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Article

Zircon U–Pb Ages and Geochemistry of Granitoid in the Yuejinshan Copper–Gold Deposit, NE China: Constraints on Petrogenesis and Metallogenesis

by
Qingshuang Wang
1,2,
Yanlan Wei
3,*,
Yanchen Yang
1 and
Hu Peng
4,5
1
College of Earth Sciences, Jilin University, Changchun 130061, China
2
Shenyang Geological Survey Center of China Geological Survey, Shenyang 110034, China
3
Institute of Karst Geology, CAGS/Karst Dynamics Laboratory, MLR, Guilin 541004, China
4
School of Earth Resources, China University of Geosciences, Wuhan 430074, China
5
Liaoning Province Geology and Mineral Group Energy Geology Co., Ltd., Shenyang 110032, China
*
Author to whom correspondence should be addressed.
Minerals 2021, 11(11), 1206; https://doi.org/10.3390/min11111206
Submission received: 30 August 2021 / Revised: 3 October 2021 / Accepted: 23 October 2021 / Published: 29 October 2021
(This article belongs to the Section Mineral Geochemistry and Geochronology)
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Abstract

:
Yuejinshan copper–gold orebodies form a hydrothermal deposit located southwest of the Wandashan massif in the western Pacific oceanic tectonic regime. The orebodies are veins and lenses in granite porphyry and skarn or contact zones between these rocks. Early Cretaceous Yuejinshan magmatism provides critical evidence for regional mineralization and tectonic history. In this work, whole-rock major and trace elements and zircon U–Pb data for Yuejinshan granitic intrusions were studied to investigate the geochronological framework, petrogenesis, tectonic implications, and metallogenesis. Granodiorites are calc-alkaline and have geochemical characteristics that indicate affinities with subduction-related crust–mantle magmas derived from partial melting of a mantle wedge and subducted sediments metasomatized by subduction-related fluids. These magmas have experienced fractional crystallization and assimilated crustal materials. Granite porphyries, monzogranites, and quartz diorites are peraluminous, geochemically similar to remelted granites, and derived from partial melting of the crust. Zircon U–Pb LA-ICP-MS data and previous ages indicate that the granitoids were emplaced in the Early Cretaceous. We propose that mineralization mainly occurred at 130 Ma, while magmatism during 116–109 Ma triggered the enrichment of copper and gold in this deposit. Magmatism of different geological ages overlapped spatially and formed the Yuejinshan copper–gold deposit in an active continental margin setting related to the subduction of the Paleo-Pacific Plate.

1. Introduction

NE China is located between the Siberian, North China, and Pacific plates. It is an important portion of the eastern section of the Central Asian Orogenic Belt (CAOB) and records the Phanerozoic collision of microcontinental massifs and terranes [1,2,3,4]. NE China played a key role in the crustal evolution and collisional tectonics of the eastern margin of the Eurasian continent. From west to east, this region consists tectonically of the Argun, Xing’an, Songnen–Zhangguangcai, Jiamusi, Xingkai, and Wandashan massifs [2,5,6,7,8]. These massifs are separated by major faults [3,7,8,9,10].
As an important tectonic unit of the CAOB, the Wandashan massif, formerly known as the Nadanhada Range [11,12,13,14], is situated at the boundary of Russian Far East and Northeast China. This massif neighbors the Bureya–Jiamusi massif in the west, the Xingkai massif in the south, Russia’s Amurian tectonic belt in the north, and Sikhote-Alin terrane in the east (Figure 1a). In addition, the Wandashan massif is the exposed part of the Sikhote-Alin superterrane in China. The Wandashan massif is characterized by the most extensive Mesozoic marine strata in East China. As a key area for understanding the processes of paleo-Pacific subduction and accretion since the Mesozoic, the Wandashan massif has attracted much attention from scholars in China and abroad [8,11,12,13,14,15,16,17,18,19,20]. The massif began to drift at high speed from near the equator toward high latitudes in the Late Triassic epoch. After this time, it was located at the eastern edge of the Jiamusi massif in the middle of the Late Jurassic epoch and went through subduction and combination before the middle of the Early Cretaceous epoch (130 Ma) [15,18,19,20,21,22]. The Yanshanian period magmatism in the Wandashan massif resulted in a series of key gold and copper deposits, including the Yuejinshan copper–gold deposit, the Xianfengbeishan gold deposit, the Sipingshan gold deposit, and the 258 highland gold deposit. Moreover, ore genesis can be divided into skarn, volcanic hydrothermal, moderate- to low-temperature hydrothermal, and hot spring types (Figure 1b).
The Yuejinshan copper–gold ore deposit is located in the southwestern Wandashan massif as a small polymetallic deposit discovered in the 1950s (Figure 1b). Numerous previous studies have examined the metallogenic systems, metallogenic epochs, geophysics, and geological–geochemical characteristics [23,24]. However, the relationship between magmatism and metallogenesis, the timing of formation, the magmatic origin, and the tectonic setting of the Yuejinshan copper–gold deposit remains unclear, restricting understanding of the metallogenic theory of the deposit and thus affecting regional prospecting work to a certain extent.
This paper presents new whole-rock geochemical data, laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS) zircon U–Pb dating, and petrologic observations on the granitoids with the aim of constraining their petrogenesis and magmatic source and improving our understanding of the geodynamic setting of the Paleo-Pacific plate.
Minerals 11 01206 g001 550
Figure 1. (a) Tectonic subdivisions of Northeast (NE) China (modified from Wilde et al., 2000; Wu et al., 2007b) [25]. (b) Detailed geological map of the Wandashan area.
Figure 1. (a) Tectonic subdivisions of Northeast (NE) China (modified from Wilde et al., 2000; Wu et al., 2007b) [25]. (b) Detailed geological map of the Wandashan area.
Minerals 11 01206 g001

2. Geological Setting

Located in the southwestern Wandashan massif, the exposed strata in the Yuejinshan copper–gold ore deposit mainly include mudstone, siliceous rock, and siliceous slate in the Dababeishan strata as well as siliceous rock, siltstone, and siliceous slate in the upper Triassic Dajiahe Formation; upper Triassic–lower Jurassic graywacke as well as mudstone mixed with mafic-ultramafic rocks in the Dalingqiao strata; lower Cretaceous rhyolite porphyry, andesitic porphyry, and siltstone in the Dongdaling strata; and finally, Quaternary slide rocks and alluvial deposits. In addition, magmatic rocks in this region are mainly Early Cretaceous granodiorite, monzogranite, granite porphyry, quartz diorite, and south–north-trending mafic-ultramafic rock. Faults and folds have also developed in this region, mainly the Raohe anticlinorium, NE-trending Mishan–Dunhua fault, Dahezhen fault, and their derivative NW-trending, NE-trending, and E–W-trending intercrustal fault bundles. The Dahezhen fault is a class A structure and controls distribution of the intrusive rocks in the area. In addition, the deposit has mainly developed NW-trending and NE-trending transtensional fractures.
Three NW-trending mineralized zones have been outlined in the Yuejinshan copper–gold ore deposit. In addition, the distribution of orebodies (mineralization) is controlled by NW-trending faults. Current explorations focus on the northern section of mine Ⅰ in the northeastern zone, and two copper orebodies and one gold orebody have been found. The copper orebodies are in the granite porphyry and skarn with a length of 200 m, vertical depth of 165 m, and thickness of 4.49 m. For the gold orebody in the granite porphyry, the length is 100 m, and the average thickness is 3 m. In addition, the grade is 1.37% for copper and 3.87 g/t for gold.

3. Sample Descriptions

The samples for our study were collected from the Yuejinshan copper–gold deposit area in the southwestern Wandashan massif (Figure 2). The rock types included granodiorite, granite porphyry, monzogranite, and quartz diorite. The sampling locations are shown in Figure 2, and representative photomicrographs are shown in Figure 3. The granodiorites were off-white in color, had a massive structure, and were medium- to fine-grained. Under the microscope, the granodiorite samples contained 25% quartz, 20% alkali feldspar, 30% plagioclase, and 15% biotite, with apatite and epidote as accessory minerals. Chlorite in biotite is an alteration product (Figure 3b). The granite porphyry samples collected for analysis consisted of 17% phenocrysts and 83% matrix. The phenocrysts were fine-grained (0.5–1.5 mm) and metasomatized with narrow reaction edges. Locally visible alkaline feldspar and metasomatic quartz formed the micrographic structure, and the phenocrysts consisted of 5% quartz, 6% plagioclase, 4% potassium feldspar, and 2% biotite. Sericitization occurred in plagioclase, and chloritization occurred in biotite. The matrix was composed of quartz, plagioclase, and potassium feldspar (Figure 3a). The monzogranites were medium- to fine-grained, light red in color, and contained up to 40–45% quartz, 20–25% plagioclase, 20% alkali feldspar, and 5–20% biotite (Figure 3c). The quartz diorites had porphyritic texture, were ash black in color, and mainly consisted of feldspar (>50%), 10–15% quartz, and 3–5% mafic minerals. The feldspar was mainly plagioclase, and clayization and sericitization had occurred (Figure 3d).

4. Analytical Methods

4.1. Zircon U–Pb Dating

Zircons were isolated from crushed granodiorite (samples YJS-2-N and 0203-NLY), granite porphyry (samples YJS-1-N, YJS-1, and YJS-2), monzogranite (sample YJS-3-N), and quartz diorite (YJS-4-N) using combined magnetic and heavy liquid separation techniques at the Geological Laboratory of the Regional Geological Survey, Langfang City, Hebei Province, China. The zircon grains were examined under transmitted and reflected light using an optical microscope. In order to reveal their internal structures, cathodoluminescence (CL) images were obtained using a JEOL scanning electron microscope housed at the State Key Laboratory of Continental Dynamics, Northwest University, China. Distinct domains within the zircons were selected for analysis based on their CL images. An Agilent 7500a ICP-MS equipped with a 193 nm laser was used. In the experiment, high-purity He was used as the carrier gas of the ablated substance, the laser operating frequency was 10 Hz, the laser spot diameter at the test point was 36 μm, and the effective acquisition time of the mass spectrometer was 45 s.
U–Pb isotope fractionation uses the international standard zircon 91500 as the external correction and TEM (416 ± 5Ma) and QH (160 ± 1Ma) as monitoring standards. Samples housed at the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences (Wuhan) (YJS-1-N, YJS-2-N, YJS-3-N, and YJS-4-N); the State Key Laboratory of Continental Dynamics, Northwest University, China (YJS-2); and the Isotope Geology Laboratory of Tianjin Geological Survey Center, CGS(YJS-1 and 0203-NLY) were used to measure the U–Pb ages of zircons. The ICP-MS DataCal (Ver. 6.7) [26] and Isoplot (Ver. 3.0) [27] programs were used for data reduction. The correction for common Pb was made following Anderson (2002). The dating results are presented in Table 1.

4.2. Major and Trace Element Analysis

After petrographic examination and removal of altered surfaces, the samples for whole-rock analysis were crushed in an agate mill to 200 mesh. X-ray fluorescence (XRF; Rigaku RIX 2100 spectrometer) using fused glass disks and ICP-MS (Agilent 7500a with a shield torch) were used to measure the major and trace element compositions, respectively, at the State Key Laboratory of Continental Dynamics, Northwest University, China, and ALS Minerals (ALS Chemex) after acid digestion of samples in Teflon bombs. The analytical precision was better than 5% for major elements and often better than 10% for trace elements [28]. The detailed analytical procedures for major element analysis by XRF are described in [29], while those for trace element analysis by ICP-MS are described in [30]. The results of the analyses for major and trace elements are listed in Table 2.

5. Analytical Results

5.1. Zircon U–Pb Ages

In this study, two granodiorite samples (YJS-2-N and 0203-NLY) from the western Yuejinshan Cu–Au deposits, three granite porphyry samples (YJS-1-N, YJS-1 and YJS-2) from the northern mineralized zone I, one monzogranite sample (YJS-3-N), and one quartz diorite sample (YJS-4-N) from the dike that crosses the granite porphyry were chosen for LA-ICP-MS U–Pb zircon dating. The CL images of representative zircon are shown in Figure 4, and the U–Pb data are listed in Table 1 and plotted in Figure 5.
Zircons from granodiorite (YJS-2-N and 0203-NLY) are idiomorphic to hypidiomorphic and form long columnar crystals. Most zircons are 100–200 μm long and display fine-scale oscillatory growth zoning (Figure 4), indicating a magmatic origin [31,32,33]. The 206Pb/238U ages of 20 analytical spots in sample YJS-2-N, which ranged from 122 ± 2 to 141 ± 2 Ma (Table 1), showed two age populations with weighted mean ages of 141 ± 2 and 126.3 ± 1.8 Ma (mean square weighted deviation (MSWD) = 3.1, n = 17; Figure 5a). The latter age (126.8 ± 1.8 Ma) was interpreted as the crystallization age of the granodiorite, whereas the former age (141 ± 2 Ma) was interpreted as the crystallization age of inherited or captured zircons entrained in the granodiorite. In addition, 20 spots analyzed on 20 zircon grains from a second sample of granodiorite (0203-NLY) yielded ages of 122 ± 1 to 133 ± 1 Ma (Table 1) and a weighted mean 206Pb/238U age of 128.73 ± 0.69 Ma (MSWD = 2.8; n = 16; Figure 5b), which was interpreted as the crystallization age of the granodiorite.
Most of the zircons from three representative granite porphyry samples were translucent and euhedral to subhedral (Figure 4). They ranged in size from 20 to 200 μm and showed oscillatory zoning (Figure 4). The Th/U ratios of the analyzed spots were greater than 0.1. All of these features suggest a magmatic origin for the zircons [31,32,33,34,35]. U–Pb dating by LA-ICP-MS of zircons from granite porphyry samples was carried out consecutively in 2013 (YJS-2), 2014 (YJS-1), and 2015 (YJS-1-N). A total of 20 analyses of the sample YJS-2 were not near the concordia line (Figure 5c) and ranged from 106 ± 2 to 128 ± 2 Ma (Table 1). The 206Pb/238U ages of 20 analytical spots in sample YJS-2 were irregular and showed approximately two age populations with weighted mean ages of 111.8 ± 2.9 (MSWD = 3.2, n = 12; Figure 5c) and 123.6 ± 3.4 (MSWD = 1.8, n = 5; Figure 5c) Ma, which were inaccurately interpreted as the crystallization age of the granite porphyry. Therefore, we resampled the granite porphyry samples for U–Pb dating by LA-ICP-MS in different laboratories. The results were as follows. A total of 20 analyses obtained from 20 zircon grains in granite porphyry sample YJS-1 yielded ages of 106 ± 1 to 114 ± 2 Ma (Table 1) and a weighted mean 206Pb/238U age of 109.17 ± 0.91 Ma (MSWD = 2.7, n = 20; Figure 5d), which was interpreted as the crystallization age of the granite porphyry. The 206Pb/238U ages of 21 analytical spots on 21 zircon grains (YJS-1-N) ranged from 108 ± 3 to 124 ± 3 Ma (Table 1) and had a weighted mean 206Pb/238U age of 115.8 ± 1.1 Ma (MSWD = 1.11; n = 21; Figure 5e), which was interpreted as the crystallization age of the granite porphyry.
Most zircons from the monzogranite (YJS-3-N) were subhedral to euhedral or formed long irregular columns with grain sizes of 120–200 μm and length-to-width ratios of 2:1 to 3:1. They displayed fine-scale oscillatory zoning in CL images (Figure 4). The Th/U ratios of the analyzed spots were 0.38–0.88. All of these features indicate a magmatic origin for the zircons [31,32,33]. From 19 analytical spots, the monzogranite sample YJS-3-N yielded 206Pb/238U ages of 108 ± 2 to 130 ± 3 Ma (Table 1) with age populations of 114.7 ± 1.4 (MSWD = 3.1, n = 18) and 130 ± 3 (n = 1; Figure 5f) Ma. Again, the latter age (114.7 ± 1.4 Ma) was interpreted as the time of crystallization of the monzogranites, and the former age (130 ± 3 Ma) was interpreted as the crystallization age of the inherited or captured zircons entrained in the monzogranites, consistent with the age of granodiorite (YJS-2-N and 0203-NLY).
Zircons from the quartz diorite sample (YJS-4-N) were translucent and euhedral to subhedral or formed short prisms to long columns (Figure 4). They ranged in size from 50 to 250 μm, had length-to-width ratios of 1:1 to 4.5:1, and displayed fine-scale oscillatory growth zoning (Figure 3). The contents of Th and U were 187.73 to 2830.67 ppm and 391.22 to 2923.92 ppm, respectively. The Th/U ratios of the analyzed spots were greater than 0.1, indicating a magmatic origin [31,32,33]. The quartz diorite sample YJS-4-N yielded 206Pb/238U ages of 110 ± 4 to 791 ± 12 Ma (Table 1). Four age populations, namely 116.0 ± 1.3 (MSWD = 1.2, n = 16; Figure 5h), 191.7 ± 2.9 (MSWD = 0.79, n = 5; Figure 5h), 512 ± 8 (n = 1), and 791 ± 12 (n = 1, Figure 5g) Ma, were identified. The youngest age of 116.0 ± 1.3 Ma represented the time of crystallization of the quartz diorite. The other three spots yielded concordia ages of 791 ± 12, 512 ± 8, and 191.7 ± 2.9 Ma, representing the crystallization ages of xenocrystic zircons in the quartz diorite.
The results of the LA-ICP-MS zircon U–Pb dating provided crystallization ages for these granitoids as Early Cretaceous (130–127 and 116–109 Ma). In addition, the inherited zircon ages were 130, 191, 512, and 791 Ma, indicating the presence of intermittent magmatic activity in the Yuejinshan area.

5.2. Whole-Rock Geochemistry

The whole-rock major and trace element data are listed in Table 2.
The calc-alkaline granodiorites were metaluminous to weakly peraluminous (Figure 6a,b) and had high SiO2 (68.50–70.30 wt%) and Al2O3 (14.65–15.93 wt%) but low CaO (1.98–3.66 wt%) and MgO (0.98–1.54 wt%), with K2O = 2.51–2.89 wt% and Na2O = 3.56–4.52 wt%. They belonged to the subalkalic series (Figure 7). The total rare earth elements (REEs) ranged from 174.67 to 391.72 ppm. The samples had fractionated light REE (LREE) patterns, showed enrichment in LREEs relative to heavy REEs (HREEs) ((La/Yb)N = 27.97–67.08; Figure 8a), and had negative Eu anomalies (δEu = 0.54–0.88). Furthermore, the granodiorites were uniformly enriched in large ion lithophile elements (LILEs) and high field strength elements (HFSEs) and relatively depleted in Sr, Nb, and P (Figure 8b).
The granite porphyries resulted in peraluminous on the A/CNK–A/NK diagram (Figure 6b). They were part of the high-potassium calc-alkaline series on the SiO2–K2O diagram (Figure 6a) and belonged to the subalkalic series on the total alkali–silica (TAS) diagram (Figure 7). These rocks had high SiO2 = 69.60–78.03 wt% and Al2O3 = 12.34–14.00 wt%, total Fe2O3 (TFe2O3) = 0.83–3.64 wt%, Na2O = 3.22–4.40 wt%, K2O = 2.56–4.20 wt%, CaO = 0.60–2.45 wt%, and MgO = 0.08–1.30 wt%. In a chondrite-normalized REE diagram (Figure 8a), the granite porphyries displayed clear LREE enrichments and were depleted in HREEs, with LREE/HREE = 6.05–9.58, (La/Yb)N = 5.49–10.31, and moderate negative Eu anomalies (δEu = 0.20–0.52). In the primitive mantle-normalized trace element diagram (Figure 8b), the rocks were enriched in LILEs and depleted in HFSEs. In addition, due to the large amount of apatite in the samples containing phosphorus, the rocks were heavily depleted in P. Similarly, the quartz diorites were part of the peraluminous calc-alkaline series (Figure 6a,b). They had intermediate SiO2 concentrations (57.60–68.10 wt%), with Al2O3 = 15.15–19.40 wt%, Na2O = 3.90–6.83 wt%, K2O = 1.67–2.29 wt%, TFe2O3 = 1.28–1.3 wt%, CaO = 2.55–3.98 wt%, and MgO = 0.98–1.74 wt%.
They were relatively enriched in LREEs and depleted in HREEs ((La/Yb)N = 8.00-11.35)), and they showed negative Eu anomalies (δEu = 0.45–0.77; Figure 8a). Furthermore, the calc-alkaline andesites were relatively enriched in LILEs and HFSEs and relatively depleted in Sr and P (Figure 8b).
The monzogranites were high-potassium calc-alkaline (Figure 6a,b) and metaluminous rocks with A/NK >1.0 and A/CNK <1.0. They had high SiO2 (76.81–77.24 wt%), Na2O (3.96–4.06 wt%), and K2O (3.88–3.90 wt%) but low TFe2O3 (1.28–1.3 wt%). They showed relative enrichment in LREEs and depletion in HREEs (Figure 8a), with (La/Yb)N = 5.35–6.13 and negative Eu anomalies (δEu = 0.28–0.32). They were relatively enriched in LILEs and depleted in HFSEs (Figure 8b).

6. Discussion

6.1. Ages of Granitoid Magmatism and Mineralization in the Yuejinshan Deposit

The Yuejinshan copper–gold mineralization is mainly controlled by faults oriented NW, and the orebodies mainly occur in the skarn, the granite porphyry, and the contact sites between the skarn and granite porphyry. Spatially, the orebodies are related to the generation of granite porphyry and create porphyritic copper–gold deposits and skarn-type copper deposits. Therefore, the chronological study of granitic intrusions in mining areas can effectively restrict the metallogenetic events.
In the last decade, major advancement has been accomplished in the geochronology of granitoids in the Wandashan massif. The authors of [39] reported that the thermal ionization mass spectrometry (TIMS) U–Pb age of the granitoids in Hamahe was 115 ± 1.5 Ma. In 1995, they found that the age of syenite granite and alkali feldspar granite in Yuejinshan was 116.6–99.5 Ma. In 2006, Cheng found the LA-ICP-MS zircon U–Pb data showed the ages of the biotite granodiorites in Hamahe were 114 ± 1, 116 ± 1, and 124 ± 0.4 Ma; the cordierite granodiorite was 124 ± 0.4 Ma; the syenite granite in Taipingcun was 111 ± 1 Ma; and the cordierite alkali feldspar granite was 114 ± 1 Ma [40]. Three granitic magmatic events occurred at 115, 124, and 131 Ma during the Early Cretaceous period, and 124 Ma was the peak of the granitic intrusions in Raohe. The zircon U–Pb ages of the granite diorite and the quartz diorite porphyry in Xianfengbeishan were 128 and 113 Ma, respectively, [41]; the granitoids in Hamahe were dated within the range of 130–118 Ma [42], the granitoids in Taipingcun was 128–110 Ma [25,43], and the granite in Yuejinshan was 126–116 Ma [24].
In the present study, our new zircon U–Pb age data indicated two stages of granitic magmatism in the Yuejinshan area, with one occurring from 130 to 127 Ma and the other from 116 to 109 Ma, whereas the Early Cretaceous magmatism formed the Jianshanzi plutons. The inherited magmatic zircons in the granitoids, which yielded ages of 791, 512, and 191 Ma, were consistent with the age of the ancient crust of the Jiamusi crustal block during the Precambrian (700 Ma) [8], advanced metamorphism and magmatism during the Paleozoic Era (500 Ma) [25,44,45,46,47,48], and a magmatic arc during the Permian Period (250 Ma) [48,49,50,51,52,53,54], indicating that three earlier magmatic events in the Precambrian, Cambrian, and Early Jurassic occurred in the Wandashan massif.
Previous research results have shown that the metallogenesis of magmatic hydrothermal deposits in the east of the CAOB mainly occurred in six metallogenetic periods, namely 510–473, 373–330, 320–253, 250–210, 210–127, and 155–100 Ma [55]. The large-scale metallogenesis in northern China took place during three peak periods, namely 200–160, approximately 140, and approximately 120 Ma [56,57]. The large-scale Mesozoic metallogenesis in East China occurred in the Middle–Late Jurassic to Early Cretaceous (165 ± 5 to 135 Ma) and from the late Early Cretaceous to the early Late Cretaceous (135–80 Ma) [56,57]. Two metallogenic events occurred at 195–165 and 115–110 Ma in the eastern section of the Xingmeng orogenic belt [58], and three stages of mineralization occurred in Northeast China, namely 170–160, 130–110, and 110–90 Ma [59]. Based on the new zircon U–Pb data and regional geological investigations, we propose that the main mineralization event took place at 130–127 Ma. Moreover, the magmatism during 116–109 Ma enriched the copper and gold elements in the Yuejinshan copper–gold deposit. Together with the metallogenesis ages from deposits obtained in the Wandashan massif by other researchers [23,42,60,61,62], these findings indicate that two major metallogenetic events occurred at 130–127 and 117–109 Ma in the Wandashan massif.

6.2. Petrogenesis and Magma Source of the Early Cretaceous Granitoids

Regarding the origin of the granitoids, several models have been proposed: (1) fractional crystallization from mantle-derived magma [63], (2) magmatic migmatization [64], (3) partial melting of crustal rocks [65,66,67,68], and (4) origin from a deep crustal hot zone [69,70,71,72].
The granitic intrusions in Yuejinshan consist of a rock association of quartz diotite, granodiorite, monzogranite, and granite porphyry. The Yuejinshan granitoids have distinct and heterogeneous geochemical compositions (Table 2 and Figure 9), implying that they probably formed from various sources or by different petrogenetic processes.
The granodiorites showed enrichment in LREEs relative to HREEs; were enriched in LILEs and HFSEs and relatively depleted in Sr, Nb, and P; and had negative Eu anomalies. They exhibited trace element signatures attributed to subduction. The test results revealed that the average value of Nb/Ta was 12.13, which is much lower than the average value of 17.5 for original crust but similar to the Nb/Ta value of crustal magma (11–12) [73]. The average value of Rb/Nb was 7.77, which is higher than the average value of the Earth’s crust (4.5) [73]. Rb/Sr was 0.24–0.27, which is higher than the average value of the upper mantle (0.034) but similar to the average value of the crust (0.3) [73], indicating that some crustal material were involved. The average Zr/Hf value was 30.39, which is similar to the average value of the original mantle (36.27) but far higher than the average value of the continental crust (11), implying mantle-derived magma-derived characteristics [73]. The Zr/Nb average value was 13.38, which is similar to the average value of the original mantle (14.8) but much lower than the average value of the continental crust (16.2) [74,75]. Ba/Th was 24.34–53.41, with an average value of 40.92, which is far below the average value of the continental crust (124) [74,75]. The Ba/La average value was 11.66, which is similar to the average value of the original mantle (9.6) but far lower than the average value of the continental crust (25) [74,75], indicating that the granodiorites were derived from mixing of mantle- and crust-derived magmas. Th/Ce was 0.14–0.16, which is higher than the values for mid-ocean ridge basalt (MORB, 0.016) and ocean island basalt (OIB, 0.05). This result means that subducted sediment contributed some constituents to the source [76]. The (La/Yb)N-δEu diagram (Figure 10) shows the sampling points of granodiorite plot within the crust–mantle granite area. Combining this information with Th/Ta = 10.04–29.92 and Th/Nb = 1.32–1.87 implies that the source was metasomatized by subduction-related fluid (Figure 11a,b). Therefore, we believe that the granodiorite in the Yuejinshan area was derived from the mixing of mantle- and crust-derived magmas. These granodiorite rocks were generated from the partial melting of the mantle wedge and subducted sediments caused by metasomatism from subduction-related fluids, and these magmas assimilated some amounts of crustal material.
Granite porphyry (109–115 Ma), monzogranite (114 Ma), and granodiorite (116 Ma) were the products of magmatic activity during the same period (117–110 Ma). These rocks had similar geochemical trace element characteristics, showed relative enrichment in LREEs and depletion in HREEs (Figure 8a), and were relatively enriched in LILEs and depleted in HFSEs. Sr and P were strongly deficient, implying that plagioclase and apatite were important residual phases, and both exhibited trace element signatures attributed to plagioclase and apatite fractionation [78,79]. The negative Eu anomalies indicated that feldspar remained in the magma during partial melting. Rb/Sr was 0.3–1.93, with an average value of 0.76 (>0.35, the average value of the crust [73]). These ratios were greater than the value of the original mantle (0.03), enriched MORB (E-MORB, 0.033), and OIB (0.047) and fell within the scope of crust-derived magmas (>0.5 [80]). The Zr/Hf was 19.98–36.93 and Nb/Ta was 2.07–16.55 (<37 and <17.8, the original mantle values, respectively [81]), but both ratios were approximately the crustal values (33 and 17.8, respectively [73]), exhibiting crust-derived magma signatures. In addition, these rocks had similar specific values of incompatible elements, and the values of Zr/Nb, La/Nb, Ba/Nb, Ba/Th, Rb/Nb, K/Nb, Th/Nb, Th/La, and Ba/La were considerably different from the corresponding values of the original mantle (14.8, 0.94, 9.0, 77, 0.91, 323, 0.117, 0.125, and 9.6, respectively) [74,75] but quite similar to the corresponding values of the original crust (16.2, 2.2, 54, 124, 4.7, 1341, 0.44, 0.204, and 25, respectively) [74,75], implying that they were derived from a crustal source. Th/Ce was 0.07–0.24, which indicates that the sediments were derived from a crustal source [76]. In the (La/Yb)N-δEu diagram (Figure 10), the granite porphyry, monzogranite, and granodiorite samples are plotted within the crustal granite area. All of these geochemical features, combined with the regional tectonic evolution, suggest that the granite porphyry, monzogranite, and granodiorite were derived from a crustal source, which is also supported by the occurrence of abundant inherited zircons.

6.3. Geodynamic Settings

The geochemical data presented in this study show that the Early Cretaceous granitoids, which is composed of a quartz diorite–granodiorite–monzogranite–granite porphyry association, belong to the subalkaline series (Figure 6). All the analyzed samples had high Al2O3 contents and high Na2O/K2O ratios and were enriched in LREEs and LILEs and depleted in HREEs and HFSEs (Figure 8a,b). On the Nb vs. Y and Rb vs. Y+Nb diagrams (Figure 12a,b), all of the granitoids fell in the volcanic arc granite (VAG) + syncollisional granite (Syn-COLG) and the VAG fields. On the Nb vs. Nb/Th and Ta/Yb vs. Th/Yb diagrams (Figure 12c,d), all of the granitoids were plotted in the island arc volcanic rock field and the active continental margin field. Major and trace element data suggest that the Early Cretaceous granitoids formed in an active continental margin setting [82,83].
This conclusion is also evidenced by the following observations: (1) the identical setting of the Early Cretaceous plutons and coeval alkaline volcanics in the Wandashan massif, including the 122–116 Ma contemporaneous rhyolite [60,61] and the 114–111 Ma Taipingcun and 131–115 Ma Hamahe plutons [18,24,39,40,41,42,43,48]; (2) the presence of mafic-ultramafic igneous rocks, namely the Yuejinshan complex, exposed in the Wandashan terrane between the Late Jurassic and Early Cretaceous [40,52,62,89]; and (3) the large-scale mineralization in northern China that occurred in the three peak periods of 200–160, 140, and 120 Ma with geodynamic backgrounds of postcollision orogeny, late tectonic regime transition, and large-scale rapid thinning of the lithosphere, respectively [56,57]. The time limit for mineralization in East China is 160–100 Ma, and the geodynamic background is the large-scale collapse of the lithosphere in an active continental margin setting [56,57,58,59].
Regionally, as a result of the small-angle oblique subduction of the Pacific Plate in the Mesozoic, a significant change occurred in the tectonic system in East China as the tectonic system gradually changed from a postcollisional extrusion to a postcollisional extensional setting. Thus, this change caused large-scale crust–mantle interactions. Energy and material from the depths of the Earth intruded into the shallow crust, providing significant thermal energy, fluids, and metallogenic components for mineralization [56,57,90]. The late Mesozoic (130–100 Ma) was the peak of magmatism. The thickened crust became thinner and even collapsed in a postcollisional extensional setting, causing a large number of calc-alkaline magmas to invade and erupt. Therefore, calc-alkaline granites, volcanic rocks, and a series of important mineral deposits and concentration areas are widely distributed in Northeast China [90,91].
Wandashan is located in eastern Northeast China and is the part of the Xihuote-Alin terrane that crops out and comprises ultramafic-mafic rocks, bathypelagic siliceous sediments, and ophiolite suite [11,12,92,93,94,95,96]. During the Late Jurassic, the late Indosinian movement caused the Pacific crust to approach the eastern edge of the Jiamusi massif and completed the collage in the Early Cretaceous (130 Ma). Then, the Wandashan massif entered an island arc tectonic environment [8,15,16,17,18,19,20,21,22].
In summary, we propose that the Yuejinshan copper–gold ore deposit developed along an active continental margin and was closely related to the westward subduction of the Paleo-Pacific Plate beneath the Eurasian continent (Figure 13).

7. Conclusions

Based on the zircon U–Pb ages and geochemical data presented in this study, we draw the following conclusions.
  • The main mineralization event took place at 130–127 Ma. Moreover, the magmatism during 116–109 Ma enriched the copper and gold elements in the Yuejinshan copper–gold deposit.
  • The granodiorites were derived from partial melting of mantle wedge material and upper sediments, and the granite porphyries, monzogranites, and quartz diorites were derived from the partial melting of the crust.
  • The Cretaceous granitoids and Yuejinshan copper–gold deposit formed in an active continental margin setting that was closely related to the westward subduction of the Paleo-Pacific oceanic plate.

Author Contributions

Conceptualization, Q.W.; methodology, Y.W.; software, H.P.; formal analysis, Y.Y.; investigation, Q.W. and Y.W.; data curation, H.P.; writing—original draft preparation, Q.W.; writing—review and editing, Q.W. and Y.W.; visualization, Y.W.; supervision, Y.Y. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the China Geological Survey (Grants DD20190438 and DD20201162) and Chinese Academy of Geological Science (Grants JYYWF201833 and 2002372017001).

Acknowledgments

We extend our thanks to the staff of the State Key Laboratory of Continental Dynamics, Northwest University, China; the State Key Laboratory of Geological Processes and Mineral Resources, China; University of Geosciences (Wuhan), China; and the Isotope Geology Laboratory of Tianjin Geological Survey Center, CGS for assistance during zircon LA–ICP–MS U–Pb dating. We also extend our thanks to the State Key Laboratory of Continental Dynamics, Northwest University, China, and ALS Minerals (ALS Chemex) for assistance during major and trace element analyses.

Conflicts of Interest

The authors declare no conflflict of interest.

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Minerals 11 01206 g002 550
Figure 2. Detailed geological map of the Yuejinshan copper–gold deposit area.
Figure 2. Detailed geological map of the Yuejinshan copper–gold deposit area.
Minerals 11 01206 g002
Minerals 11 01206 g003 550
Figure 3. Representative photomicrographs for the granitic intrusions in the Yuejinshan. (a)—granite porphyry; (b)—granodiorite; (c)—monzogranite; (d)—quartz diorite. Q = quartz; Pl = plagioclase; Bt = biotite; Kfs = K-feldspar; Chl = chlorite.
Figure 3. Representative photomicrographs for the granitic intrusions in the Yuejinshan. (a)—granite porphyry; (b)—granodiorite; (c)—monzogranite; (d)—quartz diorite. Q = quartz; Pl = plagioclase; Bt = biotite; Kfs = K-feldspar; Chl = chlorite.
Minerals 11 01206 g003
Minerals 11 01206 g004 550
Figure 4. Representative cathodoluminescence (CL) images of zircons from the Yurjinshan granitic intrusions. Red circles show the locations of LA-ICP-MS U–Pb analyses, and the diameter of the circles in all CL images is 26 μm in length.
Figure 4. Representative cathodoluminescence (CL) images of zircons from the Yurjinshan granitic intrusions. Red circles show the locations of LA-ICP-MS U–Pb analyses, and the diameter of the circles in all CL images is 26 μm in length.
Minerals 11 01206 g004
Minerals 11 01206 g005 550
Figure 5. Zircon LA-ICP-MS U–Pb concordia diagrams for the samples YJS-2-N (a), 0203-NLY (b), YJS-2 (c), YJS-1 (d), YJS-1-N (e), YJS-3-N (f), YJS-4-N (g,h) from Yuejinshan copper–gold deposit.
Figure 5. Zircon LA-ICP-MS U–Pb concordia diagrams for the samples YJS-2-N (a), 0203-NLY (b), YJS-2 (c), YJS-1 (d), YJS-1-N (e), YJS-3-N (f), YJS-4-N (g,h) from Yuejinshan copper–gold deposit.
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Minerals 11 01206 g006 550
Figure 6. (a) K2O versus SiO2. (b) A/NK versus A/CNK [36].
Figure 6. (a) K2O versus SiO2. (b) A/NK versus A/CNK [36].
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Minerals 11 01206 g007 550
Figure 7. Plots of total alkali versus SiO2 (TAS). The boundary lines are from [37].
Figure 7. Plots of total alkali versus SiO2 (TAS). The boundary lines are from [37].
Minerals 11 01206 g007
Minerals 11 01206 g008 550
Figure 8. Chondrite-normalized REE patterns (a) and primitive mantle (PM) normalized trace element (b) diagrams of the granitoids from Yuejinshan. The values of chondrite and PM are from [38].
Figure 8. Chondrite-normalized REE patterns (a) and primitive mantle (PM) normalized trace element (b) diagrams of the granitoids from Yuejinshan. The values of chondrite and PM are from [38].
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Minerals 11 01206 g009 550
Figure 9. SiO2-Al2O3 (a), SiO2-MgO (b), SiO2-TFe2O3 (c), SiO2-TiO2 (d), SiO2-Na2O (e), SiO2-K2O (f), SiO2-CaO (g) and SiO2-P2O5 (h) diagrams showing the magmatic evolution of the granitoids from Yuejinshan.
Figure 9. SiO2-Al2O3 (a), SiO2-MgO (b), SiO2-TFe2O3 (c), SiO2-TiO2 (d), SiO2-Na2O (e), SiO2-K2O (f), SiO2-CaO (g) and SiO2-P2O5 (h) diagrams showing the magmatic evolution of the granitoids from Yuejinshan.
Minerals 11 01206 g009
Minerals 11 01206 g010 550
Figure 10. La/Yb vs. δEu for granitoids from Yuejinshan.
Figure 10. La/Yb vs. δEu for granitoids from Yuejinshan.
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Minerals 11 01206 g011 550
Figure 11. Rb/Y vs. Nb/Y (a) and Nb/Zr vs. Th/Zr (b) for granitoids from Yuejinshan [77].
Figure 11. Rb/Y vs. Nb/Y (a) and Nb/Zr vs. Th/Zr (b) for granitoids from Yuejinshan [77].
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Minerals 11 01206 g012 550
Figure 12. Trace element–tectonic setting discrimination diagram for granitoids from Yuejinshan. (a) Nb vs. Y [84], (b) Rb vs. Y + Nb [85], (c) Nb/Th vs. Nb [86], (d) Th/Yb vs. Ta/Yb [86]. Abbreviations shown in the figure are as follows: VAG = volcanic arc granites; syn-COLG = syn-collisional granites; WPG = within-plate granites; ORG = oceanic ridge granites (in a,b); MORB = mid-ocean ridge basalts; OIB = ocean-island basalts; SZ = subduction zone; FC = fractional crystallization. Primitive mantle [87], continental crust, MORB, OIB, and arc volcanic compositions [88] in (c).
Figure 12. Trace element–tectonic setting discrimination diagram for granitoids from Yuejinshan. (a) Nb vs. Y [84], (b) Rb vs. Y + Nb [85], (c) Nb/Th vs. Nb [86], (d) Th/Yb vs. Ta/Yb [86]. Abbreviations shown in the figure are as follows: VAG = volcanic arc granites; syn-COLG = syn-collisional granites; WPG = within-plate granites; ORG = oceanic ridge granites (in a,b); MORB = mid-ocean ridge basalts; OIB = ocean-island basalts; SZ = subduction zone; FC = fractional crystallization. Primitive mantle [87], continental crust, MORB, OIB, and arc volcanic compositions [88] in (c).
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Minerals 11 01206 g013 550
Figure 13. Cross section geodynamic reconstruction showing the metallogenetic model for the Yuejinshan copper–gold deposit, southwestern Wandashan massif. See the text for detailed explanation.
Figure 13. Cross section geodynamic reconstruction showing the metallogenetic model for the Yuejinshan copper–gold deposit, southwestern Wandashan massif. See the text for detailed explanation.
Minerals 11 01206 g013
Table
Table 1. LA-ICPMS U–Pb zircon dating data of the granitoids from the Yuejinshan copper–gold deposit.
Table 1. LA-ICPMS U–Pb zircon dating data of the granitoids from the Yuejinshan copper–gold deposit.
Analysis Content (ppm) Th/U Isotopic Ratios Isotopic Ages (Ma)
PbThU 207Pb/206Pb±1𝜎207Pb/235U±1𝜎206Pb/238U±1𝜎 207Pb/206Pb±1𝜎207Pb/235U±1𝜎206Pb/238U±1𝜎Concordance
YJS-2-N-Granodiorite
YJS-2-N-01 144.52 873.77 2531.65 0.35 0.0516 0.0041 0.1497 0.0115 0.0211 0.0003 267 14210134294%
YJS-2-N-02 195.43 1238.50 3781.95 0.33 0.0499 0.0042 0.1424 0.0110 0.0207 0.0007 18919313510132598%
YJS-2-N-03 156.57 809.69 3462.02 0.23 0.0470 0.0028 0.1310 0.0076 0.0202 0.0003 491301257129297%
YJS-2-N-04 199.36 741.56 5099.89 0.15 0.0527 0.0047 0.1435 0.0121 0.0198 0.0006 31620413611126492%
YJS-2-N-05 85.76 479.59 2201.93 0.22 0.0508 0.0037 0.1341 0.0095 0.0192 0.0003 2311661289122295%
YJS-2-N-06 130.41 803.20 2265.97 0.35 0.0461 0.0028 0.1364 0.0079 0.0215 0.0004 1321307137295%
YJS-2-N-07 135.87 748.47 4061.45 0.18 0.0538 0.0029 0.1437 0.0075 0.0194 0.0003 3631261367124291%
YJS-2-N-08 158.89 1248.50 2981.19 0.42 0.0516 0.0031 0.1466 0.0083 0.0207 0.0004 265971397132295%
YJS-2-N-09 72.35 511.02 1807.78 0.28 0.0478 0.0025 0.1318 0.0067 0.0200 0.0003 87861266128298%
YJS-2-N-10 67.74 372.32 1695.24 0.22 0.0561 0.0048 0.1709 0.0142 0.0220 0.0004 45415616012141287%
YJS-2-N-11 371.81 2891.26 6918.85 0.42 0.0503 0.0023 0.1340 0.0059 0.0193 0.0002 2091071285123196%
YJS-2-N-12 146.86 707.53 2323.62 0.30 0.0472 0.0036 0.1303 0.0097 0.0200 0.0003 611691249128297%
YJS-2-N-13 135.63 756.21 3168.27 0.24 0.0509 0.0037 0.1426 0.0100 0.0203 0.0004 2371661359130296%
YJS-2-N-14 110.18 755.33 2242.62 0.34 0.0530 0.0033 0.1517 0.0093 0.0205 0.0003 3301121438131291%
YJS-2-N-15 143.12 941.83 3443.67 0.27 0.0496 0.0029 0.1358 0.0076 0.0199 0.0003 1751331297127298%
YJS-2-N-16 99.12 777.47 2501.95 0.31 0.0520 0.0029 0.1396 0.0073 0.0194 0.0003 287921336124293%
YJS-2-N-17 113.19 682.95 3084.79 0.22 0.0490 0.0020 0.1397 0.0061 0.0203 0.0003 149761335130298%
YJS-2-N-18 55.55 352.70 1677.90 0.21 0.0505 0.0027 0.1360 0.0071 0.0196 0.0004 216861306125296%
YJS-2-N-19 59.28 395.69 1502.44 0.26 0.0504 0.0038 0.1324 0.0092 0.0191 0.0004 2121221268122297%
YJS-2-N-20 105.35 747.64 2391.95 0.31 0.0503 0.0027 0.1408 0.0075 0.0202 0.0003 207941347129296%
0203-NLY-Granodiorite
0203-NLY-01 19.14 358.00 967.63 0.37 0.0480 0.0014 0.1323 0.0039 0.0200 0.0001 10169126 4 127 1 99%
0203-NLY-02 34.91 732.35 1684.53 0.43 0.0466 0.0007 0.1338 0.0021 0.0208 0.0001 2935127 2 133 1 96%
0203-NLY-03 26.77 474.44 1338.64 0.35 0.0488 0.0006 0.1364 0.0018 0.0203 0.0001 13831130 2 129 1 100%
0203-NLY-04 41.84 809.25 2022.34 0.40 0.0489 0.0006 0.1378 0.0020 0.0205 0.0001 14130131 2 131 1 100%
0203-NLY-05 28.94 604.96 1419.78 0.43 0.0495 0.0017 0.1393 0.0050 0.0204 0.0001 17381132 5 130 1 98%
0203-NLY-06 28.07 624.29 1350.95 0.46 0.0481 0.0007 0.1353 0.0020 0.0204 0.0001 10633129 2 130 1 99%
0203-NLY-07 19.92 373.97 984.92 0.38 0.0488 0.0039 0.1380 0.0111 0.0205 0.0001 138186131 11 131 1 100%
0203-NLY-08 19.66 344.32 976.01 0.35 0.0488 0.0010 0.1373 0.0029 0.0204 0.0001 13849131 3 130 1 100%
0203-NLY-09 21.16 377.25 1073.95 0.35 0.0491 0.0021 0.1365 0.0059 0.0202 0.0001 154100130 6 129 1 99%
0203-NLY-10 36.74 597.07 1843.19 0.32 0.0471 0.0008 0.1333 0.0023 0.0205 0.0001 5340127 2 131 1 97%
0203-NLY-11 28.33 477.15 1445.76 0.33 0.0489 0.0023 0.1347 0.0064 0.0200 0.0001 144112128 6 128 1 99%
0203-NLY-12 37.00 715.22 1895.01 0.38 0.0500 0.0019 0.1376 0.0054 0.0199 0.0001 19789131 5 127 1 97%
0203-NLY-13 23.27 313.86 1206.57 0.26 0.0495 0.0010 0.1358 0.0029 0.0199 0.0001 17149129 3 127 1 98%
0203-NLY-14 20.44 322.98 1100.61 0.29 0.0475 0.0009 0.1248 0.0023 0.0191 0.0001 7444119 2 122 1 98%
0203-NLY-15 21.68 431.19 1101.02 0.39 0.0497 0.0020 0.1360 0.0056 0.0198 0.0001 18192129 5 127 1 98%
0203-NLY-16 26.94 463.27 1371.75 0.34 0.0500 0.0013 0.1382 0.0038 0.0200 0.0001 19662131 4 128 1 97%
0203-NLY-17 38.12 899.60 1889.83 0.48 0.0499 0.0009 0.1378 0.0026 0.0201 0.0001 18843131 2 128 1 98%
0203-NLY-18 50.27 597.99 2571.81 0.23 0.0489 0.0007 0.1369 0.0021 0.0203 0.0001 14536130 2 129 1 99%
0203-NLY-19 29.15 97.49 1552.51 0.06 0.0491 0.0008 0.1374 0.0024 0.0203 0.0001 15440131 2 129 1 99%
0203-NLY-20 30.60 513.40 1510.69 0.34 0.0480 0.0010 0.1350 0.0028 0.0204 0.0001 10248129 3 130 1 99%
YJS-2-Granite porphyry
YJS-2-01 39.11 285.02 752.79 0.38 0.0901 0.0032 0.2227 0.0056 0.0179 0.0003 1427242045115244%
YJS-2-02 37.43 464.54 965.87 0.48 0.0476 0.0017 0.1090 0.0029 0.0166 0.0003 80331053106297%
YJS-2-03 67.93 878.31 1477.48 0.59 0.0478 0.0016 0.1196 0.0027 0.0182 0.0003 87261152116296%
YJS-2-04 45.26 506.98 1009.85 0.50 0.0625 0.0022 0.1432 0.0035 0.0166 0.0003 692261363106269%
YJS-2-05 81.41 775.99 1393.84 0.56 0.0960 0.0030 0.2381 0.0046 0.0180 0.0003 1547172174115236%
YJS-2-06 38.82 473.62 1057.60 0.45 0.0481 0.0017 0.1173 0.0029 0.0177 0.0003 106291133113297%
YJS-2-07 45.26 624.55 1112.21 0.56 0.0450 0.0018 0.1022 0.0032 0.0165 0.0003 −2133993105290%
YJS-2-08 27.97 250.68 763.49 0.33 0.0544 0.0021 0.1453 0.0043 0.0194 0.0003 386381384124286%
YJS-2-09 98.75 1474.02 2130.52 0.69 0.0457 0.0014 0.1092 0.0023 0.0173 0.0003 −19181052111287%
YJS-2-10 21.55 220.45 614.17 0.36 0.0511 0.0020 0.1229 0.0037 0.0174 0.0003 244401183111289%
YJS-2-11 31.91 366.67 852.67 0.43 0.0454 0.0017 0.1184 0.0034 0.0189 0.0003 311143121284%
YJS-2-12 89.96 1245.99 1934.48 0.64 0.0474 0.0015 0.1101 0.0024 0.0168 0.0003 69241062108288%
YJS-2-13 84.65 1209.60 1883.62 0.64 0.0452 0.0014 0.1106 0.0024 0.0177 0.0003 −9191072113299%
YJS-2-14 46.50 493.89 1343.94 0.37 0.0474 0.0016 0.1170 0.0027 0.0179 0.0003 71281122114291%
YJS-2-15 44.93 488.24 1166.88 0.42 0.0497 0.0017 0.1228 0.0031 0.0179 0.0003 181311183114289%
YJS-2-16 32.60 257.27 749.32 0.34 0.0574 0.0021 0.1585 0.0044 0.0200 0.0003 506321494128270%
YJS-2-17 37.24 374.09 988.29 0.38 0.0449 0.0016 0.1196 0.0031 0.0193 0.0003 −25241153123290%
YJS-2-18 85.95 1305.01 1825.18 0.72 0.0458 0.0014 0.1090 0.0023 0.0173 0.0003 −13181052110293%
YJS-2-19 44.54 487.23 1040.16 0.47 0.0503 0.0017 0.1245 0.0031 0.0179 0.0003 208301193115298%
YJS-2-20 52.85 651.34 1259.48 0.52 0.0477 0.0016 0.1256 0.0029 0.0191 0.0003 82271203122299%
YJS-1-Granite porphyry
YJS-1-01 5.99 358.00 2855.51 0.52 0.0478 0.0025 0.1150 0.0061 0.0174 0.0002 90 124 110.56 1111100%
YJS-1-02 4.93 732.35 462.08 0.39 0.0513 0.0028 0.1226 0.0072 0.0173 0.0002 256 127 117.47 111194%
YJS-1-03 4.86 474.44 2995.25 0.34 0.0490 0.0039 0.1169 0.0096 0.0173 0.0002 146 188 112.39 111199%
YJS-1-04 8.29 809.25 810.80 0.33 0.0493 0.0026 0.1169 0.0071 0.0172 0.0002 163 124 112.37 110198%
YJS-1-05 7.10 604.96 1761.11 0.48 0.0505 0.0024 0.1210 0.0059 0.0174 0.0002 217 109 1166 111196%
YJS-1-06 13.76 624.29 1164.35 0.41 0.0500 0.0015 0.1173 0.0036 0.0170 0.0002 197 69 112.63 109197%
YJS-1-07 11.54 373.97 1340.09 0.39 0.0487 0.0013 0.1140 0.0030 0.0170 0.0002 135 61 109.63 108199%
YJS-1-08 4.83 344.32 880.90 0.42 0.0473 0.0034 0.1167 0.0086 0.0179 0.0003 64 170 112.18 114298%
YJS-1-09 7.54 377.25 426.44 0.47 0.0499 0.0021 0.1173 0.0050 0.0170 0.0002 191 96 112.75 109197%
YJS-1-10 5.51 597.07 1013.83 0.36 0.0489 0.0023 0.1126 0.0054 0.0167 0.0002 145 111 108.35 107199%
YJS-1-11 5.06 477.15 1022.22 0.33 0.0528 0.0027 0.1231 0.0064 0.0169 0.0003 319 115 117.96 108291%
YJS-1-12 21.21 715.22 1477.75 0.72 0.0512 0.0007 0.1183 0.0016 0.0168 0.0001 249 31 113.62 107194%
YJS-1-13 3.98 313.86 960.31 0.29 0.0470 0.0033 0.1112 0.0080 0.0171 0.0003 51 168 1078 110297%
YJS-1-14 6.48 322.98 688.99 0.40 0.0504 0.0020 0.1213 0.0049 0.0175 0.0002 211 91 116.35 112196%
YJS-1-15 9.07 431.19 844.34 0.39 0.0487 0.0016 0.1156 0.0038 0.0172 0.0002 131 76 111.14 110199%
YJS-1-16 11.30 463.27 1941.62 0.43 0.0498 0.0012 0.1173 0.0030 0.0171 0.0002 187 58 112.63 109197%
YJS-1-17 12.76 899.60 776.53 0.58 0.0502 0.0012 0.1159 0.0027 0.0168 0.0002 203 54 111.43 107196%
YJS-1-18 18.44 597.99 546.49 0.54 0.0525 0.0009 0.1201 0.0021 0.0166 0.0001 308 40 115.22 106192%
YJS-1-19 11.21 97.49 2743.31 0.54 0.0529 0.0014 0.1250 0.0034 0.0171 0.0002 325 61 119.63 109191%
YJS-1-20 9.59 513.40 1302.49 0.03 0.0454 0.0006 0.1104 0.0080 0.0176 0.0002 −33 30 106.48 113194%
YJS-1-N-Granite porphyry
YJS-1-N-01 114.85 1088.50 2855.51 0.38 0.0499 0.0021 0.1233 0.0051 0.0179 0.0003 190701185115297%
YJS-1-N-02 20.38 159.76 462.08 0.35 0.0503 0.0068 0.1205 0.0160 0.0179 0.0004 20825311614114398%
YJS-1-N-03 160.97 1692.06 2995.25 0.56 0.0472 0.0029 0.1179 0.0071 0.0181 0.0002 581361136116291%
YJS-1-N-04 35.28 379.87 810.80 0.47 0.0540 0.0049 0.1320 0.0110 0.0180 0.0003 37015712610115291%
YJS-1-N-05 75.55 756.78 1761.11 0.43 0.0532 0.0035 0.1328 0.0087 0.0181 0.0003 3351191278116291%
YJS-1-N-06 66.89 825.77 1164.35 0.71 0.0524 0.0050 0.1334 0.0131 0.0185 0.0004 30318312712118392%
YJS-1-N-07 79.51 815.40 1340.09 0.61 0.0467 0.0038 0.1196 0.0096 0.0186 0.0003 341841159119289%
YJS-1-N-08 38.91 377.16 880.90 0.43 0.0513 0.0048 0.1243 0.0113 0.0179 0.0004 25516811910114295%
YJS-1-N-09 20.99 173.91 426.44 0.41 0.0461 0.0047 0.1151 0.0116 0.0181 0.0004 21111111116378%
YJS-1-N-10 64.73 714.22 1013.83 0.70 0.0487 0.0042 0.1228 0.0107 0.0180 0.0003 13616511810115297%
YJS-1-N-11 64.07 675.40 1022.22 0.66 0.0528 0.0044 0.1366 0.0110 0.0188 0.0003 32115113010120291%
YJS-1-N-12 53.11 478.45 1477.75 0.32 0.0475 0.0027 0.1192 0.0067 0.0180 0.0003 73961146115299%
YJS-1-N-13 50.42 546.51 960.31 0.57 0.0481 0.0035 0.1191 0.0086 0.0181 0.0003 1061301148116298%
YJS-1-N-14 40.16 385.67 688.99 0.56 0.0523 0.0058 0.1214 0.0134 0.0169 0.0005 29720011612108392%
YJS-1-N-15 42.50 423.53 844.34 0.50 0.0594 0.0064 0.1448 0.0145 0.0179 0.0004 58218013713114381%
YJS-1-N-16 105.47 1228.75 1941.62 0.63 0.0495 0.0029 0.1242 0.0073 0.0180 0.0003 1711041197115296%
YJS-1-N-17 40.44 462.69 776.53 0.60 0.0513 0.0053 0.1243 0.0119 0.0179 0.0004 25317611911115296%
YJS-1-N-18 29.12 314.63 546.49 0.58 0.0546 0.0067 0.1406 0.0182 0.0193 0.0006 39424013416123392%
YJS-1-N-19 119.12 1231.93 2743.31 0.45 0.0504 0.0023 0.1248 0.0057 0.0178 0.0002 214801195114295%
YJS-1-N-20 61.80 574.36 1302.49 0.44 0.0516 0.0039 0.1311 0.0101 0.0181 0.0003 2691431259116292%
YJS-1-N-21 61.14 443.31 1273.44 0.35 0.0492 0.0058 0.1313 0.0151 0.0194 0.0005 15825412514124380%
YJS-3-N-Monzogranite
YJS-3-N-01 104.63 986.19 2513.94 0.39 0.0503 0.0022 0.1250 0.0052 0.0181 0.0002 209731205115196%
YJS-3-N-02 249.85 2730.04 4658.31 0.59 0.0499 0.0018 0.1266 0.0043 0.0184 0.0002 190551214118197%
YJS-3-N-03 239.61 2728.00 4822.05 0.57 0.0492 0.0021 0.1171 0.0049 0.0172 0.0003 156651124110297%
YJS-3-N-04 75.10 870.91 1397.38 0.62 0.0496 0.0034 0.1198 0.0081 0.0174 0.0003 1741241157111296%
YJS-3-N-05 76.93 622.01 1307.41 0.48 0.0475 0.0052 0.1198 0.0130 0.0183 0.0003 7523111512117270%
YJS-3-N-06 58.51 489.58 1105.29 0.44 0.0461 0.0043 0.1129 0.0102 0.0178 0.0004 1991099114277%
YJS-3-N-07 121.57 1193.21 2645.96 0.45 0.0494 0.0022 0.1250 0.0058 0.0182 0.0002 165831205116296%
YJS-3-N-08 157.68 1418.19 2782.14 0.51 0.0461 0.0025 0.1186 0.0062 0.0187 0.0002 1171146119286%
YJS-3-N-09 80.97 680.89 1175.73 0.58 0.0473 0.0060 0.1331 0.0166 0.0204 0.0005 6225412715130378%
YJS-3-N-10 68.04 705.00 1099.18 0.64 0.0495 0.0033 0.1241 0.0079 0.0184 0.0003 1691141197117298%
YJS-3-N-11 161.30 1683.32 3572.29 0.47 0.0504 0.0020 0.1270 0.0052 0.0180 0.0002 215701215115194%
YJS-3-N-12 51.29 467.91 1176.77 0.40 0.0494 0.0036 0.1193 0.0083 0.0178 0.0003 1671201147113299%
YJS-3-N-13 142.89 1193.73 2558.68 0.47 0.0461 0.0038 0.1153 0.0090 0.0181 0.0005 41821118116377%
YJS-3-N-14 60.79 467.31 1214.92 0.38 0.0461 0.0035 0.1076 0.0077 0.0169 0.0004 1671047108273%
YJS-3-N-15 125.55 1337.36 2994.84 0.45 0.0474 0.0025 0.1122 0.0059 0.0170 0.0003 69871085109299%
YJS-3-N-16 120.28 1372.72 1568.35 0.88 0.0503 0.0050 0.1202 0.0117 0.0173 0.0003 20822711511111277%
YJS-3-N-17 74.73 457.53 978.85 0.47 0.0557 0.0078 0.1396 0.0194 0.0182 0.0004 44231713317116237%
YJS-3-N-18 85.79 927.78 1394.39 0.67 0.0492 0.0029 0.1241 0.0070 0.0183 0.0003 1581011196117298%
YJS-3-N-19 154.39 1837.52 2306.19 0.80 0.0472 0.0033 0.1194 0.0090 0.0181 0.0004 581261158115299%
YJS-3-N-20 123.00 1355.49 2586.36 0.52 0.0477 0.0021 0.1181 0.0055 0.0178 0.0002 83811135114199%
YJS-4-N-Quartzdiorite
YJS-4-N-01 134.39 1351.01 2689.18 0.50 0.0478 0.0029 0.1208 0.0073 0.0182 0.0003 9110711671162100%
YJS-4-N-02 94.89 559.17 719.74 0.78 0.0517 0.0049 0.2130 0.0192 0.0304 0.0005 27217219616193398%
YJS-4-N-03 91.00 534.53 761.36 0.70 0.0525 0.0042 0.2230 0.0176 0.0311 0.0006 30914520415197497%
YJS-4-N-04 110.10 712.27 754.03 0.94 0.0541 0.0051 0.2205 0.0197 0.0301 0.0006 37416920216191394%
YJS-4-N-05 93.75 943.05 1783.14 0.53 0.0482 0.0030 0.1197 0.0071 0.0182 0.0003 1081051156116299%
YJS-4-N-06 244.43 2830.67 2923.92 0.97 0.0503 0.0024 0.1249 0.0058 0.0181 0.0003 211821205116297%
YJS-4-N-07 110.15 719.57 817.82 0.88 0.0502 0.0043 0.2006 0.0168 0.0295 0.0006 20515018614188499%
YJS-4-N-08 23.84 187.73 466.13 0.40 0.0608 0.0104 0.1448 0.0243 0.0173 0.0006 63138513722110478%
YJS-4-N-09 127.41 1447.87 1968.51 0.74 0.0483 0.0034 0.1200 0.0083 0.0180 0.0003 11312311581152100%
YJS-4-N-10 56.10 564.89 876.38 0.64 0.0539 0.0056 0.1320 0.0134 0.0182 0.0004 36719212612116292%
YJS-4-N-11 43.58 327.98 535.07 0.61 0.0620 0.0128 0.1553 0.0317 0.0182 0.0005 67443814728116376%
YJS-4-N-12 84.94 745.10 1169.16 0.64 0.0619 0.0046 0.1504 0.0112 0.0175 0.0004 66912514210112276%
YJS-4-N-13 130.44 262.49 391.22 0.67 0.0461 0.0107 0.2020 0.0466 0.0318 0.0009 38018739202692%
YJS-4-N-14 292.64 463.04 625.71 0.74 0.4299 0.1196 14.7234 5.9043 0.1708 0.0496 4017303279838110162737%
YJS-4-N-15 194.51 315.83 385.03 0.82 0.0670 0.0036 1.1887 0.0623 0.1305 0.0022 83682795297911299%
YJS-4-N-16 126.88 1177.01 3047.08 0.39 0.0486 0.0024 0.1188 0.0059 0.0177 0.0003 126861145113299%
YJS-4-N-17 42.50 393.72 689.58 0.57 0.0588 0.0052 0.1469 0.0129 0.0183 0.0004 56015213911117383%
YJS-4-N-18 59.24 575.12 1023.00 0.56 0.0493 0.0043 0.1275 0.0113 0.0188 0.0004 16115912210120398%
YJS-4-N-19 124.67 1240.27 2536.80 0.49 0.0489 0.0027 0.1249 0.0066 0.0185 0.0003 141891206118298%
YJS-4-N-20 229.35 1523.74 2143.53 0.71 0.0527 0.0020 0.2183 0.0082 0.0299 0.0004 315592007190395%
YJS-4-N-21 51.81 557.28 980.10 0.57 0.0485 0.0048 0.1212 0.0117 0.0182 0.0004 126174116111163100%
YJS-4-N-22 381.23 785.23 1414.28 0.56 0.0587 0.0040 0.6689 0.0442 0.0827 0.0013 55515352027512898%
YJS-4-N-23 73.76 721.36 1705.03 0.42 0.0480 0.0031 0.1229 0.0077 0.0185 0.0003 10011211871182100%
YJS-4-N-24 117.02 1300.02 2000.96 0.65 0.0522 0.0026 0.1317 0.0066 0.0181 0.0003 293861266116292%
YJS-4-N-25 40.83 399.03 661.76 0.60 0.0496 0.0064 0.1328 0.0174 0.0193 0.0005 17724812716123397%
Table
Table 2. Major (wt%) and trace (ppm) elements of the granitoids from the Yuejinshan copper–gold deposit.
Table 2. Major (wt%) and trace (ppm) elements of the granitoids from the Yuejinshan copper–gold deposit.
No.YJS-15YJS-2aYJS-009YJS-022YJS-044YJS-1-1YJS-1-2YJS-1-4 YJS-2-1YJS-2-2YJS-014YJS-0450203-003 YJS-3-1YJS-3-2 YJS-4-1YJS-037YJS-001YJS-002
Rock TypeGranite Porphyry Granodiorite Monzogranite Quartzdiorite
Major element (wt%)
SiO271.1575.1676.575.569.678.1678.0377.84 68.768.5468.570.370.1 77.2476.81 64.4557.668.163.8
Al2O313.8213.0212.5512.41412.512.3412.44 15.9315.6715.3514.714.65 12.5712.4 16.2419.415.1515.65
Fe2O30.650.181.451.943.020.260.210.39 0.330.623.372.652.54 0.370.35 1.334.574.736.5
Na2O3.533.223.963.744.444.063.67 3.843.783.563.664.52 4.063.96 4.156.833.93.97
K2O2.563.783.573.822.843.393.194.2 2.512.612.572.892.56 3.93.88 1.852.291.672.04
CaO2.451.760.650.61.681.141.110.69 3.663.543.442.731.98 0.840.85 3.982.712.612.55
P2O50.120.050.010.020.120.0200 0.130.110.140.110.11 0.010.01 0.210.180.180.27
TiO20.420.190.070.10.570.070.070.07 0.50.460.460.370.35 0.070.07 0.670.650.50.72
MgO1.30.410.10.141.090.120.080.23 1.471.341.540.981.4 0.060.06 1.271.740.981.48
MnO0.080.050.010.020.010.010.010.01 0.030.030.060.020.07 0.020.02 0.030.040.020.02
TFe2O33.641.911.451.943.020.880.831.41 3.092.843.372.652.54 1.31.28 6.224.574.736.5
LOI0.960.490.540.761.51 0.480.551.05 2.91.11.53
TOTAL99.7499.8699.6299.3599.03 99.6899.1499.62 99.1799.4799.03
Trace element (ppm)
Rb84.297.39776.980.741.735.253.5 57.960.699.199.982.1 73.570 87.361.293107.5
Ba519.31128111021009941177.81062.4894.7 587.9599.1633705697 1063.21082 479.112701045553
Th13.411.212.1512.610.7511.8311.3714.29 21.324.6112.1514.9513.05 12.2410.98 5.1419.155.774.05
U2.212.522.882.193.062.512.284.62 2.723.641.812.951.77 2.862.66 0.983.781.491.2
Ta0.981.452.21.50.91.711.852.28 0.840.821.20.81.3 1.961.9 1.231.31.21.1
Nb12.4916.8419.414.71318.9915.916.1 14.0413.199.111.37.9 19.317.6 16.31520.718.2
Sr185.1187.479.113127063.879.936 246.2254.2396422306 40.136.2 225.1346272354
Zr237.7115.79710329755.948.151.1 106.7111.9163169142 54.250.8 127319185161
Trace element (ppm)
Hf7.274.074.43.88.12.682.362.53 4.314.484.84.84.3 2.712.53 3.448.95.34.5
La35.9431.1729.22831.627.4931.5130.15 88.85107.8142.547.942.2 29.0427.8 30.1562.534.229
Ce74.2157.6755.353.465.353.7462.8663.37 154.14182.078291.481.6 58.4755.74 55.871306457.6
Pr8.736.286.295.377.195.626.526.84 15.1918.368.199.118.33 6.335.84 6.413.257.016.35
Nd32.4921.6823.619.328.720.9724.3726.27 51.3362.4428.231.629 24.2322.01 24.8551.427.225.6
Sm6.693.95.333.435.744.054.695.59 6.437.854.454.84.73 5.234.46 4.69.865.635.01
Eu1.080.570.390.430.860.50.50.36 1.21.231.131.050.87 0.460.47 1.111.3510.83
Gd5.923.424.622.755.243.43.875.12 4.735.513.153.452.89 4.724.24 4.017.795.24.88
Tb1.010.580.690.450.850.550.610.92 0.540.630.440.420.4 0.860.74 0.651.090.780.71
Dy5.543.174.672.855.553.373.595.95 2.322.652.132.191.9 5.774.86 3.97.015.014.57
Ho1.110.630.830.61.120.650.681.19 0.390.450.350.370.39 1.140.96 0.741.320.970.88
Er3.241.952.741.953.481.9723.63 1.161.311.061.221.03 3.422.89 2.144.122.792.79
Tm0.560.370.40.290.470.320.320.58 0.150.180.180.150.16 0.580.48 0.340.570.40.38
Yb3.322.242.712.093.342.222.193.94 0.951.081.091.031.01 3.893.26 2.133.952.862.6
Lu0.460.350.410.310.480.350.350.6 0.140.160.160.170.16 0.590.5 0.330.60.410.41
Y30.4918.9525173018.5119.1436.83 11.2312.1310.311.110.5 34.8529.49 21.5336.826.325.5
ΣREE180.3133.97137.18121.22159.92125.19144.08154.5 327.53391.72175.03194.86174.67 144.74134.25 137.22294.81157.46141.61
LREE159.15121.26120.11109.93139.39112.36130.45132.57 317.13379.76166.47185.86166.73 123.77116.32 122.98268.36139.04124.39
HREE21.1512.717.0711.2920.5312.8313.6221.93 10.3911.968.5697.94 20.9617.93 14.2426.4518.4217.22
LREE/HREE7.539.557.049.746.798.769.586.05 30.5131.7419.4520.6521 5.96.49 8.6410.157.557.22
LaN/YbN7.779.977.739.616.798.8910.315.49 67.0871.7327.9733.3629.97 5.356.13 10.1511.358.588
δEu0.520.470.230.410.470.40.350.2 0.630.540.880.750.67 0.280.32 0.770.450.560.51
δCe10.950.9511.0211.021.04 0.940.921.0111 1.011.02 0.941.050.960.99
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Wang, Q.; Wei, Y.; Yang, Y.; Peng, H. Zircon U–Pb Ages and Geochemistry of Granitoid in the Yuejinshan Copper–Gold Deposit, NE China: Constraints on Petrogenesis and Metallogenesis. Minerals 2021, 11, 1206. https://doi.org/10.3390/min11111206

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Wang Q, Wei Y, Yang Y, Peng H. Zircon U–Pb Ages and Geochemistry of Granitoid in the Yuejinshan Copper–Gold Deposit, NE China: Constraints on Petrogenesis and Metallogenesis. Minerals. 2021; 11(11):1206. https://doi.org/10.3390/min11111206

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Wang, Qingshuang, Yanlan Wei, Yanchen Yang, and Hu Peng. 2021. "Zircon U–Pb Ages and Geochemistry of Granitoid in the Yuejinshan Copper–Gold Deposit, NE China: Constraints on Petrogenesis and Metallogenesis" Minerals 11, no. 11: 1206. https://doi.org/10.3390/min11111206

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