra diagram for a hydrothermal K-feldspar sample (HLT-ZK18-3-2); (C) 40Ar/39Ar age spectra diagram for a hydrothermal K-feldspar sample (HLT-ZK16-3-1).
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Figure 5. S isotope compositions of sulfides for vein-type Cu mineralization and porphyry Cu (Mo) mineralization of the Huoluotai Cu (Mo) deposit [15], and important S reservoirs [33,34,35].
Figure 5. S isotope compositions of sulfides for vein-type Cu mineralization and porphyry Cu (Mo) mineralization of the Huoluotai Cu (Mo) deposit [15], and important S reservoirs [33,34,35].
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Figure 6. Pb isotope compositions of sulfides for vein-type Cu mineralization and porphyry Cu (Mo) mineralization of the Huoluotai Cu (Mo) deposit [15]. (A) 206Pb/204Pb vs. 207Pb/204Pb. (B) 206Pb/204Pb vs. 208Pb/204Pb. The average growth lines are taken from [36].
Figure 6. Pb isotope compositions of sulfides for vein-type Cu mineralization and porphyry Cu (Mo) mineralization of the Huoluotai Cu (Mo) deposit [15]. (A) 206Pb/204Pb vs. 207Pb/204Pb. (B) 206Pb/204Pb vs. 208Pb/204Pb. The average growth lines are taken from [36].
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Figure 7. Distribution of late Early Cretaceous magmatic rocks in NE China [48].
Figure 7. Distribution of late Early Cretaceous magmatic rocks in NE China [48].
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Table 1. S isotope data of sulfide samples for vein-type Cu mineralization of the Huoluotai Cu (Mo) deposit.
Table 1. S isotope data of sulfide samples for vein-type Cu mineralization of the Huoluotai Cu (Mo) deposit.
Sample No.MineralSample Descriptionδ34SV–CDT (‰)
HLT-ZK18-3-S1PyritePy vein1.4
HLT-ZK18-3-S2Chalcopyritedisseminated Ccp0.4
HLT-ZK18-3-S3Chalcopyritemassive Ccp0.6
HLT-ZK18-3-S4PyritePy + Ccp vein1.2
Abbreviations: Ccp—chalcopyrite; Py—pyrite.
Table 2. Pb isotope data of sulfide samples for vein-type Cu mineralization of the Huoluotai Cu (Mo) deposit.
Table 2. Pb isotope data of sulfide samples for vein-type Cu mineralization of the Huoluotai Cu (Mo) deposit.
Sample No.MineralSample Description206Pb/204PbError207Pb/204PbError208Pb/204PbError
HLT-ZK18-3-Pb1PyritePy vein18.10620.000315.52520.000338.38890.0008
HLT-ZK18-3-Pb2Chalcopyritedisseminated Ccp18.10580.000515.51210.000438.22720.0011
HLT-ZK18-3-Pb3Chalcopyritemassive Ccp18.10680.000515.51200.000438.22650.0011
Abbreviations: Ccp—chalcopyrite; Py—pyrite.
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Sun, Y.; Yang, Z.; Wang, M.; Xie, C.; Chen, X.; Meng, F. Overprinting Mineralization in the Huoluotai Porphyry Cu (Mo) Deposit, NE China: Evidence from K-Feldspar Ar-Ar Geochronology and S-Pb Isotopes. Minerals 2024, 14, 859. https://doi.org/10.3390/min14090859

AMA Style

Sun Y, Yang Z, Wang M, Xie C, Chen X, Meng F. Overprinting Mineralization in the Huoluotai Porphyry Cu (Mo) Deposit, NE China: Evidence from K-Feldspar Ar-Ar Geochronology and S-Pb Isotopes. Minerals. 2024; 14(9):859. https://doi.org/10.3390/min14090859

Chicago/Turabian Style

Sun, Yonggang, Zhongjie Yang, Mingliang Wang, Chengcheng Xie, Xusheng Chen, and Fanbo Meng. 2024. "Overprinting Mineralization in the Huoluotai Porphyry Cu (Mo) Deposit, NE China: Evidence from K-Feldspar Ar-Ar Geochronology and S-Pb Isotopes" Minerals 14, no. 9: 859. https://doi.org/10.3390/min14090859

APA Style

Sun, Y., Yang, Z., Wang, M., Xie, C., Chen, X., & Meng, F. (2024). Overprinting Mineralization in the Huoluotai Porphyry Cu (Mo) Deposit, NE China: Evidence from K-Feldspar Ar-Ar Geochronology and S-Pb Isotopes. Minerals, 14(9), 859. https://doi.org/10.3390/min14090859

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